B Gourcerol
email: gourcerol.blandine@gmail.com

E Gloaguen

J Melleton

J Tuduri

Xavier Galiegue

Re-assessing the European lithium resource potential -A review of hard-rock resources and metallogeny

Keywords: lithium, metallogeny, pegmatite, Europe, resources

Highlights:

 Lithium is not rare in Europe and is well represented in different orogenic settings;  A pre-existing Li-rich source is required for Li-enrichment processes;  Lithospheric thickening may reflect a favorable process for concentrating Li;  Extensional geodynamical settings appear favorable for Li enrichment.

Introduction

Over the past decade, lithium has become a strategic metal due to its physical and chemical properties, being the lightest solid element and an excellent conductor of heat and electricity. This makes it an excellent candidate for electromobility and green technologies, such as Li-ion batteries and other energy-storage devices [START_REF] Tarascon | Building better batteries[END_REF][START_REF] Tarascon | Is lithium the new gold?[END_REF][START_REF] Ziemann | Tracing the fate of lithium--The development of a material flow model[END_REF][START_REF] Manthiram | Lithium battery chemistries enabled by solid-state electrolytes[END_REF]. As a result, Li demand has increased significantly and a "lithium rush" is currently happening world wide (e.g., Roskill Information Services Ltd., 2016). In this context, the identification and assessment of lithium mineral resources and -reserves is a crucial step, as is understanding lithium metallogeny, a major subject for discovering new mineral resources.

Historically, two distinct deposit types are identified: 1) brine deposits in which the lithium grade is about 0.1% Li 2 O; and 2) hard-rock deposits where the lithium grade generally varies from 0.6 to 1.0% Li 2 O hosted by various Li-bearing minerals [START_REF] Kesler | Global lithium resources: relative importance of pegmatite, brine and other deposits[END_REF][START_REF] Mohr | Lithium resources and production: Critical assessment and global projections[END_REF].

The brine-deposit type refers to relatively recent (mostly Quaternary), enclosed, tectonically active basins that contain Li-rich lacustrine evaporites. These are produced by high evaporation rates in an arid to hyper-arid climate and/or by various water inputs such as groundwater and spring water circulation (e.g., [START_REF] Ericksen | Geology and resources of salars in the central Andes[END_REF][START_REF] Bradley | A preliminary deposit model for lithium brines[END_REF]. In these deposits, the Li source and enrichment processes are specific to each brine. However, the most accepted model is the weathering of felsic rocks and/or local hydrothermal activity driven by a magmatic heat source through active channel pathways [START_REF] Bradley | A preliminary deposit model for lithium brines[END_REF][START_REF] Hofstra | Silicate melt inclusion evidence for extreme pre-eruptive enrichment and post-eruptive depletion of lithium in silicic volcanic rocks of the Western United States: Implications for the origin of lithium-rich brines[END_REF]. In North America, several deposits have been identified within the Basin and Range extensional province of the western United States, including the Clayton Valley and the Great Salt Lake (e.g., [START_REF] Bradley | A preliminary deposit model for lithium brines[END_REF]. In South America and more particularly on the Puna Plateau, brine deposits, referred to as salars, cover an area of about 400,000 km 2 from northern Argentina and northern Chile to western Bolivia (Ericksen and Salas,

Overview of hard-rock lithium deposit types in Europe

A compilation of lithium occurrences and -deposits was made by collecting information from various geological survey organizations, exploration and mining companies, and scientific research projects and related publications. This resulted in an up-to-date quantification of the European lithium potential, considering only hard-rock ore types, identifying 527 lithium occurrences, projects and deposits (provided as electronic supplementary material). This was almost five times more than the previous Mineral4EU-ProMine (http://minerals4eu.brgm-rec.fr/) inventory [START_REF] Cassard | ProMine Mineral Databases: New tools to assess primary and secondary mineral resources In 3D, 4D and Predictive Modelling of Major Mineral Belts in Europe[END_REF].

In addition, mineral resource and -reserve and -production data were gathered from available published data by exploration and mining companies, such as technical and annual reports, from data repositories (e.g., https://sedar.com) and from governmental surveys. Note that the data from England, France and, locally, Germany are based on historical (before 1995), non-compliant CRIRSCO (Committee for Mineral Reserves International Reporting Standards) compliant estimates.

We emphasize that lithium deposits related to seawater, and geothermal-and oilfield brines are not considered in this study.

According to our compilation (and previous ones, e.g., Christmann et al., 2015), two distinct categories of lithium deposits and occurrences are found in Europe. They are: 1) Magmatic-related (Fig. 1A,B,C) deposits; and 2) Sedimentary/hydrothermal-related deposits (Fig. 1D).

Magmatic-related deposits

2.1.1 Rare-metal granites Rare-metal granites (RMG; Černý et al., 2005) are felsic, peraluminous to peralkaline intrusive rocks that host magmatic disseminated mineralization. They occur as very small, mostly subsurface, granitic plugs, typically less than 1 km 3 , such as the Beauvoir RMG in France [START_REF] Raimbault | Geochemical evidence for a multistage magmatic genesis of Ta-Sn-Li mineralization in the granite de Beauvoir, French Massif Central[END_REF]Fig. 1A). According to their geochemistry and geodynamic setting, three main types [START_REF] Linnen | Granite-related rare-element deposits and experimental constraints on Ta-Nb-W-Sn-Zr-Hf mineralization[END_REF][START_REF] Černý | The classification of granitic pegmatites revisited[END_REF] are recognized:

1) Peralkaline RMG have very high contents of F, REE, Y, Zr, Nb, related to anorogenic settings; their Li content is relatively moderate (up to a few 1000 ppm) and is mainly illustrated by zinnwaldite and polylithionite occurrences (Tables 1,2). This type is not documented in Europe;

2) Metaluminous to peraluminous, low-to intermediate-phosphorus RMG with high concentrations of Nb, Ta, Sn, that occur in both post-and an-orogenic geodynamic settings. The Li content again is moderate (up to a few 1000 ppm) and is mostly related to zinnwaldite. Examples include Cinovec (Fig. 1C), Podlesi (Fig. 2A), the Sejby and Homolka granites in the Czech Republic, the Chavence and Les Châtelliers granites in France (Table 2; Černý et al., 2005 and references therein); 3) Peraluminous, high-phosphorus RMG with strong enrichment in Ta, Sn, Li and F, occurring in a continental-collision setting. In this RMG type, Li concentrations can be high, from 0.5% to 1.0% Li 2 O, and occurring as lepidolite, Li-rich muscovite and amblygonite-montebrasite series, such as at Beauvoir (Figs. 1A,2B), Montebras (Fig. 2C) and the Richemont rhyolite dike in the French Massif Central, and Argemela in Portugal (Table 2; Černý et al., 2005 and references therein).

2.1.2 LCT Pegmatites With the exception of some rare giant Precambrian occurrences, lithium-cesium-tantalum (LCT) pegmatites (e.g., [START_REF] London | Pegmatites[END_REF][START_REF] London | Ore-forming processes within granitic pegmatites[END_REF][START_REF] Černý | The classification of granitic pegmatites revisited[END_REF] are relatively small-sized (a few m 3 to <1/2 km 3 ; Fig. 1B), coarse-grained and/or aplitic igneous rocks of granitic composition. Geochemically, Li-rich LCT pegmatites are similar to peraluminous high-phosphorus RMG. They are the result of crystallization of fluid-rich melts, enriched in various amounts of incompatible elements, such as Li, Ta, Sn, Rb, Be, Nb and Cs, and strongly depleted in REEs, close to chondritic values [START_REF] London | Geochemical features of peraluminous granites, pegmatites, and rhyolites as source of lithophile metal deposits[END_REF][START_REF] London | Granitic pegmatites -An assessment of current concepts and directions for the future[END_REF][START_REF] London | Pegmatites[END_REF][START_REF] London | Ore-forming processes within granitic pegmatites[END_REF][START_REF] Černý | The classification of granitic pegmatites revisited[END_REF][START_REF] Černý | Granitic pegmatites as reflections of their sources[END_REF][START_REF] Linnen | Granitic pegmatites as sources of strategic metals[END_REF].

Pegmatites can form under various P/T conditions (Table 3) representing various classes (e.g., Černý, 1989, 1990; Černý et al., 2012). They are generally clustered in kilometer-size pegmatite fields (e.g., the Ambazac pegmatite field, Deveaud et al., 2013;[START_REF] Silva | Chapter 3 -Spatial geostatistical analysis applied to the Barroso-Alvão rare-elements pegmatite field (Northern Portugal)[END_REF], and occur as dikes and/or sills (e.g., Emmes pegmatite, Finland, [START_REF] Eilu | Metallogenic areas in Finland[END_REF]; Gonçalo pegmatite field, Portugal, [START_REF] Ramos | Mineralizações de metais raros de Seixo Amarelo-Gonçalo (Guarda)[END_REF] or lenticular bodies (e.g., Bohemian pegmatites, [START_REF] Melleton | How are the emplacement of rareelement pegmatites, regional metamorphism and magmatism interrelated in the Moldanubian Domain of the Variscan Bohemian Massif Czech Republic[END_REF]. Contacts with hostrock range from relatively sharp to progressive, depending on the nature of the host and the depth of emplacement. Host-rocks are mainly metasedimentary and/or metavolcanic rocks metamorphosed from lower greenschist to amphibolite facies (Černý, 1992) as well as granite intrusions (e.g., Gonçalo, Ambazac).

LCT pegmatites show heterogeneous textures and compositions, and are composed of variable amounts of quartz, plagioclase, potassium feldspar, micas, with various amounts of garnet, tourmaline, apatite and (usually) accessory Li-bearing minerals -locally rock-forming -such as spodumene, petalite, etc. Although not systematically observed, LCT pegmatites generally show layering and/or concentric zoning. Lithium-bearing minerals, including spodumene, petalite, the amblygonitemontebrasite group, lepidolite (Figs. 2D,E), eucryptite, elbaite and the lithiophilite-triphylite group are commonly found in pegmatite bodies, whereas cookeite and holmquistite occur mainly in the pegmatite aureole, or as secondary minerals (e.g., cookeite after petalite). Note that eucryptite may reflect the alteration of primary spodumene. Li 2 O content varies as a function of the LCT pegmatite subtype and the Li-bearing minerals themselves (Table 3), ranging from 0.5 to 1.5%.

Mixed niobium-yttrium-fluorine (NYF)-LCT pegmatites are known from Norway (e.g., Birkeland, Frikstad, Skripeland) and Ukraine (Volodarsk-Volynsky). In Norway, pegmatite fields such as Evje-Iveland show a typical initial NYF chemical signature, but are depleted in REEs and F in replacement areas. Moreover, the replacement zones show a "cleavelandite signature" as well as chemical and mineralogical LCT features, including beryl, columbite group minerals and tourmaline (Černý, 1991a, b). Lithium-ore tonnages or grades are not reported for these pegmatites.

2.1.3 Greisen Greisen deposits (e.g., St Austell, UK; Cinovec, CZ) result from a high-temperature hydrothermal transformation of fractionated granitic intrusions (pegmatites, granites) with their upper part being a porous muscovite-quartz assemblage at the granite/host-rock contact. They can occur as multi-stage swarms crosscutting Sn-W quartz veins (e.g., [START_REF] Černý | The classification of granitic pegmatites revisited[END_REF][START_REF] Štemprok | The petrogenesis of a wolframite-bearing greisen in the Vykamov granite stock, Western Krusné Hory pluton (Czech Republic)[END_REF]Launay et al., 2018), or may form up to 100-m thick units with irregular to sheet-like bodies. Li is mainly hosted in micas, such as Li-rich muscovite, lepidolite, zinnwaldite, and amblygonite-montebrasite group minerals. Peraluminous RMG and metaluminous intrusions are favorable rock types for the development of such deposit types (Fig. 1C), whereas fractionated granites appear to be unrelated with significant Li endowment. Thus, the Li 2 O content in the greisen around the world-class Panasqueira W deposit (Portugal) is only about 732 ppm [START_REF] Bussink | Geochemistry of the Panasqueira tungsten-tin deposit[END_REF], whereas Li 2 O values from the Erzgebirge province (e.g., [START_REF] Štemprok | The petrogenesis of a wolframite-bearing greisen in the Vykamov granite stock, Western Krusné Hory pluton (Czech Republic)[END_REF][START_REF] Jarchovský | The nature and genesis of greisen stocks at Krasno, Slavkovsky les areawestern Bohemia, Czech Republic[END_REF] vary from 80 to 3100 ppm for greisen of the RMG Vykmanov and Schnöd granites.

Quartz, cassiterite, wolframite, micas, topaz, tourmaline, sericite and chlorite are common in greisen, showing vertical and horizontal zoning. Alteration is generally shown by kaolinization, tourmalinization, feldspathization (microclinization and/or albitization) and greisenization forming haloes around the granitic body. REE enrichment may occur and is indicated by precipitation of monazite, xenotime and other REE-rich minerals.

Note that this deposit type can be related to both magmatic and hydrothermal processes. Here, we consider a "granite-related" classification even though hot hydrothermal fluids are involved.

Co-products commonly consist of industrial minerals, such as feldspar, quartz and kaolin (e.g., Beauvoir, France); Sn and W are of first interest, Be, Ta, In, Sc, Rb representing potential byproducts.

2.1.4 Quartz-montebrasite hydrothermal veins Several authors (e.g., [START_REF] Martín-Izard | Cassiterite U-Pb geochronology constrains magmatic-hydrothermal evolution in complex evolved granite systems: The classic Erzgebirge Tin Province (Saxony and Bohemia)Martínez[END_REF][START_REF] Roda-Robles | Geology and mineralogy of Li-mineralization in the Central Iberian Zone (Spain and Portugal)[END_REF] reported the existence of quartz-montebrasite hydrothermal veins associated with leucogranitic cupolas in the central part of the Central Iberian Zone in Spain (e.g., Valdeflores, Barquilla, Golpejas, El Trasquilón) and Portugal (e.g., Argemela area and Massueime).

Hosted by granites or metasedimentary rock of the Schist-Metagreywacke Complex, these veins are generally <1 m thick and fill fracture sets. They contain a high proportion of quartz and few minerals such as K-feldspars and micas [START_REF] Roda-Robles | Geology and mineralogy of Li-mineralization in the Central Iberian Zone (Spain and Portugal)[END_REF]. Accessory minerals such as Nb-Ta oxides, cassiterite and sulfides are common, and Li-bearing minerals consist of the montebrasite-amblygonite series (Table 1). Note that only few Li 2 O values are reported for these occurrences (i.e., 0.45% Li 2 O on average for the Argemela mine, PANNN, 2017) and, except for the Argemela mine, such deposits appear to be relatively uneconomic in view of their small size.

2.1.5 Tosudite mineralization related to gold deposits An occurrence of Li-bearing tosudite in the the Châtelet gold deposit (France) was reported in several studies [START_REF] Braux | Le Châtelet gold-bearing arsenopyrite deposit, Massif Central France: Mineralogy and geochemistry applied to prospecting[END_REF][START_REF] Piantone | Zoned hydrothermal alteration and genesis of the gold deposit at Le Châtelet (French Massif Central)[END_REF]; Li 2 O values range from 142 to 920 ppm. These authors suggested that the Li is related to late hydrothermal fluid circulation, itself related to the RMG emplacement in the northern part of the French Massif Central.

2.2 Sedimentary/hydrothermal/supergene deposits These types include deposits related to either sedimentary rocks affected (or not) by hydrothermal processes, or surficial rocks affected by supergene weathering.

Jadar deposit type

In 2004, Rio Sava (a subsidiary of the Rio Tinto mining corporation) discovered the Jadar Basin in Serbia, now considered as a "non-conventional" world-class lithium deposit through the occurrence of the mineral jadarite [START_REF] Stanley | Jadarite, LiNaSiB3O7(OH), a new mineral species from the Jadar Basin, Serbia[END_REF], a lithium boron silicate (Table 1). The basin consists of a relatively large (>20 kilometers long) intramontane lacustrine (paleo)-evaporite basin composed of dolomite, marble, various siliciclastic sedimentary rocks, pyroclastic units and notable oil shales [START_REF] Obradovic | Phytogenic lacustrine sedimentation -oil shales in Neogene from Serbia Yugoslavia[END_REF]. The mineralization is hosted in a 400 to 500 m thick Miocene sedimentary unit dominated by calcareous claystone, siltstone, sandstone and clastic rocks, unconformably overlying a Cretaceous basement composed of various metasedimentary rocks, limestone, sandstone and granite, including Miocene intrusions (Fig. 1D).

The lithium and borate mineralization occurs as 1.5 to 35 m thick stratiform lenses of three gently dipping tabular zones covering a surface area of 3 by 2.5 km. The ore is composed of jadaritebearing siltstone and mudstone with locally interbedded sodium borate lenses (i.e., ezcurrite, kernite, borax; Fig. 1D). Jadarite occurs as 1-10 mm white and rounded grains, nodules or concretions in the siltstone or mudstone matrix that contains various amounts of calcite, dolomite, K-feldspar, rutile, albite, pyrite, muscovite and ilmenite (Fig. 2F; [START_REF] Tinto | Notice to ASX, Increase to Jadar Project Mineral Resources[END_REF][START_REF] Stanley | Jadarite, LiNaSiB3O7(OH), a new mineral species from the Jadar Basin, Serbia[END_REF]. In 2017, the mineral resources were reported as 135.7 Mt of ore at a grade of 1.86% Li 2 O and 15.4% B 2 O 3 [START_REF] Tinto | Notice to ASX, Increase to Jadar Project Mineral Resources[END_REF], representing a giant deposit of 2.524 Mt of Li 2 O.

2.2.2 Mn-(Fe) deposits Among the various types of host-rocks for Li-bearing minerals in Europe, the small-scale and discontinuous Mn-Fe-rich sedimentary units (e.g., Drosgol Mine in Scotland and Clews Gill in England), exploited in the 19 th century for their Fe and Mn contents, are a favorable site for secondary Li-oxides such as lithiophorite (Table 1). Stratigraphically, they can be subdivided into two distinct units: 1) a reddish siliciclastic host rock, mainly pelite, shale and/or sandstone, enhanced in Mn and Fe relative to the average shale composition; and 2) discontinuous Mn lenses or layers (coticules). The minerals include cryptomelane, goethite, hematite and other manganese oxides including Li-rich lithiophorite, chalcophanite and pyrolusite.

The Li 2 O content in lithiophorite is relatively low (1.23 wt.% for Li 2 O versus 55 wt.% for MnO), indicating an uneconomic lithium grade. However, its occurrence is relatively important in view of the sedimentary and European histories (cf. Section 3 hereafter).

2.2.3 Bauxite deposits Similar to the Mn-Fe deposit type, bauxite deposits can contain various amounts of lithiophorite, cookeite (Table 1) and tosudite (Li-rich gibbsite; [START_REF] Nishyama | Lithium-bearing tosudite[END_REF]. Lithiophorite is the most common Li-bearing manganese oxide mineral in karst bauxites. It occurs in several localities, such as the Halimba, Fenyöfö and Kincsesbanya deposits in Hungary, where aluminum and gallium in bauxite deposits were exploited from the 1950s to recently [START_REF] Anderson | The mineral Industry of Hungary; In 2012 Yearbook[END_REF].

Al and Mn are of first interest in this deposit type. The presence of lithiophorite and local cookeite reflect Li enrichment, though this is not systematically evaluated. However, values of up to 0.53% Li 2 O within bauxite are known from China [START_REF] Wang | Discovery and preliminary study of the high tungsten and lithium contents in the Dazhuyuan bauxite deposit, Guizhou, China[END_REF] and the USA [START_REF] Tourtelot | Lithium, a preliminary survey of its mineral occurrence in flint clay and related rock types in the United States[END_REF].

2.2.4

Other lithium deposit types A few other deposit types show relatively minor anomalous lithium contents, including: 1) Mississippi-Valley type (MVT) deposits that include some lithiophorite (Usingen, Germany), and 2) Aalenian black shales from the Dauphinois region, Isère, France, where cookeite is disseminated in black shale and in tension gashes crosscutting the shales [START_REF] Jullien | Occurrences de cookéite et de pyrophyllite dans les schistes du Dauphinois (Isèe, France) -Conséquences sur la répartition du métamorphisme dans les zones extemes alpines[END_REF]. For the latter occurrence, values [START_REF] Henry | Evolution of synmetamorphic veins and their wallrocks through a Western Alps transect: No evidence for large-scale flow. Stable isotope, major-and traceelement systematics[END_REF] are in the range of 9 to 1 847 ppm Li 2 O with an average of 441 ppm Li 2 O (n=10). These lithium occurrences are symptomatic for local conditions allowing minor enrichment, implying that they are not economically significant regarding their Li content.

2.3

Lithium resources and reserves In Europe, lithium resources and reserves have been estimated or evaluated according to a CRIRSCO (i.e., Committee for Mineral Reserves International Reporting Standards) reporting system, or based on historical evaluations, for only 35 sites (Table 4). Thirsteen occurrences in England, Ireland, France and Germany, such as Beauvoir, Montebras, St Austell or Aclare, were evaluated before systematic reporting was established, and their mineral-resource and -reserve estimates are mostly based on historic evaluations by geological survey organizations. Fifteen projects, including Jadar, are defined in the Australian JORC classification; one project (Zinnwald) was defined in the European PERC; one project (Alberta I) is defined in the Canadian NI43-101 system; Four projects in Ukraine are defined in an unknown system (Table 4); and one project is defined in the United Nations Framework Classification (UNFC). This list reflects the active exploration of lithium in Europe.

However, most of these deposits report mineral resources and only five specify reserve values, indicating that a feasibility study was carried out. This generally includes a study of potential processing and metallurgical-treatment methods, resulting in an economically feasible recovery of lithium from the various Li-bearing minerals.

In order to compare the Li-content in known Li-deposits, the sum of ore production + ore reserves + ore resources has been converted into contained Li 2 O (ore tonnage x ore grade) for each deposit. These deposits were then categorized and classified into categories A, B, C, D and E 1 according to their commodities and their reported mineral resources and -reserves (Table 4), following the system of the European ProMine database [START_REF] Cassard | ProMine Mineral Databases: New tools to assess primary and secondary mineral resources In 3D, 4D and Predictive Modelling of Major Mineral Belts in Europe[END_REF]. Note that we consider only the A, B, C and D categories as (potential) lithium deposits (Table 4), which corresponds to 28 deposits.

Among them, three deposits are identified as category A, including the Cinovec (Czech Republic), St Austell (UK) greisen and the Jadar deposit (Serbia). However, the historical estimate by the British Geological Survey for the St Austell deposit may be unrealistic, as it was based on extraction from an area of about 92.5 km 2 on the edges of protected landscape zones (British Geological Survey, 2016).

Lithium occurrences appear to be well distributed in Europe. However, the Iberian area and Finland regroup most of the identified lithium deposits (Table 4), indicating that these countries are relatively active in lithium exploration and suggesting that they have a strong Li-potential.

Lithium metallogeny in Europe throughout the Earth's evolution

In Europe, several orogenic events throughout geological history are associated with lithium mineralization. In this section, we assess and contextualize the lithium mineralization to orogenic features in order to establish-if possible-potential metallogenetic settings.

As a reminder, Europe's landmass results from a long geological history spanning 3.6 billion years, including the assemblage of numerous continental blocks. The European lithosphere can be broadly divided into two large regions: 1) The old East European Craton, partly covered by weakly deformed Phanerozoic and Meso-to Neo-Proterozoic rift and platform successions, mostly located in eastern and north-eastern Europe; and 2) A thinner, dominantly Phanerozoic, lithosphere, accreted to 1 Category refers to: Category A ≥ 1,000,000 t Li 2 O; 1,000,000 t ≥ Category B ≥ 100,000 t Li 2 O; 100,000 t ≥ Category C ≥ 50,000 t Li 2 O; 50,000 t ≥ Category D ≥ 5,000 t Li 2 O; Category E < 5,000 t Li 2 O, based on the sum of production + reserves + resources. the East European Craton during Palaeozoic and younger orogenies, mostly in Western Europe (e.g., [START_REF] Gee | The Timanide, Caledonide and Uralide orogens in the Eurasian high Arctic, and relationships to the palaeo-continents Laurentia, Baltica and Siberia[END_REF][START_REF] Artemieva | EUNAseis: A seismic model for Moho and crustal structure in Europe, Greenland, and the North Atlantic region[END_REF].

Hard-rock lithium mineralization in European Archean to Paleo-Proterozoic terranes

3.1.1 The Ukrainian Shield (3.5 to 1.9 Ga) The Ukrainian Shield forms an assembly of Precambrian crystalline megablocks that is 900 km long and 60-150 km wide in the central part of the country (Fig. 3A). This area is fault-bounded by the younger Dnister-Fore Black Sea and the Dniprovsko-Donnetska metallogenic provinces, and was affected by three distinct magmatic events at ca. 3.2, 2.6 and 1.9 Ga [START_REF] Vinogradov | The geologic age of pre-Cambrian rocks of the Ukrainian and Baltic shields[END_REF], which may have been partly coeval with the Svecofennian magmatism (2.1 to 1.8 Ga).

Several Li-rich deposits and occurrences are reported, such as: 1) the spodumene-and petalitesubtype of lithium-cesium-tantalum (LCT) pegmatites that occur in the Dnester-Bug (Podolia) and Azov Megablocks (e.g., Krutaya Balka, Nadyia); and 2) zinnwaldite and lepidolite occurrences in mixed miarolitic niobium-yttrium-fluorine (NYF)-LCT pegmatites (e.g., Volodarsk-Volynsky) and rare-metal granites (RMG), such as the Perzhanskoe ore district) in the Northern Volyn Megablock [START_REF] Kvasnista | Carbon isotopic composition of diamonds in Ukraine and their probable polygenetic nature[END_REF].

Although these lithium occurrences are known, only very little information is available. This makes their evaluation, regarding metallogenic settings and geological context from a European perspective, very difficult.

The Svecofennian orogenic belt (2.1 to 1.8 Ga)

The Svecofennian orogenic belt (Fig. 3) is part of the Columbia/Nuna supercontinent accretion that took place from 2.1 to 1.8 Ga [START_REF] Zhao | Review of global 2.1-1.8 Ga orogens: Implications for a pre-Rodinia supercontinent[END_REF]. It consists of magmatic-arc accretionary phases joining the juvenile Svecofennian arc terrane to the Archean Karelia Craton [START_REF] Nironen | The Svecofennian Orogen: A tectonic model[END_REF] along the Luleå-Kuopio thrust zone (Fig. 3; [START_REF] Zhao | Review of global 2.1-1.8 Ga orogens: Implications for a pre-Rodinia supercontinent[END_REF].

Prior to the Svecofennian orogen, continental break-up of the Karelian Province led to the formation of an ocean basin and deposition of sedimentary units such as the 1.92 Ga Pohjanmaa schist belt. Initial accretion started at 1.91 Ga and ended at 1.87 Ga, followed by large-scale extension in a back-arc setting (1.87-1.84 Ga) shown by psammites/pelites and intruded by granites and mafic dikes [START_REF] Korja | The Svecofennian orogen-a collage of microcontinents and island arcs[END_REF]). An oblique continent-continent collision occurred from 1.87 to 1.79 Ga, illustrated by the advancing accretion of retro-arc fold-and-thrust belts with alkaline bimodal magmatism (e.g., [START_REF] Lahtinen | Palaeproteroizoic accretionary processes in Fennoscandia[END_REF]. Significant lithospheric thickening, local migmatization and formation of S-type granites in southern Finland and central Sweden occurred as well. Finally, gravitational collapse ended the orogen between 1.79 and 1.77 Ga. Two major amphibolite grade metamorphic events are recorded at 1.88-1.87 Ga [START_REF] Lecomte | Uraniferous bitumen nodules in the Talvivaara Ni-Zn-Cu-Co deposit (Finland): Influence of metamorphism on uranium mineralization in black shales[END_REF] and 1.83 to 1.80 Ga [START_REF] Eilu | Metallogenic areas in Finland[END_REF]. Within this geological framework, lithium mineralization took place in metasedimentary and metavolcanic units along major fault and shear zones. They are dated as relatively late, between 1.8 to 1.79 Ga (Fig. 3, Table 5; e.g., [START_REF] Alviola | Svecofennian rare-element granitic pegmatites of the Ostrobothnia region, western Finland: their metamorphic environment and time of intrusion[END_REF], post-dating local migmatization. They include the ca. 1.88-1.86 Ga Vaasa Migmatite Complex on the margins of the Evijärvi belt [START_REF] Suikkanen | The age and origin of the Vaasa migmatite complex revisited[END_REF], and the ca. 1.84-1.82 Ga late-orogenic migmatizing microcline granites in southwestern Finland [START_REF] Kurhila | U-Pb ages and Nd isotope characteristics of the late orogenic, migmatizing microcline granites in southwestern Finland[END_REF], and appear coeval with the regional amphibolite-grade metamorphism. The mineralization occurs as LCT pegmatite fields, such as the Kaustinene and Somero-Tammela fields (Fig. 3). The Kaustinene one occurs in the 1.92 Ga Pohjanmaa schist belt comprising the Länttä, Syväjärvi and Outovesi deposits, which are albite-spodumene pegmatites owned by Keliber Oy. In the Somero-Tammela region (Fig. 3), the petalite/spodumene Luolamaki, Hirvikallio and Kietyömaäki LCT pegmatites, owned by Nortec Minerals Corp., are hosted in the Håme belt that consists of metavolcanic rock intercalated with metagreywacke and metapelite. In these pegmatites, petalite was formed first and later converted to spodumene, suggesting a temperature decrease at constant pressure during crystallization that involved rapid cooling of the terranes [START_REF] Eilu | Metallogenic areas in Finland[END_REF]. Triphylite is reported from several LCT pegmatites, mainly in Sweden.

The Sveconorwegian orogenic belt (1140 to 850 Ma)

Part of the Grenvillian orogeny, the Sveconorwegian orogenic belt is related to the collision between Fennoscandia and an undetermined major plate (likely Amazonia), which contributed to the Rodinia supercontinent assemby (e.g., Li et al., 2008). The orogen spans from 1140 to 850 Ma, amalgamating Mesoproterozoic (1750-1500 Ma) lithotectonic units separated by major shear zones (Bingen et al., 2008a, b); according to these authors, the orogen can be divided into several tectonic phases. Among these, the Arendal phase (1140-1080 Ma) marks the collision between the Idefjorden and Telemarkia terranes (Fig. 3). This initial phase was related to closure of an oceanic basin, and subsequent accretion of a volcanic arc and a high-grade metamorphic event (ca. 1140(ca. -1125 Ma) Ma). The Adger phase (1050-980 Ma) corresponded to oblique continent-continent collision, and underthrusting and burial/exhumation of the Idefjorden Terrane (Fig. 3). This phase was contemporaneous with crustal thickening of the Telemarkia Terrane, when widespread syn-collisional magmatism was followed by high-grade metamorphism. Finally, the Dalane phase (970-900 Ma) corresponded to gravitational collapse, associated with post-collisional magmatism, and formation of a gneiss dome and core complex (930-920 Ma) with low-pressure/high-temperature metamorphism.

In this context, lithium mineralization occurred within polymetamorphic Paleoproterozoic amphibolite gneiss, gabbroic amphibolite and metadiorite, mainly within the Idefjorden and Telemark terranes. In the latter, the Evje-Iveland pegmatite field, recognized as the largest one (Fig. 3; e.g., Birkeland and Frikstad), comprises over 400 pegmatite bodies. These were dated at ca. 909±14 Ma [START_REF] Scherer | Calibration of the lutetium-hafnium clock[END_REF]Table 5), appear to be unrelated to granites, but are coeval with late regional partial melting and crustal collapse. Among these NYF pegmatites, several indicate a late-magmatic event shown by a REE-depleted replacement zone consisting of "cleavelandite", amazonite, quartz and muscovite, suggesting overprinting of a LCT magma onto pre-existing NYF pegmatite bodies (Černý, 1991a,b). Lepidolite and zinnwaldite are reported from these pegmatites, which are considered as mixed NYF-LCT pegmatites, although the Li enrichment is related to the replacement zones.

3.2

Hard-rock lithium mineralization in European Neoproterozoic to Neogene terranes

3.2.1

The Cadomian orogenic belt (620-540 Ma) In Europe, the Cadomian orogeny is characterized by a continental magmatic arc, which occurred during the Ediacaran along the rim of the West African Craton and resulted in opening of the Rheic Ocean between the Avalonia and Armorica microplates, respectively associated with the Laurentia and Gondwana supercontinents. This took place from Cambrian to Ordovician (Fig. 4; e.g., [START_REF] Linnemann | The Cadomian orogeny and the opening of the Rheic Ocean: The diacrony of geotectonic processes constrained by LA-ICP-MS U-Pb zircon dating (Ossa-Morena and Saxo-Thuringian Zones, Iberian and Bohemian Massifs)[END_REF][START_REF] Nance | A brief history of the Rheic Ocean[END_REF].

A notable relic of this event is the occurrence of discontinuous Cambrian-Early Ordovician Mn-(Fe) rich metasedimentary rocks in Scotland, Wales, the Lake District of England, Belgium and Germany (Fig. 4; [START_REF] Kroner | Two plates -Many subductions zones: The Variscan orogeny reconsidered[END_REF]. Here, Li-bearing minerals such as lithiophorite can occur. Such occurrences are restricted to the Avalonian Shelf, constrained by the Rheic suture in the south, and were formed by weathering of the Cadomian continental magmatic arc at the edge of the peri-Gondwana plate in an extensional regime [START_REF] Romer | Geochemical signature of Ordovician Mn-rich sedimentary rocks on the Avalonian shelf[END_REF]. They were formed during the first stage of the orogeny (ca. 590-570 Ma) and are not stratigraphically correlative, but can be found along the Avalonia Shelf from Nova Scotia through the Government Point Formation of the sedimentary Goldenville Group (Canada; [START_REF] White | Defining the stratigraphy on the Meguma Supergroup in southern Nova Scotia; Where do we go from here?[END_REF] to Poland. [START_REF] Kroner | Two plates -Many subductions zones: The Variscan orogeny reconsidered[END_REF] suggested that coeval and similar deposits may be found in the southern part of the Ossa Morena Zone (Spain).

The Caledonian orogenic belt (475-380 Ma)

The Caledonian orogeny was a series of tectonic events related to the closure of the Iapetus Ocean [START_REF] Mckerrow | The Caledonian orogeny redefined[END_REF], reflecting Ordovician-Silurian oblique interactions between the Laurentian (Scotland), Avalonia (Ireland) and Baltica terranes. The initial Grampian phase (475-460 Ma) consisted, at the north end of the Iapetus Ocean, of collision between the Laurentian continental margin and an intra-ocean island arc complex. This resulted in the emplacement of S-type granites in the NW highlands of Scotland and was followed by oblique subduction under the Laurentian (north), Avalonian (south) and Baltica (east) terranes (Fig. 5A). In the Late Silurian (425 Ma), the Iapetus Ocean was closed and continents collided with the Laurentian Terrane along the Iapetus Suture Zone (Fig. 5A). Widespread calc-alkaline magmatism occurred from ca. 425 to 380 Ma as a post-subduction event [START_REF] Miles | Tectonic controls on post-subduction granite genesis and emplacement: The Late Caledonian suite of Britain and Ireland[END_REF], related to orogen-wide sinistral transtension induced by subsequent episodes of lithospheric extension during the Early Devonian (Brown et al. 2008). In this Caledonian context, LCT pegmatites are known from Scotland and Ireland. In Scotland, the Glenbuchat pegmatite lies in the northern part of the Iapetus Suture Zone, hosted by Dalradian metasedimentary rocks of the Grampian Terrane. It consists of lepidolite and elbaite rich pegmatite (Fig. 5B; [START_REF] Jackson | An occurrence of gem quality elbaite from Glenbuchat, Aberdeenshire, Scotland[END_REF]. The Dalradian Inzie Head gneiss and Grampian granite are associated with the ca. 470 Ma Grampian migmatization [START_REF] Johnson | Melt segregation structures within the Inzie Head gneisses of the northeastern Daldarian[END_REF].

In Ireland, the ca. 412 Ma Leinster LCT pegmatite field (Table 5; [START_REF] Barros | Petrogenesis of the Leinster LCT (Li-Cs-Ta) pegmatite belt in southeast Ireland[END_REF] that includes the spodumene Aclare and Molyisha pegmatites, shows a relatively late time of formation (Fig. 5B). The pegmatite field is hosted by the ca. 417-405 Ma poly-phase Tullow Lowlands pluton [START_REF] Fritschle | Age and origin of late Caledonian granites and Ordovician arc magmatic rocks in Ireland and the Isle of Man[END_REF] along the East Carlow Deformation Zone and includes up to 60 wt.% spodumene [START_REF] Luecke | Lithium pegmatites in the Leinster Granite (southeast Ireland)[END_REF]. Thus, their emplacement may be related to a transtensional regime in this late orogenic process.

The Variscan orogenic belt (400-250 Ma)

The European Variscan orogen extends from southern Iberia to northeastern Bohemia, forming a 3000 km long and 700-800 km wide belt. It results of Late Paleozoic convergence and collision of the Gondwana (south) and Laurasia-Baltica (north) megacontinents along the Variscan Front (Fig. 6), involving several intermediate microcontinents and closures of oceanic domains (e.g., [START_REF] Matte | La chaîne varisque parmi les chaînes paléozoïques péri atlantiques, modèle d'évolution et position des grands blocs continentaux au Permo-Carbonifère[END_REF][START_REF] Matte | Accretionary history and crustal evolution of the Variscan belt in Western Europe[END_REF].

The earliest continental collision started locally in the Early Devonian (385-380 Ma) with migmatization and related anatexis of continental crust, as well as exhumation of Late Silurian rocks along a regional deformation event. In the Middle-Late Devonian (360-350 Ma), arc and back-arc magmatism occurred in the northern Gondwana margins and Central Armorican Domain, attesting of southward subduction and subsequent closure of the Rheic Ocean (Fig. 6; [START_REF] Faure | Paleozoic tectonic evolution of Medio-Europa from the example of the French Massif Central and Massif Armoricain[END_REF]. This event was associated with a variable pressure-temperature metamorphic and deformation event. Late Visean synorogenic extension related to a synorogenic collapse of the inner zones occurred along NW-SE stretching and 333 to 326 Ma migmatization [START_REF] Faure | Paleozoic tectonic evolution of Medio-Europa from the example of the French Massif Central and Massif Armoricain[END_REF]. Finally, post-orogenic collapse took place around 300 Ma. It was coeval with N-S extension, development of intramontane coal basins and ca. 306 Ma local migmatization [START_REF] Faure | Paleozoic tectonic evolution of Medio-Europa from the example of the French Massif Central and Massif Armoricain[END_REF]. These events appear to have been diachronous throughout the Variscan orogeny.

Considerable amounts of granitic intrusions and several districts of RMG/greisen and LCT pegmatite deposits illustrate the Variscan orogeny. At the scale of the belt, such deposit types are relatively late in the orogeny, coeval with crustal extension together with regional partial melting and melt emplacement. Thus, in the Bohemian Massif, the easternmost part of the European Variscan belt (Fig. 6), greisen and RMG are common in the Saxothuringian and Teplá-Barrandian zones consisting of Neoproterozoic basement (e.g., [START_REF] Matte | Accretionary history and crustal evolution of the Variscan belt in Western Europe[END_REF]. The Moldanubian area contains mainly LCT pegmatites (e.g., [START_REF] Cháb | Outline of the geology of the Bohemian Massif: The basement rocks and their Carboniferous and Permian cover[END_REF][START_REF] Ackerman | Temporal evolution of mineralization events in the Bohemian Massif inferred from the Re-Os geochronology of molybdenite[END_REF], which appear to be spatially related to migmatitic domes and shear zones. According to [START_REF] Melleton | How are the emplacement of rareelement pegmatites, regional metamorphism and magmatism interrelated in the Moldanubian Domain of the Variscan Bohemian Massif Czech Republic[END_REF], two ages of pegmatite emplacement were identified, including an independent orogenic stage in the Bohemian Massif with LP-HT regional metamorphism related to significant reheating and anatexis; they note that the emplacement of LCT pegmatite here is the oldest known magmatic event of the Variscan orogeny.

In France, the northwestern part of the Massif Central is a favorable area for rare-element magmatic bodies [START_REF] Marignac | Ore deposits of the French Massif Central: Insight into the metallogenesis of the Variscan collision belt[END_REF]. This province can be divided into three distinct deposit types (Table 5): 1) rare-metal granite such as the 317±6 Ma Beauvoir and the 314±4 Ma Montebras [START_REF]Les coupoles granitiques de Montebras et d'Echassières (Massif Central français) et la genèse de leurs minéralisations en étain, lithium, tungstène et béryllium[END_REF][START_REF] Cuney | The Beauvoir topaz-lepidolite albite granite (Massif Central, France): The disseminated magmatic Sn-Li-Ta-Nb-Be mineralization[END_REF][START_REF] Cuney | The timing of W-Sn -rare metals mineral deposit formation in the Western Variscan chain in their orogenic setting: the case of the Limousin area (Massif Central, France); In The Timing of Major Ore Deposits in an Evolving[END_REF]; 2) rare-metal rhyolite represented by the 313±3 Ma Richemont rhyolite [START_REF] Raimbault | The Richemont rhyolitic dyke, Massif Central, France: A subvolcanic equivalent of rare-metal granite[END_REF]; and 3) LCT pegmatites such as the Mont d'Ambazac rare-element pegmatite field (e.g., [START_REF] Raimbault | Geochemical evidence for a multistage magmatic genesis of Ta-Sn-Li mineralization in the granite de Beauvoir, French Massif Central[END_REF]Deveaud et al., 2013). The latter includes the 309±5 Ma lepidolite-subtype LCT Chédeville pegmatite, which postdates the 324±4 Ma host granite [START_REF] Hollinger | Age carbonifère de l'unité de Brame du complexe granitique peralumineux de Saint-Sylvestre (NO du Massif Central) défini par les données isotopiques U-Pb sur zircon et monazite[END_REF]) and appears to be sub-synchronous with local partial melting (315±4 and 316±4 Ma; [START_REF] Gébelin | Syntectonic crustal melting and high-grade metamorphism in a transpressional regime, Variscan Massif Central, France[END_REF] and with shearing (La Marche shear zone: 316±5 to 312±2 Ma, [START_REF] Gébelin | Transpressional tectonics and Carboniferous magmatism in the Limousin[END_REF][START_REF] Gébelin | Syntectonic crustal melting and high-grade metamorphism in a transpressional regime, Variscan Massif Central, France[END_REF]. This east-west La Marche fault system, located in the northern part of the Limousin, appears to have been a key-control on magmatic activity [START_REF] Cuney | The timing of W-Sn -rare metals mineral deposit formation in the Western Variscan chain in their orogenic setting: the case of the Limousin area (Massif Central, France); In The Timing of Major Ore Deposits in an Evolving[END_REF].

The Galicia-Trás-os-Montes Zone (GTOMZ) and the Central Iberian Zone (CIZ) in the Iberian Variscan belt host widespread LCT pegmatite fields. At least five main mineralized pegmatite fields are recognized in the former from north to south: Forcarei-Lalín, Serra de Arga, Barroso-Alvão, La Fregeneda-Almendra and Gonçalo-Guarda. In the CIZ, the 326±3 Ma Argemela granite is the only RMG known from Iberia [START_REF] Charoy | The Argemela granite-porphyry (Central Portugal): the subvolcanic expression of a high-fluorine, rare-element pegmatite magma[END_REF]1996). The average age of intrusion of LCT pegmatites in the GTOMZ is 310±5 Ma, whereas in the CIZ and in the southern GTOMZ the ages are younger: 301±3 Ma [START_REF] Melleton | U-Pb dating of columbite-tantalite from Variscan rare-elements granites and pegmatites[END_REF], 295.1±4.1 Ma and 296.4±4.1 Ma [START_REF] Roda-Robles | Petrogenetic links between granites and pegmatites in the Fregeneda-Almendra area (Salamanca, Spain and Guarda, Portugal): New insights from 40Ar/39Ar dating in micas[END_REF][START_REF] Vieira | Aplitopegmatitos com elementos raros da região entre Almendra (V. N. de Foz-Côa) e Barca d'Alba (Figueira de Castelo Rodrigo)[END_REF]. Moreover, late quartz-montebrasite hydrothermal veins are reported from several areas in the CIZ (e.g., [START_REF] Roda-Robles | Geology and mineralogy of Li-mineralization in the Central Iberian Zone (Spain and Portugal)[END_REF].

Finally, in the Austroalpine unit of the Eastern Alps, Permian LCT spodumene-bearing pegmatites are known (e.g., [START_REF] Thöni | Permo-Triassic pegmatites in the eo-Alpine eclogite facies Koralpe complex, Austria: Age and magma source constraints from mineral, chemical, Rb-Sr and Sm-Nd isotope data[END_REF][START_REF] Ilickovic | Spodumene bearing pegmatites in the Austroalpine unit (Eastern Alps): Distribution and new geochronologiocal data[END_REF]. These pegmatites appear to be coeval with lithospheric extension, causing crustal basaltic underplating, HT and LP metamorphism, as well as intense magmatic activity [START_REF] Schuster | The Permian metamorphic event in the Alps[END_REF].

The Mediterranean and circum-Mediterranean orogens (Mesozoic-2.5 Ma)

Several styles of lithium mineralization are contemporaneous with the circum-Mediterranean and Mediterranean Tethys mountain belts, such as the Carpathians Mountains or the Egean Domain, which resulted from oceanic closure and collision of the European continental foreland (Bohemian Massif) with the African promontory of the Adriatic microplate (Fig. 7). Rifting of the Alpine Tethys and its subsequent subduction underneath the Adriatic margin, followed by continent-continent collision, promoted widespread magmatic activity through time, as well as the development of related orogens such as the Carpathians Mountains. The initial continental rifting of the Alpine Tethys and its related magmatism occurred from the Middle to Late Triassic in the eastern part of the Mediterranean domain [START_REF] Bertotti | Crustal thermal regime prior to, during, and after rifting: a geochronological and modelling study of the Mesozoic South Alpine rifted margin[END_REF][START_REF] Schmid | The Alpine-Carpathian-Dinaridic orogenic system: Correlation and evolution of tectonic units[END_REF]). In the central Alpine-Carpathian-Dinaridic orogenic system, ca. 242 Ma Li-phosphate pegmatites occur in the Brissago area (Switzerland; [START_REF] Vignola | Phosphate assemblages from the Brissago granitic pegmatite, western Southern Alps, Switzerland[END_REF]; these authors suggested that the pegmatites formed from partial melting of the Early Permian Ivrea gabbro.

This tectono-magmatic event was followed by development of the Adriatic passive margin in the Middle Jurassic [START_REF] Bertotti | Crustal thermal regime prior to, during, and after rifting: a geochronological and modelling study of the Mesozoic South Alpine rifted margin[END_REF][START_REF] Schmid | The Alpine-Carpathian-Dinaridic orogenic system: Correlation and evolution of tectonic units[END_REF] in an extensional tectonic regime, and later by the subduction of the Tethys oceanic lithosphere beneath the Adriatic margin from Cretaceous to Late Paleogene. This crustal shortening led to the final consumption of the Neotethys Ocean associated with widespread calk-alkaline magmatism in the Carpathian arc (Fig. 7; [START_REF] Schmid | The Alpine-Carpathian-Dinaridic orogenic system: Correlation and evolution of tectonic units[END_REF] and formation of the Apennines in Italy. Meanwhile, Jurassic to Cretaceous bauxite deposits with lithiophorite are reported from Hungary and Greece (Fig. 7), suggesting a tropical climate during this period.

In the external domain of the Dauphinois zone (French Alps), an Eocene greenschist metamorphic event led to the formation of cookeite-bearing formations and -tension gashes within Aalenian black shales (Fig. 7). According to [START_REF] Jullien | Occurrences de cookéite et de pyrophyllite dans les schistes du Dauphinois (Isèe, France) -Conséquences sur la répartition du métamorphisme dans les zones extemes alpines[END_REF], the Li was sourced from the metasediments that themselves resulted from erosion of the continental crust.

Within the Central Alps (i.e., Penninic Zone), a kilometer-scale east-west extensional area occurs with several Oligocene-Miocene LCT pegmatites in the Vigezzo, Bodengo and Codera areas. They are Tertiary (Fig. 7; 30 to 20 Ma, [START_REF] Guastoni | Tertiary pegmatite dikes of the Central Alps[END_REF][START_REF] Romer | Alpine and pre-Alpine magmatism in the root-zone of the western Central Alps[END_REF] and show a beryl-phosphate affinity with elbaite and columbite as potential accessory minerals [START_REF] Guastoni | Tertiary pegmatite dikes of the Central Alps[END_REF][START_REF] Guastoni | Monazite-(Ce) and xenotime-(Y) from an LCT, NYF tertiary pegmatite field: evidence from a regional study in the Central Alps (Italy and Switzerland)[END_REF].

Finally, extensional collapse and back-arc extension promoted development of the Miocene Pannonian and the Jadar basins within the Alpine-Carpathian-Dinarides domain along several late Oligocene-Miocene detachment zones [START_REF] Jolivet | From mantle to crust: Stretching the Mediterranean[END_REF][START_REF] Menant | 3D subduction dynamics: A first-order parameter of the transition from copper-to gold-rich deposits in the eastern Mediterranean region[END_REF][START_REF] Stojadinovic | Structure and provenance of Late Cretaceous-Miocene sediments located near the NE Dinarides margin: Interferences from kinematics of orogenic building and subsequent extensional collapse[END_REF] and in response to rapid slab roll-back [START_REF] Simić | Evolution of Neogene Intramontane basins in Serbia[END_REF][START_REF] Stojadinovic | Structure and provenance of Late Cretaceous-Miocene sediments located near the NE Dinarides margin: Interferences from kinematics of orogenic building and subsequent extensional collapse[END_REF]. Basin formation was accompanied by calc-alkaline magmatism with a paroxysm of silicic volcanism during the early and middle Miocene [START_REF] Kovács | Paleogene-Early Miocene igneous rocks and geodynamics of the Alpine-Carpathian-Pannonian-Dinaric region: An integrated approach[END_REF]. Rapid exhumation of metamorphic rocks caused episodic migmatization as well as related magmatism (Bergell intrusion; Beltrando et al., 2010).

Within the northern part of the Apennines, the ca. 6.7-6.9 Ma [START_REF] Ferrara | Radiometric geochronology in Tuscany: Results and problems[END_REF] LCT pegmatites from Elba Island are famous for their gem-quality elbaites.

Interpretation and discussion

Considering all lithium occurrences in Europe, one of the first observations regarding their distribution is their apparent clustering (Figs. 3,4,5,6,7). This clustering defines pegmatite and/or RMG fields with similar ages of emplacement, suggesting a relatively coeval magmatic activity related to common endogenous processes. Furthermore, the Li-rich sedimentary basins such as Jadar reflect late sedimentary/hydrothermal Li re-concentration through exogenous processes.Endogenous processes related to lithium mineralization We have identified several Li-magmatic events through time as illustrated by RMG, greisen and LCT pegmatites (Table 5;Figs. 3,4,5,6,7,[START_REF] Launay | Dynamic permeability related to greisenization reactions in Sn-W ore deposits: Quantitative petrophysical and experimental evidence[END_REF], ranging from Paleoproterozoic to Miocene. These events occurred during times of collisional orogeny, including the Svecofennian (2.1-1.8 Ga; Fig. 3), Sveconorwegian (1140-850 Ma; Fig. 3), Caledonian (490-390 Ma; Fig. 5), Variscan (400-250 Ma; Fig. 6) and Mediterranean (Mesozoic-2.5 Ma; Fig. 7) orogenies. These events were mainly related to supercontinent formation, as observed elsewhere by [START_REF] Bradley | Secular trends in the geologic record and the supercontinent cycle[END_REF]. Accordingly, in the Svecofennian orogen, LCT pegmatite ages are 1.8-1.79 Ga This suggests relatively late emplacement in the orogenic cycle that postdated arc accretion and the first regional metamorphism, and might be related to crustal thickening as well as to a late amphibolite-facies metamorphic event.

During the Sveconorwegian orogen, emplacement of Li-rich pegmatites (910-906 Ma) appears coeval with the late Dalane phase (970-900 Ma), corresponding to gravitational collapse and postcollisional magmatism, as well as the formation of a gneiss dome and core complex related to low pressure/high temperature metamorphism. The Scottish and ca. 412 Ma LCT pegmatites from Ireland, which are part of the Caledonian orogenic belt, appear coeval with crustal thickening and postsubduction magmatism.

In the Variscan belt, RMG (Beauvoir, Montebras and Richemon, France; Argemela, Portugal; St Austell, UK), greisen (Cligga Head, Tregonning-Godolphin, Meldon, UK; Dlha Dolina, Slovakia; Montebras, France; Krasno-Konik, Krupka, Czech Republic) and various LCT pegmatites (Table 5, Fig. 6) are widely distributed (Fig. 8). Their ages suggest mostly emplacement during the Late Carboniferous (Table 5) reflecting highly fractionated magmatic events throughout the European core related to a post-collisional stage ending the Variscan orogeny sensu stricto (Fig. 6,Table 5; e.g., [START_REF] Bonin | Orogenic to non-orogenic magmatic events: Overview of the Late Variscan magmatic evolution of the Alpine Belt[END_REF]Chen et al., 1993;[START_REF] Cuney | The timing of W-Sn -rare metals mineral deposit formation in the Western Variscan chain in their orogenic setting: the case of the Limousin area (Massif Central, France); In The Timing of Major Ore Deposits in an Evolving[END_REF][START_REF] Melleton | How are the emplacement of rareelement pegmatites, regional metamorphism and magmatism interrelated in the Moldanubian Domain of the Variscan Bohemian Massif Czech Republic[END_REF][START_REF] Neace | Zircon La-ICPMS geochronology of the Cornubian Batholith[END_REF]. Moreover, from the internal to the external orogenic domains Li-magmatism appears to be diachronous, indicating southward prograding Li-rich magmatic activity traversing the entire belt. In the internal zones (France, Germany, Czech Republic and NW Iberia) RMG, greisen and LCT pegmatites were mostly emplaced between 320 and 307 Ma corresponding to the Bavarian phase (330-315 Ma;[START_REF] Finger | Resolving the Variscan evolution of the Moldanubian sector of the Bohemian Massif: The significance of the Bavarian and the Moravo-Moldanubian tectonometamorphic phases[END_REF] in the Bohemian Massif and to synorogenic collapse and NW-NE stretching in the French Massif Central (320-310 Ma). In the external zones (UK, parts of Spain and Portugal), similar deposits tended to be emplaced around 305 and 301 Ma (excluding the ca. 326 Ma Argemela granite) suggesting late-orogenic magmatism [START_REF] Melleton | Rare-elements (Li-Be-Ta-Sn-Nb) magmatism in the European Variscan belt, a review[END_REF]. Finally, deposits belonging to the Gemeric unit in the Western Carpathians of Slovakia, as well as the Austroalpine pegmatites of the Eastern Alps that form the extreme margins of the belt, indicate Permian ages coeval with regional partial melting (Finger et al., 2003[START_REF] Petrik | Alpine oxidation of lithium micas in Permian S-type granites (Gemeric unit, Western Carpathians, Slovakia)[END_REF][START_REF] Ilickovic | Spodumene bearing pegmatites in the Austroalpine unit (Eastern Alps): Distribution and new geochronologiocal data[END_REF].

Thus, it appears that the emplacement of RMG, greisen and LCT pegmatites was relatively late in the orogenic cycle and may have been coeval with continent-continent collision, commonly postdating arc accretion. It could also be related to crustal thickening [START_REF] Alviola | Svecofennian rare-element granitic pegmatites of the Ostrobothnia region, western Finland: their metamorphic environment and time of intrusion[END_REF], a favorable setting for crustal peraluminous melt [START_REF] Cuney | The Beauvoir topaz-lepidolite albite granite (Massif Central, France): The disseminated magmatic Sn-Li-Ta-Nb-Be mineralization[END_REF][START_REF] Tomljenovic | Strukturne Znacajke Medvednice i Samoborskoj gorja[END_REF] through wall-rock assimilation, the unmixing of restite, and/or internal fluid circulation related to convective fractionation [START_REF] Lehmann | Granite-related rare-metal mineralization: a general geochemical framework[END_REF][START_REF] Martin | The patterns of enrichment in felsic pegmatites ultimately depend on tectonic setting[END_REF].

Importantly, it also appears that the reported greisen were developed from RMG, suggesting that most of the greisen associated with fractionated S-type peraluminous granite may not show significant Li contents. The formation model involves early exsolution of an F-CO 2 -H 2 O-rich aqueous phase from the granitic magma, along with fluid/rock interactions leading to dissolution/precipitation and reconcentration of incompatible elements, such as Li, F, Sn, W, etc., within the greisen [START_REF] Heinrich | The chemistry of hydrothermal tin (-tungsten) ore deposition[END_REF]. Here: 1) miarolitic cavities are common and reflect volatile saturation; and 2) a decrease in rock volume and increase of porosity are reported. In the 321.5±3 Ma Cinovec deposit, dissolution of the protolithionite-formed during magmatic intrusion-and precipitation of zinnwaldite during greisenization have led led to remobilization of Li into its final host mineral (Johan and Johan, 2005).

4.2

Exogenous processes related to lithium occurrences Several Li-occurrences in Europe reflect a concentration of lithium in sedimentary rocks through various exogenous processes, such as hydrothermal circulation and/or erosion and transport. Thus, distinct occurrence types can be distinguished.

Jadar deposit type

The Jadar deposit type is exclusively Neogene (Oligocene to Pliocene), based on available data. The existence of several other isolated intramontane lacustrine evaporite basins is suggested in Serbia (Fig. 8) as well as in Bosnia, such as the Valjevo-Mionica or Lopare basins from where jadarite was reported. Interestingly, the subsurface of these basins includes LCT pegmatite and Cretaceous to Miocene granitic intrusions, suggesting local lithium enrichment in the basement [START_REF] Stojadinovic | Structure and provenance of Late Cretaceous-Miocene sediments located near the NE Dinarides margin: Interferences from kinematics of orogenic building and subsequent extensional collapse[END_REF]. These basins were formed during the late stage of the Dinadiric orogeny (Fig. 7), coeval with the extensional collapse and back-arc extension due to Carpathian slab retreat [START_REF] Simić | Evolution of Neogene Intramontane basins in Serbia[END_REF].

Jadarite precipitation is poorly constrained. Some authors suggested that interaction between clastic sedimentary rocks and the surrounding brine-possibly involving hydrothermal devitrification and hydration of andesitic-dacitic pyroclastic material or alteration of clay minerals-may contribute to its precipitation [START_REF] Stanley | Jadarite, LiNaSiB3O7(OH), a new mineral species from the Jadar Basin, Serbia[END_REF][START_REF] Stojadinovic | Structure and provenance of Late Cretaceous-Miocene sediments located near the NE Dinarides margin: Interferences from kinematics of orogenic building and subsequent extensional collapse[END_REF].

Mn-(Fe) deposits

Two distinct periods of Mn-(Fe) precipitation in Europe are described here. A first group of deposits in Scotland, Wales (e.g., Drosgol Mine), England (Clews Gill), Belgium (Ottré, Beez) and Germany (Harz) is Cambrian to Early Ordovician in age (Fig. 8; [START_REF] Waldron | Cambrian successions of the Meguma Terrane, Nova Scotia and Harlech Dome, North Wales: dispersed fragments of a peri-Gondwana basin?[END_REF][START_REF] Romer | Geochemical signature of Ordovician Mn-rich sedimentary rocks on the Avalonian shelf[END_REF], representing a notable relic of the Cadomian orogeny (650-550 Ma; Fig. 4). They are exclusively located in the Avalonian plate, constrained by the Rheic Suture, and are formed from weathering of the Cadomian magmatic arc of the Gondwana plate, as suggested by Nd and Sr isotopes [START_REF] Romer | Geochemical signature of Ordovician Mn-rich sedimentary rocks on the Avalonian shelf[END_REF]. Interestingly, in Europe, the Cadomian orogeny was subsequently reworked during the Caledonian and Variscan orogenies [START_REF] Zelazniewicz | Variscides in the Sudetes and the reworked Cadomian orogeny: evidence from the GB-2A seismic reflection profiling in southerwestern Poland[END_REF][START_REF] Melleton | How are the emplacement of rareelement pegmatites, regional metamorphism and magmatism interrelated in the Moldanubian Domain of the Variscan Bohemian Massif Czech Republic[END_REF].

The second group is mainly found in Hungary, where the Eplény and Urkut Mn deposits are Jurassic in age [START_REF] Polgari | Manganese-impregnated wood from a Toarcian manganese ore deposit, Eplény mine, Bakony Mts., Transdanubia, Hungary[END_REF]Figs. 7, 8). These deposits are associated with marine sedimentary rocks mainly composed of bioclastic limestone and black shale.

The Li-bearing mineral lithiophorite, as most Mn-and Fe-oxides, was formed from secondary fluid circulation in the host rock [START_REF] Nicholson | The Dalradian rocks of the Lecht, NE Scotland: Stratigraphy, faulting, geochemistry and mineralization[END_REF]. [START_REF] Romer | Geochemical signature of Ordovician Mn-rich sedimentary rocks on the Avalonian shelf[END_REF] suggested that the lithium component derived from chemical weathering of continental crust and was originally concentrated in siliciclastic or carbonate rocks. Thus, late hydrothermal fluid circulation may have remobilized-and still remobilizes-the Li 2 O content via dissolution/precipitation processes , thus helping the precipitation of Li-bearing oxides under oxidizing conditions. Moreover, several authors pointed out their distribution along regional faults that are favorable sites for fluid circulation, such as the Candwr Fault in Wales [START_REF] Cotterell | Supergene manganese mineralization associated with the Camdwr fault in the Central Wales orefield[END_REF] and the Red Gill Fault in the UK [START_REF] Clark | The geology and pretrology of the Ennerdale granophyre. Its metamorphic aureole and associated mineralization[END_REF].

Bauxite deposits

Li-bearing minerals in bauxite deposits are Cretaceous in Hungary [START_REF] D'argenio | Cretaceous bauxites in the tectonic framework of the Mediterranean[END_REF] and Jurassic to Cretaceous in Greece where they are located along the northern shores of the Mediterranean Sea [START_REF] Bardossy | Karst bauxites, Bauxite deposits on carbonate rocks[END_REF].

In Hungary, these deposits are stratiform where bedrock is a non-uniform karst carbonate rock, in which the bauxite horizons are relatively large. The Halimba mining district is one of the largest, with bauxite thickness varying from 1 to 40 m. Here, the Li-bearing mineral lithiophorite originated from secondary fluid circulation through the host rock [START_REF] Bardossy | Karst bauxites, Bauxite deposits on carbonate rocks[END_REF] forming Mn-rich layers in epi-and supergene crusts. Cookeite is also reported from these deposits [START_REF] Bardossy | Karst bauxites, Bauxite deposits on carbonate rocks[END_REF].

4.3

Discussion of rare-metal magma formation There are currently two distinct models of rare-metal magma formation. The first one involves the escape of late-stage melts ending the crystallization of huge highly fractionated felsic magma chambers (e.g., [START_REF] Jahns | Experimental studies of pegmatites gneiss: A model for the derivation and crystallization of granitic pegmatities[END_REF][START_REF] London | The application of experimental petrology to the genesis and crystallization of granitic pegmatites[END_REF]. One of the major arguments for this model is the regional zoning of pegmatite bodies in the margins of supposed parent granites (e.g., [START_REF] Cameron | Internal structure of granitic pegmatites[END_REF][START_REF] Černý | The classification of granitic pegmatites revisited[END_REF]. An example is the Fregeneda-Almendra pegmatite field where crystalfractionation modelling and geochronology support a magmatic origin [START_REF] Vieira | Chemical variation and significance of micas from the Fregeneda-Almendra pegmatitic field (Central-Iberian Zone, Spain and Portugal)[END_REF][START_REF] Roda-Robles | Geology and mineralogy of Li-mineralization in the Central Iberian Zone (Spain and Portugal)[END_REF]. Moreover, the widespread presence of pegmatites and RMG in granites (e.g., [START_REF] London | The application of experimental petrology to the genesis and crystallization of granitic pegmatites[END_REF][START_REF] Černý | The classification of granitic pegmatites revisited[END_REF] suggests a granite-related origin (e.g. [START_REF] Roda-Robles | Geology and mineralogy of Li-mineralization in the Central Iberian Zone (Spain and Portugal)[END_REF].

However, some aspects disagree with this model, suggesting a second model that involves lowgrade partial melting of crustal sequences (e.g., [START_REF] Norton | Lithium, cesium, and rubidium-the rare alkali metals (United States Mineral Resources)[END_REF][START_REF] Zasedatelev | Quantitative model of metamorphic generation of rare-metal pegmatite with lithium mineralization[END_REF][START_REF] Stewart | Petrogenesis of lithium-rich pegmatites[END_REF][START_REF] Melleton | U-Pb dating of columbite-tantalite from Variscan rare-elements granites and pegmatites[END_REF][START_REF] Müller | The chemistry of quartz in granitic pegmatites of Southern Norway: Petrogenetic and economic implications[END_REF][START_REF] Bongiolo | Origin of pegmatites and fluids at Ponta Negra (RJ, Brazil) during late-to post-collisional stages of the Gondwana Assembly[END_REF]. In southern Ireland, geochemical evidence points to the absence of a relationship between the LCT-spodumene Aclare pegmatite field and the surrounding Tullow Lowlands and Blackstairs plutons that are part of the Leinster Granite. This absence concerns their capacity of generating a residual pegmatite melt [START_REF] Barros | The origin of spodumene pegmatites associated with the Leinster granite in southeast Ireland[END_REF]. These authors suggested a separate partial-melting event for both units, although the intrusion of the granitic unit may have triggered anatexis of the surrounding sedimentary rocks.

In the French Massif Central, the Monts d'Ambazac pegmatite field has δ 7 Li mica values that are consistent with a crustal metasedimentary source. It is also coeval with evidence of a partial-melting event, excluding the influence of magmatic fractionation from the nearby St Sylvestre granite in the formation of pegmatites. It also demonstrates that strong Li enrichment in pegmatite is not related to a fractionation process [START_REF] Deveaud | The genesis of LCT-type granitic pegmatites, as illustrated by lithium isotopes in micas[END_REF]. In the Bohemian Massif and in Austria, LCT pegmatite fields are also supposed to be formed by partial melting processes [START_REF] Melleton | How are the emplacement of rareelement pegmatites, regional metamorphism and magmatism interrelated in the Moldanubian Domain of the Variscan Bohemian Massif Czech Republic[END_REF].

Thus, a model of partial melting during anatexis of sedimentary rock (evaporites, cookeite-bearing metapelite, Li-rich metasedimentary rock, or Li-rich Ordovician orthogneiss, etc.) may be applied (Fig. 10), involving coeval emplacement for S-type granite (e.g., [START_REF] Kontak | A petrological, geochemical, isotopic and fluid inclusion study of 370 Ma pegmatite-aplite sheets, Peggys Cove, Nova Scotia, Canada[END_REF] and nearby LCT pegmatite, but not promoting a "parental" relationship. Moreover, micas, garnet and staurolite, which are widespread in metasedimentary rock, are seen as a potential source for lithophile elements such as Li [START_REF] London | Granitic pegmatites -An assessment of current concepts and directions for the future[END_REF][START_REF] London | Ore-forming processes within granitic pegmatites[END_REF]. For instance, in the Brissago-Valle di Ponte area (Switzerland-Italy), poorly fractionated LCT phosphate pegmatites are suspected to be derived from local partial melting of kinzigites during high-temperature metamorphism [START_REF] Vignola | Phosphate assemblages from the Brissago granitic pegmatite, western Southern Alps, Switzerland[END_REF]. At the European scale, various Li-bearing minerals are reported from pegmatites, including Li-micas, lepidolite, spodumene and petalite, involving variations in the fluxing content (F, B and P) of the magmatic fluid (Roda-Robles et al., 2010), as well as varying P/T conditions (e.g., spodumene versus petalite; [START_REF] London | Magmatic -hydrothermal transition in the Tanco rare-element pegmatite: Evidence from fluid inclusions and phase-equilibrium experiments[END_REF][START_REF] London | Internal differentiation of rare element pegmatites; A synthesis of recent research[END_REF]. These variations are also seen in the Scandinavian orogenies, where zonation of Li-bearing minerals is highlighted: 1) the Svecofennian LCT pegmatites are associated with Li-silicate and Liphosphate minerals; but 2) the Sveconorwegian LCT pegmatites show a Li-phyllosilicate affinity.

4.4

From source to sink As suggested above, several parameters may control the lithium mineralization locations in Europe. The observed clustering of endogenous lithium deposits such as LCT pegmatites, RMG and/or greisen may involve a crustal anomaly (>20 ppm; [START_REF] Rudnick | Composition of the continental crust[END_REF], or a Li "pre-concentration" related to paleoenvironmental sedimentation conditions (e.g., type of basin, host rock, climate) and/or postdeposition processes (weathering, basin-fluid circulation in the crust), more generally preserved along a paleo passive-margin (Fig. 9; [START_REF] Romer | Phanerozoic tin and tungsten mineralization -Tectonic controls on the distribution of enriched protoliths and heat sources for crustal melting[END_REF].

In any case, this involves the existence of a primary Li-source that can be of magmatic origin, such as erosional material from a continental magmatic arc and related Mn(-Fe) deposits and lithiophorite occurrences. Another possibility is a sedimentary origin, such as the Schist-Metagreywacke Complex in the Galicia-Trás-Os-Montes Zone [START_REF] Roda-Robles | Geology and mineralogy of Li-mineralization in the Central Iberian Zone (Spain and Portugal)[END_REF], or the Pohjanmaa schist belt in Finland and related LCT pegmatites [START_REF] Eilu | Metallogenic areas in Finland[END_REF]. In that respect, significant lithospheric thickening may be favorable for concentrating Li in a specific location [START_REF] Eilu | Metallogenic areas in Finland[END_REF]. The occurrence of several types of Li mineralization in the French Massif Central (Fig. 6; LCT pegmatite, greisen, RMG, Li-bearing tosudite) forming clusters may suggest a possible common Li-source [START_REF] Cuney | Uranium , rare metals, and granulite-facies metamorphism[END_REF]. Moreover, a recent isotopic δ 7 Li study of pegmatites [START_REF] Deveaud | Caractérisation de la mise en place des champs de pegmatites à éléments rares de type LCT -Exemples représentatifs de la chaine Varisque[END_REF][START_REF] Deveaud | The genesis of LCT-type granitic pegmatites, as illustrated by lithium isotopes in micas[END_REF], suggested that beryl-columbite and lepidolite-petalite LCT pegmatites from the Monts d'Ambazac show a distinct crustal contribution, indicating that Li-rich sources may contribute to "secondary" lithium deposits if suitable processes are involved.

The timing of fluid circulation appears to be another important feature for Li-concentration, whether related to a regional or to a local extensional regime in an orogenic cycle (Figs. 9, 10; e.g., [START_REF] Eilu | Metallogenic areas in Finland[END_REF][START_REF] Jolivet | From mantle to crust: Stretching the Mediterranean[END_REF][START_REF] Melleton | Rare-elements (Li-Be-Ta-Sn-Nb) magmatism in the European Variscan belt, a review[END_REF][START_REF] Stojadinovic | Structure and provenance of Late Cretaceous-Miocene sediments located near the NE Dinarides margin: Interferences from kinematics of orogenic building and subsequent extensional collapse[END_REF][START_REF] Menant | 3D subduction dynamics: A first-order parameter of the transition from copper-to gold-rich deposits in the eastern Mediterranean region[END_REF]. Sedimentary/hydrothermal lithium deposits are thus mainly related to regional extension (rifting or back-arc extension; [START_REF] Kroner | Two plates -Many subductions zones: The Variscan orogeny reconsidered[END_REF][START_REF] Simić | Evolution of Neogene Intramontane basins in Serbia[END_REF][START_REF] Stojadinovic | Structure and provenance of Late Cretaceous-Miocene sediments located near the NE Dinarides margin: Interferences from kinematics of orogenic building and subsequent extensional collapse[END_REF], whereas magmatic-related lithium deposits are associated with local decompression and/or transtension strike-slip deformation in late continent-continent orogenic cycles, leading to the formation of a volatile-rich melt (Fig. 10). According to [START_REF] Kontak | A petrological, geochemical, isotopic and fluid inclusion study of 370 Ma pegmatite-aplite sheets, Peggys Cove, Nova Scotia, Canada[END_REF], this melt may cause over-pressuring and/or hydro-fracturing, resulting in the formation of dilatant zones and related fracture sets. Remarkably, sedimentary rocks enriched in Li during an extensional regime (e.g., Jadar Basin) may be a favorable Li source during a subsequent magmatic event. Unfortunately, a lack of data makes it impossible to confirm this hypothesis.

Finally, the distribution of Li-occurrences is strongly influenced by the location and geometry of fracture sets (Figs. 9, 10; Deveaud et al., 2012[START_REF] Deveaud | Caractérisation de la mise en place des champs de pegmatites à éléments rares de type LCT -Exemples représentatifs de la chaine Varisque[END_REF][START_REF] Silva | Chapter 3 -Spatial geostatistical analysis applied to the Barroso-Alvão rare-elements pegmatite field (Northern Portugal)[END_REF]. High permeability fractured zones seem to act as favorable channels for: 1) The emplacement of LCT pegmatite or RMG from evolved magma; or 2) Hydrothermal fluid circulation through sedimentary successions (Jadar Basin, lithiophorite occurrences in Aalenian black shales) leading to secondary Li-bearing mineral (lithiophorite, cookeite) precipitation. A recent geostatistical study showed that most pegmatites occur less than 500 m from a fault system (Deveaud et al, 2013).

4.5

Grade assessment of and tonnage estimation 4.5.1 Data quality When regarding the available dataset, several problems are obvious. The differences in knowledge and definition of mineral resources and reserves vary between historical data (St Austell, Beauvoir), JORC (Jadar project) and NI43-101 (Alberta I project). Historical data estimates predate the CRIRSCO system (before 1995; www.crirsco.com). They are based on drilling campaigns managed by geological surveys and related subsidiaries. Such data may lead to under-or over-estimates. Figure 11 shows that projects and occurrences are distributed homogeneously despite their reference system (historical data in italics versus CRIRSCO system in bold). Note that mineral resources from the St Austell deposits appear to be strongly anomalous from the main population (Fig. 11,Table 4); they are unrealistic for environmental and societal reasons, and probably not economically viable regarding ore grades. For these reasons, the St Austell data are not used in the following sections. The JORC system, however, may exclude some commercially sensitive information, such as mineral reserves if mineral resources (Table 4), which is not allowed with the NI43-101 report. However, these points do not affect the mineral resources comparison on which our estimates are based.

As mentioned above, thirsteen projects in England (Meldon), Ireland (Aclare), France (Beauvoir, Montebras), Germany (Altenberg) and Ukraine were evaluated before setting up a "reporting system", as such mineral resource and -reserve estimates refer to historical evaluations. These data represent only 5% of the entire dataset (Table 4). Fifteen projects were defined in the Australian JORC system (e.g., Wolfsberg, Austria); one project (Zinnwald, Germany) in the European PERC; one in the Canadian NI43-101 system (e.g., Alberta I project which comprises Presqueria deposit, Spain) and one project is defined in the United Nation Framework Classification (UNFC; Alijo deposit).

However, we think that, despite the apparent discrepancies between reference systems, our dataset is a good starting point for estimating the European Li hard-rock potential (Figs. 11,12).

Moreover, Li-bearing minerals in lithiophorite and Li-chlorite occurrences in sedimentary deposits-bauxite, Mn-(Fe), MVT and Li-bearing clay deposits-were not systematically described, as Li was not of first interest at the time. This was the case in Spain, France and Turkey, and may hide significant local Li grades, as in China [START_REF] Wang | Discovery and preliminary study of the high tungsten and lithium contents in the Dazhuyuan bauxite deposit, Guizhou, China[END_REF] and USA [START_REF] Tourtelot | Lithium, a preliminary survey of its mineral occurrence in flint clay and related rock types in the United States[END_REF]. Available data from bauxite deposits in China show that the average Li grade is very low (2045 ppm Li 2 O; [START_REF] Wang | Discovery and preliminary study of the high tungsten and lithium contents in the Dazhuyuan bauxite deposit, Guizhou, China[END_REF]. The same is true for Li-bearing shales in the Dauphinois area, France, where the average Li content is 949.34 ppm Li 2 O [START_REF] Henry | Evolution of synmetamorphic veins and their wallrocks through a Western Alps transect: No evidence for large-scale flow. Stable isotope, major-and traceelement systematics[END_REF]. Accordingly, these occurrences can hardly be considered as potential Li deposits regarding their ore grade.

Based on the available dataset, 8,839,750 t of Li 2 O (Table 4) are presently reported in Europe from various deposit types and related to various Li-bearing minerals.

Furthermore, our study does not cover lithium in seawater, whose average content has been estimated at 0.17 ppm [START_REF] Fasel | Availability of lithium in the context of future D-T fusion reactors[END_REF][START_REF] Yaksic | Using the cumulative availability curve to assess the threat of mineral depletion: The case of lithium[END_REF], nor that potrentially contained in oilfields (e.g., Pechelbronn in France) and geothermal brines (e.g., the South Crofty deposit in the UK; Cornish Lithium/Strongbow). Such potential lithium sources are difficult to quantify due to fluid mixing, dilution and/or movement [START_REF] Houston | The evaluation of brine prospects and the requirement for modifications to filing standards[END_REF], but research is ongoing (e.g., Eramet-IFPEN), as are potential resource estimates from such sources.

Range of ore grade and tonnage

At the deposit scale, metric tons of ore and average grades (Fig. 11,Table 4) of European hard-rock lithium deposits are relatively competitive compared to the world-class LCT pegmatites from the Greenbushes in Australia and Whabouchi in Canada, which are representative examples of such Lideposits. In detail, the Proterozoic Ukrainian pegmatites show similar grades and tonnages, whereas Variscan pegmatites host lower tonnages. Thus, as pointed out before, significant differences in Li content are seen among the various orogens. Interestingly, the Svecofennian, Sveconorwegian and Variscan orogenies, which involved supercontinent accretion, continent-continent collision and notable late lithospheric thickening, resulted in richer lithium deposits than the Cadomian, Caledonian and Alpine orogenies. This suggests that processes involving extensive crustal anatexis from lithospheric thickening lead to significant Li enrichment (Černý, 1991a, b). For the Apine orogen, the dearth in Li deposits could be related to a present-day deep erosional level, as indicated by the presence of few LCT pegmatites emplaced at the highest structural levels, highlighted by miarolitic [START_REF] Guastoni | Tertiary pegmatite dikes of the Central Alps[END_REF][START_REF] Guastoni | Monazite-(Ce) and xenotime-(Y) from an LCT, NYF tertiary pegmatite field: evidence from a regional study in the Central Alps (Italy and Switzerland)[END_REF] features (MI class of [START_REF] Černý | The classification of granitic pegmatites revisited[END_REF].

It also appears that greisen and RMG containing mainly Li-micas (lepidolite, zinnwaldite, Limuscovite) and Li-phosphates, may contain relatively higher tonnages, but lower grades, than the LCT pegmatites, which contain mainly spodumene-and petalite-dominated Li-bearing minerals (Figs. 11,12). This is, first, a function of deposit size: pegmatites are narrow and well constrained whereas greisen and RMG can form kilometer-scale cupolas and may have deep roots (e.g., Beauvoir). Second, the type of Li-bearing mineral, within which the Li 2 O content may vary significantly (Table 1), is another major parameter, illustrated by spodumene versus zinnwaldite.

Finally, in addition to the above points, ore grade can be controlled by several other parameters. These include the geochemistry of fluxing fluids (F, B and P), different crystallization parameters and P-T conditions (spodumene versus petalite; [START_REF] Černý | The Tanco pegmatite at Bernic Lake, Manitoba. IV. Petalite and Spodumene relations[END_REF], and variable degrees of fractionation (Li-phosphate occurrences against amblygonite-montebrasite or triphylite-sickleriteferrisicklerite series; Černý, 1991b). All these may affect the number and type of Li-bearing minerals, as well as their mineral size and relative abundance, and therefore the overall Li content.

4.6

Perspectives As emphasized by this study, lithium in hard-rock deposits is not rare in Europe and well distributed within Proterozoic to Cenozoic orogens (Fig. 8). The Variscan orogeny (Fig. 6) shows the most important Li-content (more than 60% of the identified deposits in Table 4) in various deposit types (greisen, RMG, pegmatite). The oldest orogens mainly contain LCT pegmatites (Figs. 3,5) that tend to cluster, potentially because of successive orogenic reworking. However, only very few studies report lithium occurrences related to young Mediterranean orogens, suggesting either a lack of exploration or a significant difference between the Variscan and Alpine orogenies.

As for jadarite occurrences, greenfield exploration in Balkan countries such as Serbia and Bosnia may identify latent deposits related to lacustrine evaporite basins. Currently, this area is relatively underexplored and several exploration and mining companies showed recent interest in acquiring permits, such as the Australian firm South East Asia Resources, recently renamed Jadar Lithium.

Regarding Li-production, LCT pegmatites that generally have high lithium grades and low tonnages could be rapidly in production as Li-extraction processes for spodumene are operational. Greisen and RMG, which have low Li grades and high tonnages, will take somewhat longer to reach production as the extraction processes of Li-bearing micas must be demonstrated at deposit scale.

Conclusions

This review of Li hard-rock lithium metallogeny in Europe demonstrates that a wide range of deposit types, including endogenous (LCT pegmatites, RMG, greisen) and exogenous (Jadar, bauxite) processes, is involved. The lithium is contained in various Li-bearing minerals, such as spodumene, lepidolite and zinnwaldite, which are related to different orogenies through time. A favorable geodynamic setting for endogenous magmatic lithium accumulation comprises a late orogenic process, commonly postdating arc accretion, coeval with continent-continent collision, and related to local crustal thickening. A post-orogenic extensional setting is favorable for exogenous processes that can concentrate lithium into a deposit.

At present, 27 potential hard-rock deposits have been identified in Europe. The sum of such Li resources is estimated at 8,839,750 t of Li 2 O. Their production may secure, in part, European lithium requirements in the near future. Our inventory also reflects the heterogeneity in knowledge regarding lithium occurrences. This is due to a relative lack of interest in lithium until recently and suggests that new targets might be defined in the foreseeable future through active ongoing exploration.

Acknowledgements

We gratefully acknowledge Drs. Mali H., Uher P., and Ilickovic T. for their assistance regarding European occurrence locations. We also thank Matevž Novak from the Geological Survey of Slovenia for the use of the jadarite picture. This study was funded by the French Centre for Excellence Voltaire* -LABEX VOLTAIRE (Geofluids and VOLatils, Earth, Atmosphere -Resources and Environment) in collaboration with the French geological survey (BRGM) and the Economic Laboratory of Orléans University (LEO). We thank two anonymous reviewers and Dr. Seltmann for their constructive comments that greatly helped to improve the manuscript. Dr. H.M. Kluijver edited the final English version of the MS. Table 2: RMG classification according to [START_REF] Linnen | Granite-related rare-element deposits and experimental constraints on Ta-Nb-W-Sn-Zr-Hf mineralization[END_REF] with European examples. Table 3: Pegmatite classification according to [START_REF] Černý | The classification of granitic pegmatites revisited[END_REF] and Černý et al. ( 2012) and corresponding P/T conditions. LCT pegmatites in red show a significant lithium potential and those in orange a moderate lithium potential, with corresponding examples if known. LCT = lithium-cesiumtantalum; NYF = niobium-yttrium-fluorine. Table 4: Li projects in Europe and their past production and estimated Li metal resources/reserves. NA refers to data not available. (data were collected from exploration and mining companies; [START_REF] Lulzac | Inventaire du territoire métropolitain les minéralisations à étain, tantale et lithium de Tréguennec (Finistère), état des connaissances au 31 mars[END_REF][START_REF] Smolin | Mineral opportunities in Ukraine; 3 rd Conference on Raw Materials; European Innovation Parternship on Raw Materials[END_REF]British Geological Survey, 2016) Table 5: Location and dating of several pegmatites, RMG and greisen deposits in Europe

Figure captions

Figure 1. Cross sections of various lithium deposits. Lithium-bearing units are identified in red in each section. A) Beauvoir RMG (France) and related stockwork (modified from [START_REF] Cuney | Objectifs généraux du projet GPF Echassières n°1 et résultats essentiels acquis par le forage de 900 m sur le granite albitique à topaze-lépidolite de Beauvoir[END_REF]. B) Sepeda pegmatite in Portugal (modified from Dakota Minerals, 2017); pink area represents barren pegmatite. C) Cinovec deposit in Czech Republic (modified from [START_REF] Breiter | Diversity of Ti-Sn-W-Nb-Ta oxide minerals in the classic granite-related magmatichydrothermal Cinovec/Zinnwald Sn-W-Li deposit (Czech Republic)[END_REF]. D) Jadar Basin in Serbia and location of the jadarite layers (modified from [START_REF] Tinto | Notice to ASX, Increase to Jadar Project Mineral Resources[END_REF]. Color should be used Figure 2. Photographs of various styles of lithium mineralization. A) Quartz-feldspar and zinnwaldite mineralization (Podlesi, Czech Republic). B) Greisen and related La Bosse stockwork (Beauvoir, Massif Central, France). C) Montebras stocksheider hosted in RMG (Massif Central, France). D) Phenocrysts of petalite (yellowish-greenish minerals) surrounded by purplish lepidolite in quartzpotassic feldspar-albite matrix (Chédeville pegmatite, Massif Central, France). E) Alternating lepidolite-rich and aplite-rich layers in a horizontal pegmatite (Chédeville pegmatite, Massif Central, France). Scale represents 7 cm. Abbreviations: Lpd: lepidolite; Ptl: petalite; Znw: Zinnwaldite; Qz+Fsp: quartz+feldspar. F) Jadarite mineralization (Jadar Basin, Serbia) in mudstone (courtesy of Matevž Novak, Geological Survey of Slovenia) Color should be used Figure 3. A) Schematic map of the East European Craton and distribution of the main shields (modified after [START_REF] Roberts | Continental growth and reworking on the edge of the Columbia and Rodinia supercontinents; 1.86-0.9 Ga accretionary orogeny in southwest Fennoscandia[END_REF]. The red box highlights the studied area. B) Simplified geological map of the Fennoscandian Shield (modified after [START_REF] Koistinen | Geological Map of the Fennoscandian Shield[END_REF][START_REF] Bergh | Multiple post-Svecofennian 1750-1560 Ma pegmatite dykes in Archean-Paleoproterozoic rocks of the West Troms Basement Complex, North Norway: Geological significance and regional implications[END_REF] showing distribution of the Svecofennian and the Sveconorwegian orogens, and distribution of LCT and mixed NYF-LCT pegmatites. Red circles and surrounded red names refer to LCT pegmatite fields; blue circle and name refer to mixed NYF-LCT pegmatite field; n = number of identified pegmatite bodies. Abbreviations: B: Bamble Terrane; ES: Eastern Segment; I: Idefjorden Terrane; T: Telemark Terrane; SFDZ: Sveconorwegian Frontal Deformation Zone. Color should be used Figure 4. Simplified geological map of the crustal block involved in the Caledonian orogeny along the Rheic Suture and location of contemporaneous Mn-(Fe) rich deposits (modified after [START_REF] Linnemann | The continuum between Cadomian orogenesis and opening of the Rheic Ocean: constraints from LA-ICP-MS U-Pb zircon dating and analysis of plate-tectonic setting (Saxo-Thuringian Zone, NE Bohemian Massif, Germany)[END_REF][START_REF] Garfunkel | The relations between Gondwana and the adjacent peripheral Cadomian domainconstrains on the origin, history and paleogeography of the peripheral domain[END_REF]. Note that Caledonian relics within Gondwana were reworked during the Variscan and Alpine orogenies making reconstruction of their respective contacts difficult. Color should be used Figure 5. A) Schematic map of the Mid-Devonian paleo-continental reconstruction (modified after [START_REF] Woodcock | A Rheic cause for the Acadian deformation in Europe[END_REF]. Red box highlights studied area. B) Simplified geological map of Ireland and northern Britain with distribution of LCT pegmatites related to the Caledonian orogeny (modified after [START_REF] Miles | Tectonic controls on post-subduction granite genesis and emplacement: The Late Caledonian suite of Britain and Ireland[END_REF]. Red circle and surrounded red name refer to Leinster LCT pegmatite fields from which nine LCT pegmatites are identified. Color should be used Figure 6. Simplified geological map of the Variscan orogeny in Europe, location of various lithiumbearing deposits and a selection of ages (modified after [START_REF] Murphy | Comparative evolution of the Iapetus and Rheic oceans: A North American perspective[END_REF]Martínez Catalán, 1990). Note that the Variscan orogeny was subsequently reworked along the Alpine Front by the Alpine orogeny. Additionally, 260 Li-rich bodies including LCT pegmatites, greisen and the Argemela RMG are identified in Portugal and Spain, 50 Li-rich occurrences are identified in the Bohemian Massif and 26 LCT pegmatites are identified in South Austria. Abbreviations: AM: Armorican Massif; AVZ: Arveno-Vosgina Zones; BM: Bohemian Massif; CAZ: Central Armorican Zone; CIZ: Central Iberian Zone; CZ: Cantabrian Zone; GTMZ: Galicia-Tras-os-Montes Zone; MZ: Moldanubian Zone; NAZ: North Armorican Zone; OS: Ossa-Morena Zone; RM: Rhenish Massif; SAZ: South Armorican Zone; SPZ: South Portugese Zone; SZ: Saxothuringian Zone; TBZ: Tepla-Barradian Zone; WALZ: West Asturian-Leonese Zone. Color should be used Figure 7. Simplified geological map of the Alpine-Mediterranean area and location of lithium-bearing deposits (modified after [START_REF] Tomljenovic | Strukturne Znacajke Medvednice i Samoborskoj gorja[END_REF][START_REF] Bousquet | Tectonic framework of the Alps[END_REF]. Brissago and Elba Islands pegmatite fields are highlighted by a red circle; black circle is Dauphinois region with cookeites; n suggests number of identified pegmatite bodies. Abbreviations: BM: Bohemian Massif; EA: Eastern Alps; EC: East Carpathians; IWC: Internal West Carpathians; NCA: Northern Calcareous Alps; SC: South Carpathians. Color should be used Figure 8. Simplified geotectonic map of Europe (modified after [START_REF] Artemieva | Deep Europe today: geophysical synthesis of the upper mantle structure and lithospheric processes over 3.5 Ga[END_REF][START_REF] Charles | Rare earth elements in Europe and Greenland: a geological potential? An overview; Mineral Deposit Research for a high-Tech World[END_REF] and distribution of various Li-bearing occurrences. Color should be used Figure 9. Location map of the Li deposits (Table 4) in Europe (modified after [START_REF] Artemieva | Deep Europe today: geophysical synthesis of the upper mantle structure and lithospheric processes over 3.5 Ga[END_REF][START_REF] Charles | Rare earth elements in Europe and Greenland: a geological potential? An overview; Mineral Deposit Research for a high-Tech World[END_REF]. Categories refer to: A ≥ 1,000,000 t Li 2 O; 1,000,000 t ≥ Category B ≥ 100,000 t Li 2 O; 100,000 t ≥ Category C ≥ 50,000 t Li 2 O; 50,000 t ≥ Category D ≥ 5,000 t Li 2 O; Category E <5,000 t Li 2 O and past production and mineral resources. Color should be used Figure 10. Geological sections of favorable lithium setting. Continental collision (A; modified from [START_REF] Menant | 3D subduction dynamics: A first-order parameter of the transition from copper-to gold-rich deposits in the eastern Mediterranean region[END_REF] shifting to post-collision setting (B; modified from [START_REF] Menant | 3D subduction dynamics: A first-order parameter of the transition from copper-to gold-rich deposits in the eastern Mediterranean region[END_REF] represents favorable context for Li-hard-rock formation such as LCT pegmatites, RMG and greisen along orogenic collapse (C). Superscripts on C correspond to European examples: 1 = Chédeville, Mina Feli, or Gonçalo; 2 = Richemont; 3 = Beauvoir, Argemela and Montebras; 4 = Barroso-Alvao, Läntta and Aclare. Continental subduction (D; modified from [START_REF] Menant | 3D subduction dynamics: A first-order parameter of the transition from copper-to gold-rich deposits in the eastern Mediterranean region[END_REF] shifting to back-arc setting (E; modified from [START_REF] Menant | 3D subduction dynamics: A first-order parameter of the transition from copper-to gold-rich deposits in the eastern Mediterranean region[END_REF] represents favorable context for sedimentary/hydrothermal Li deposits such as Jadar (F; modified from Stojadinovic et al., 2016). LCT pegmatite can also occur in such a context. Color should be used Figure 11. Average lithium grade (wt.% Li 2 O) versus metric tons of ore (Mt) for the 28 identified Li deposits in Europe regarding their deposit type. Deposits and projects based on historical estimates are written in italics and those based on the CRIRSCO system in bold. The Whabouchi (Canada; blue triangle) and Greenbushes (Australia; green triangle) pegmatite deposits are mentioned here in order to compare these world-class deposits to European grades and tonnages. Color should be used Figure 12. Grade (wt.% Li 2 O) versus deposit types (A) and deposit tonnage (Mt) versus deposit types (B) considering resource estimates. The boxes indicate the median (black line), upper and lower quartiles (25%; gray boxes), maximum and minimum values (upper and lower whiskers) and outliers (black circles). Note that n reflects the total number of deposits considered for this summary plot. 4. Li projects in Europe and their past production and estimated Li metal resources/reserves. NA refers to data not available. (data were collected from mining companies; [START_REF] Lulzac | Inventaire du territoire métropolitain les minéralisations à étain, tantale et lithium de Tréguennec (Finistère), état des connaissances au 31 mars[END_REF][START_REF] Smolin | Mineral opportunities in Ukraine; 3 rd Conference on Raw Materials; European Innovation Parternship on Raw Materials[END_REF], British Geological Survey, 2016)

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 5 Fig.5

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 6 Fig.6

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 7 Fig.7

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 8 Fig.8

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 9 Fig.9

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 10 Fig.10

Fig. 11

 11 Fig.11

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 12 Fig.12

Table 1 .

 1 Main Li-bearing minerals encountered in Europe, their corresponding chemical formula, Li content and physical characteristics

					Specifi
					c
	Name	Formula	Mineral group	Theoretic al values	gravit y	Hardne ss
					(g/cm3
					)
					Li
				Li2O %	metal
					%
	Eucryptite LiAlSiO4	Feldspathoi d	11.86	5.51	2.67	6.5
	Amblygonit e	(Li,Na)Al(PO4)(F,OH)	Phosphate 10.1	4.69	2.98	5.5-6
	Montebrasit e	LiAl(PO4)(OH,F)	Phosphate 10.1	4.69	3.98	5.5-7
	Lithiophilite Li(Mn,Fe)PO4	Phosphate 9.53	4.43	3.5	5
	Sicklerite Li 1-x(Fe 3+ x, Mn 2+ 1-x)PO5	Phosphate < 9.48	4.40	3.2-3.4 4
	Ferrisickleri te	Li 1-x(Fe 3+ x, Mn 2+ 1-x)PO4	Phosphate < 9.47	4.40	3.2-3.4 4
	Triphylite Li(Fe,Mn)PO4	Phosphate 9.47	4.40	3.5	4-5
	Spodumene LiAl(Si2O6)	Inosilicate 8.03	3.73	3.2	6.5-7
	Lepidolite K(Li,Al)3(Si,Al)4O10(OH,F)2	Phyllosilica te	7.7	3.58	2.8-2.9	1.55 -1.59
	Jadarite	LiNaSiB3O7(OH)	Neosilicate 7.3	3.39	2.45	4-5
	Polylithionit e	KLi2Al(Si4O10)(F,OH)2	Phyllosilica te	6.46	3.00	2.58-2.82	2-3
	Petalite	LiAl(Si4O10)	Tectosilicat e	4.88	2.26	2.4-2.46	6-6.5
	Zinnwaldite KLiFeAl(Al,Si3)O10(OH,F)2	Phyllosilica te	4.12	1.91	2.9-3.2	5.5-6
	Elbaite	Na(Li1.5Al1.5)Al6Si6O18(BO3)3( OH)4	Cyclosilicat e	4.07	1.89	2.9-3.2 7.5
	Holmquistit e	X(Li2)(Mg3Al2)(Si8O22)(OH)2 Inosilicate 3.98	1.85	3.06-3.13	5.5
	Cookeite	LiAl4(AlSi3O10)(OH)8	Phyllosilica te	2.9	1.34	2.58-2.69	2.5-3.5
	Lithiophorit e	(Al, Li)Mn 4+ O2(OH)2	Oxide	1.23	0.57	3.14-3.37	2.5-3

Table 2 .

 2 RMG classification according toČerný et al. (2005) with European examples.

					Specifi
					c
	Name	Formula	Mineral group	Theoretic al values	gravit y	Hardne ss
					(g/cm3
					)
					Li
				Li2O %	metal
					%
	Eucryptite LiAlSiO4	Feldspathoi d	11.86	5.51	2.67	6.5
	Amblygonit e	(Li,Na)Al(PO4)(F,OH)	Phosphate 10.1	4.69	2.98	5.5-6
	Montebrasit e	LiAl(PO4)(OH,F)	Phosphate 10.1	4.69	3.98	5.5-7
	Lithiophilite Li(Mn,Fe)PO4	Phosphate 9.53	4.43	3.5	5
	Sicklerite Li 1-x(Fe 3+ x, Mn 2+ 1-x)PO5	Phosphate < 9.48	4.40	3.2-3.4 4
	Ferrisickleri te	Li 1-x(Fe 3+ x, Mn 2+ 1-x)PO4	Phosphate < 9.47	4.40	3.2-3.4 4
	Triphylite Li(Fe,Mn)PO4	Phosphate 9.47	4.40	3.5	4-5
	Spodumene LiAl(Si2O6)	Inosilicate 8.03	3.73	3.2	6.5-7
	Lepidolite K(Li,Al)3(Si,Al)4O10(OH,F)2	Phyllosilica te	7.7	3.58	2.8-2.9	1.55 -1.59
	Jadarite	LiNaSiB3O7(OH)	Neosilicate 7.3	3.39	2.45	4-5
	Polylithionit e	KLi2Al(Si4O10)(F,OH)2	Phyllosilica te	6.46	3.00	2.58-2.82	2-3
	Petalite	LiAl(Si4O10)	Tectosilicat e	4.88	2.26	2.4-2.46	6-6.5
	Zinnwaldite KLiFeAl(Al,Si3)O10(OH,F)2	Phyllosilica te	4.12	1.91	2.9-3.2	5.5-6
	Elbaite	Na(Li1.5Al1.5)Al6Si6O18(BO3)3( OH)4	Cyclosilicat e	4.07	1.89	2.9-3.2 7.5
	Holmquistit e	X(Li2)(Mg3Al2)(Si8O22)(OH)2 Inosilicate 3.98	1.85	3.06-3.13	5.5
	Cookeite	LiAl4(AlSi3O10)(OH)8	Phyllosilica te	2.9	1.34	2.58-2.69	2.5-3.5
	Lithiophorit e	(Al, Li)Mn 4+ O2(OH)2	Oxide	1.23	0.57	3.14-3.37	2.5-3

Table 3 .

 3 Pegmatite classification according toČerný and Ercit, 2005, Černý et al., 2012 and corresponding P/T conditions.

	Class	Subclas s	Type	Subtype	Host rock	Pressur e	Famil y	Examples	Reference s
					Temp
	Abyssal HREE			700-800 °C	> 5 kbar NYF
		LREE
		U					NYF
		B/Be					LCT
	Muscovite				650-580 °C	5 to 8 kbar
	Muscovite -rare element	REE			650-520 °C	3-7 kbar NYF
		Li					LCT
	Rare
	element
		REE	allanite-monazite		variabl e	variable NYF
			euxenite
			gadolinite
		Li	beryl	beryl-columbite	650-450 °C	2-4 kbar LCT	Moravany, Slovakia	Uher et al., 2010
				beryl-				Pedra da	Roda-
				columbite-				Moura,	Robles et
				phosphate				Portugal	al., 2016
			complex spodumene				Alijó, Portugal	Lima, 2000
				petalite				Varutrask, Sweden	Černý and Ercit, 2005
								Rozná,	Melleton
				lepidolite				Czech	et al.,
								Republic	2012
				elbaite				Ctidružice, Czech Republic	Novák and Povondra, 1995,
				amblygonit				Viitaniemi,	Lahti,
				e				Finland	1981
			albite-spodumen e					Most of the Barroso-Portugal Alvão,	Lima, 2000

Table

Table 5 .

 5 Location and dating of several pegmatite, RMG and greisen deposits in Europe

										Age 1
	Country	Occurrence Name	Latitude (decimal degrees)	Longitude (decimal degrees)	Orogeny	Litholo gy	Area	Age (M a)	±2 σ	Mineral analyzed	Meth od	Referenc e
	Sweden Utö gruvor	59.667133	14.316415	Svecofenni an	LCT pegma tite		182 1	16	columbite-tantalite	U/Pb	Romer and Smeds. 1994
	Sweden Rånö	58.928539	18.180919	Svecofenni an	LCT pegma tite		181 9	4	columbite-tantalite	U/Pb	Romer and Smeds. 1994
	Sweden Norrö	58.88583333 33333	18.13444444 44444	Svecofenni an	LCT pegma tite		181 9	6	columbite-tantalite	U/Pb	Romer and Smeds. 1994
	Finland Rosendal	60.123	22.553	Svecofenni an	LCT pegma tite		180 7	3	ferrotapiol ite	U/Pb	Lindroos et al.. 1996
	Finland Kaatiala	62.67916666 66667	23.49055555 55556	Svecofenni an	LCT pegma tite		180 4	2	columbite-tantalite	U/Pb	Alviola et al.. 2001
	Finland Skogsböle	60.142	22.598	Svecofenni an	LCT pegma tite	Kemiö pegmati te field	180 3	1. 3	ferrotapiol ite	U/Pb	Lindroos et al.. 1996
	Finland Seinäjoki	62.779	23.1846	Svecofenni an	LCT pegma tite		180 2	2	ferrotapiol ite	U/Pb	Alviola et al.. 2001
	Sweden Jarkvissle	62.83805555 55556	16.63888888 88889	Svecofenni an	LCT pegma tite		180 0	3. 6	columbite-tantalite	U/Pb	Romer and Smeds.. 1997
	Sweden Dyngselet	63.24422	18.156294	Svecofenni an	LCT pegma tite		179 9	11	columbite-tantalite	U/Pb	Romer and Smeds.. 1994
	Finland Haapaluoma	62.508	22.983	Svecofenni an	LCT pegma tite		179 7	2	columbite-tantalite	U/Pb	Alviola et al.. 2001
	Sweden Stenbackberget 63.239526	18.224771	Svecofenni an	LCT pegma tite		179 7	7	columbite-tantalite	U/Pb	Romer and Smeds..