The study is part of an extensive survey of the mineralogy of the Panasqueira W–Sn–Cu deposit (Central Portugal), aimed at deciphering the main factors controlling ore deposition in space and time. Wolframite was deposited in several stages: Stages I and II correspond to the primary tungsten mineralisation in quartz-wolframite veins with tourmalinized wallrocks. In stage III, deposition of wolframite, quantitatively minor, was followed by cassiterite and sulphides. In stage IV, spectacular “collector” wolframite was deposited in tubular vugs, together with cassiterite, arsenopyrite, muscovite, and apatite. Wolframite at Panasqueira is overwhelmingly ferberitic, with Fe/(Fe + Mn) ratios predominantly between 0.81 and 0.86, but Mn-rich patches, microcracks and rims developed in Stage IV. The Fe and Mn contents of wolframite record the contributions from metamorphic, magmatic, and subsolidus interaction-derived fluids. From Stages I-II to IV, fluids evolved from dominantly Fe-rich to progressively enriched in Mn through mixing with an Mn-rich fluid end-member sourced in rare-metal granites (either magmatic fluids or a result of fluid-rock interaction). Wolframite thus provides a sensitive tracer of both the structural dynamics of the vein system and the episodic magmatic–hydrothermal contributions sustaining tungsten mineralisation at Panasqueira. Wolframite is the dominant tungsten mineral at Panasqueira, deposited in multiple generations of veins. Two main episodes of wolframite formation: early quartz–wolframite stages (I–II) and late “vug stage” (IV). Wolframite is overwhelmingly ferberitic (Fe/(Fe + Mn) = 0.81–0.86), with limited oscillatory Mn zoning. Late hydrothermal hübneritisation reflects the input of Mn-rich fluids during Stage IV, likely linked to late magmatic activity (295–300 Ma).

The small elliptic Rechla granite pegmatite complex belongs to the c.525 Ma Rare Metal Granite (RMG) province of the Laouni terrane of the Pan-African Tuareg Shield (Hoggar). It intrudes a porphyritic biotite-granite and is particularized by a rim of Quartz, K-feldspar and Zinnwaldite pegmatite. The centre is occupied by a medium-grained granite, with quartz, albite (An01), rare microcline, topaz, lepidolite ( similar to 8% MnO), wolframowodginite and Hf-zircon. The pegmatite rim comprises, toward the intrusion (i) thick K-feldspar lenses (palissadic crystals similar to 50 cm), (ii) a laminated quartz-zinnwaldite-(beryl) sequence, described as a unidirectional solidification texture (UST), and (iii) a discontinuous band of fine-grained granite, with quartz, albite, topaz, lepidolite, titanowodginite and beryl. The laminated sequence overprints the K-feldspar lenses. It comprises thick (similar to 20 m) quartz lenses cross-cut by 10 cm-sized alternating bands of euhedral quartz and Mn-zinnwaldite (similar to 6.5% MnO). At the boundary with the fine-grained internal band, euhedral quartz crystals are projecting toward the inner wall. The chemical composition of the medium-grained granite is typical of a low-P peraluminous RMG deriving from highly potassic calcalkaline suites (A2 type) enriched in Ta (165 ppm, Ta/Nb between 2.4 and 2.6), expressedas columbo-tantalite and Mn-wodginite, with low P2O5 (0.05%) and Sigma REE (23 ppm) contents, with a pronounced tetrad effect and <0 Eu anomaly in the REE pattern. The fine-grained granite is equally fractionated with Ta 240 ppm (Ta/Nb = 2.4) and Be 500 ppm. The surrounding porphyritic biotite-granite is representative of the evolved magmas of the A2-type Taourirt suite in the nearby terranes. Geochemical modeling, using the filter press model, shows that the main Rechla magma is likely the fractionated product of this already differentiated magma, mainly involving quartz and Kfs. The pegmatite rim is interpreted as the result of the sequential crystallization of a Rechla-type melt, with late individualization of a Fe-rich magmatic-hydrothermal phase responsible for the quartz-zinnwaldite assemblage, leaving a strongly Be-enriched residual liquid (the fine-grained granite). As demonstrated by the Rechla occurrence, Ta concentration at levels similar to those in Beauvoir-type high-P peraluminous granites may be reached in the low-P low-Ta A2 suites, provided that extreme fractionation processes are established.

The relationship between critical metal mineralisations (W, Sn, Nb, Ta, Li) and collisional orogens remains poorly understood. We combine U-Pb geochronology of metal-carrying minerals and geochemical modelling to constrain metal mobility in the Variscan Iberian collisional orogen. Two overlapping periods of mineralisation are identified: magmatic-hydrothermal Sn-W deposits from ca. 340 to 285 Ma and rare-metal granite (RMG) and pegmatite (RMP) Li-Sn-Nb-Ta deposits from ca. 315 to 295 Ma. We show that W-rich fluids can be produced from metapelite-derived anatectic melts without further differentiation, leading to their dominance over Sn (+Li-Nb-Ta) early in orogenesis. In contrast, RMG/RMP generation is favoured by transcurrent structures and melting of felsic meta-igneous protoliths. Both features become increasingly abundant towards the end of this collisional orogen. The progression from W- to Sn-dominant magmatic-hydrothermal mineralisation, followed by RMG/RMP, is a consequence of collisional orogen dynamics.

In the Tamanrasset area of the Pan-African Tuareg Shield, some of the late Pan-African intrusions collectively known as the Taourirt granites are associated with tin and tungsten prospects of both the quartz-vein and greisen types, with a variety of greisen styles. The mineralized intrusions are albite-topaz-protolithionite granites and microgranites. In the present work, we combine new observations and mica analyses with a reinterpretation of existing wall-rock geochemical data in order to assess the possible role of both magmatic-hydrothermal and external fluids in the greisenizing process at Tamanrasset. Greisens at Tamanrasset appear to result from two process: the first is acid leaching forming quartz-topaz and quartz-rich greisens, followed by an episyenitization which is characterized by quartz dissolution and replacements by Li-rich micas, leading to mica-rich greisens (that could better be named “pseudo-greisens”). Distinct trends recorded by the mica compositions in the granitic rocks and the greisens allow to disentangle the involvement of magmatic-hydrothermal fluids, on the one hand, and of mainly metamorphic external fluids, on the other hand, in the greisenizing process. The latter fluids were CO2-rich, and could have contributed to the source of the acidity.

The Great Duchy of Luxembourg comprises a Variscan basement, part of the Ardennes-Rhenish fold-and-thrust belt and an unconformable Mesozoic sedimentary cover representative of the eastern margin of the Paris Basin. The basement hosts several vein-type ore deposits, which remain almosundocumented until now, except for a few geological and mineralogical descriptions. The Stolzembourg Cu-deposit and the Martelange and Soleuvre Pb–Zn–Ba deposits occur at the boundary of several ore deposit provinces in Belgium and Germany. By coupling the mineralogy of fracture infillings and P-T-X reconstruction thanks to a detailed fluid inclusion study, the primary fluid events and associated metal transfer and deposition are described and compared with other Mesozoic deposits in the nearby areas. At Stolzembourg copper-only deposit, the anisothermal mixing between two highly saline (a Ca–Na and a Na-only rich end-member) fluids of ca.27 wt

Chapter 3 The W Deposit at Panasqueira (Portugal) A Critical Bibliographical Review Christian MARIGNAC, Christian MARIGNAC GeoRessources, CREGU, University of Lorraine, Nancy, FranceSearch for more papers by this authorMichel CATHELINEAU, Michel CATHELINEAU GeoRessources, CREGU, University of Lorraine, Nancy, FranceSearch for more papers by this author Christian MARIGNAC, Christian MARIGNAC GeoRessources, CREGU, University of Lorraine, Nancy, FranceSearch for more papers by this authorMichel CATHELINEAU, Michel CATHELINEAU GeoRessources, CREGU, University of Lorraine, Nancy, FranceSearch for more papers by this author Sophie Decrée, Sophie DecréeSearch for more papers by this author Book Author(s):Sophie Decrée, Sophie DecréeSearch for more papers by this author First published: 29 December 2023 https://doi.org/10.1002/9781394264810.ch3 AboutPDFPDF ToolsRequest permissionExport citationAdd to favoritesTrack citation ShareShareShare a linkShare onEmailFacebookTwitterLinkedInRedditWechat Summary Variscan Western Europe is one of the world's great tin-tungsten provinces, within an initial endowment that can be estimated to have been on the order of a million tonnes of tungsten. With greisens and skarns, the peribatholic Sn-W mineralized veins play a major role. The Portuguese Panasqueira deposit is emblematic of the latter. This world-class deposit, situated in the Central Iberian Zone (CIZ) of the Variscan orogeny, contained 147 kt W when it was discovered at the end of the 19th century, that is, more than one-third of the total endowment of the CIZ, estimated at 350 kt W. The polymetallic deposit at Panasqueira (W-Sn-Cu) is situated in the Beira Baixa province (Central Portugal). It lies in the CIZ, which represents the axial zone of the Iberian Variscan belt. References Antunes , I.M.H.R. , Neiva , A.M.R. , Silva , M.M.V.G. ( 2010 ). Isotopic geochronology of granitic rocks from the central Iberian zone: Comparison of methodologies . Estud. Geol. , 66 , 45 – 50 . 10.3989/egeol.40143.097 Google Scholar Audétat , A. ( 2019 ). The metal content of magmatic-hydrothermal fluids and its relationship to mineralization potential . Econ. 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The southeastern French Massif Central represents an ideal area to study the linkage between regional metamorphism, crustal partial melting, emplacement of granitic magmas, and hydrothermal Sn-W mineralization in a polyphase tectono-metamorphic setting related to the late-Variscan orogeny. Here, we describe the mineralogical, structural, geochemical, and geochronological characteristics of cassiterite–wolframite-bearing quartz veins at St-Mélany, a small uneconomic Sn-W occurrence located in the North Cévennes area. The veins show evidence of ductile deformation (boudinage, asymmetric folding, dynamic recrystallization) consistent with a synkinematic emplacement during the regional low-pressure–medium-temperature metamorphism at ca. 320–315 Ma. This dominantly water-fluxed melting event reaching muscovite breakdown conditions ( T < 750 °C, P ≈ 0.6 GPa) was synchronous to the emplacement of the syntectonic Rocles peraluminous granite, which is interpreted as a proximal source for the mineralizing fluids at St-Mélany. The U–Pb LA-ICP-MS dating of coexisting wolframite and cassiterite from a mineralized quartz vein yielded lower-intercept ages of 318.4 ± 2.2 Ma and 311.4 ± 1.0 Ma (2 σ ), respectively. These results suggest a temporal decoupling of W and Sn mineralization with a time gap of 4–10 Myr, but additional work is needed to confirm this interpretation. A weighted mean 40 Ar/ 39 Ar date of 304.5 ± 4.8 Ma (2 σ ) was obtained for muscovite from the selvage of a mineralized vein, interpreted as a recrystallization age related to metamorphic re-equilibration or hydrothermal overprinting. Dikes of aplites and pegmatites cut the Sn-W-mineralized veins and were emplaced at 305.9 ± 3.9 Ma (2 σ ) based on U–Pb LA-ICP-MS dating of magmatic cassiterite. The dikes have highly evolved compositions typical of peraluminous high-phosphorus rare metal granites with Li-F-Ta > Nb-Sn-Be enrichments. Emplacement of the granitic dikes was coeval with the regional low-pressure–high-temperature metamorphism at ca. 305–300 Ma, reaching biotite dehydration melting conditions ( T > 800 °C, P ≈ 0.4 GPa), which led to the formation of the Velay anatectic dome possibly linked to lower crust granulitization. We conclude that polyphase emplacement of W-Sn-mineralized veins at ca. 320–310 Ma and rare metal granitic dikes at ca. 305 Ma results from contrasting crustal melting conditions, in relation to the late-Carboniferous orogenic evolution of the southeastern French Massif Central, and possibly related to delamination of the subcontinental lithospheric mantle.

Free Access Appendix 3: The Panasqueira W Deposit (Portugal) A Critical Bibliographic Review Christian MARIGNAC, Christian MARIGNAC GeoResources, CREGU, University of Lorraine, Nancy, FranceSearch for more papers by this authorMichel CATHELINEAU, Michel CATHELINEAU GeoResources, CREGU, University of Lorraine, Nancy, FranceSearch for more papers by this author Christian MARIGNAC, Christian MARIGNAC GeoResources, CREGU, University of Lorraine, Nancy, FranceSearch for more papers by this authorMichel CATHELINEAU, Michel CATHELINEAU GeoResources, CREGU, University of Lorraine, Nancy, FranceSearch for more papers by this author Sophie Decrée, Sophie DecréeSearch for more papers by this author Book Author(s):Sophie Decrée, Sophie DecréeSearch for more papers by this author First published: 29 December 2023 https://doi.org/10.1002/9781394264810.app3 AboutPDFPDF ToolsRequest permissionExport citationAdd to favoritesTrack citation ShareShareShare a linkShare onEmailFacebookTwitterLinkedInRedditWechat References Blackheath Resources ( 2015 ). 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Le fantastique gisement de tungstène de Panasquera (Portugal), d’âge varisque, est depuis longtemps l’objet d’études géologiques. Les travaux récents qui lui ont été consacrés ont mis en jeu les techniques et les concepts les plus modernes. Marignac et Cathelineau, eux-mêmes acteurs de ces travaux, proposent une lecture critique, aiguisée, de cette minéralisation péri-granitique.

The Djebel El Hamra Pb-Zn-Ba-Sr (Hg) deposits in northern Tunisia are hosted in a post-nappe anticline with a core of a Triassic evaporite diapir affected by the NE–SW-trending Ghardimaou-Cap Serrat lineament. Three stages of mineralization occurred in the Triassic dolostone: stages I and II caused alternating deposition of sulfate (Ba, Sr) and sulfide (sphalerite, galena) minerals; stage III formed late-stage calcite-marcasite-cinnabar. Zebra textures record the syntectonic transition from compression to extension in the Late Tortonian-Messinian interval. Two fluid end-members were involved in sulfate deposition: one low-salinity (L1, ~3 wt% eq. NaCl) fluid, probably from a meteoric origin, and a Na-Ca-Cl brine (L2, ~22 wt% eq. NaCl) solution which originated from the Triassic diapiric source. A third end-member fluid (L3) with long residence time in the basement was also involved in the Pb-Zn deposition. The δ 34 S values from a cluster of sulfates around +16‰, show a Triassic evaporate source. The sulfur in sphalerite resulted from bacterial sulfate reduction (BSR); however, crystallization in a closed system resulted in a range of δ 34 S between +1.6 and +26.5‰. The δ 34 S values in galena (−28.4 to +8.2‰) are consistent with a BSR and thermochemical sulfate reduction (TSR) origin of the sulfur. Secondary ion mass spectrometry (SIMS) lead isotope data in galena ( 207 Pb/ 204 Pb: 15.595 to 16.193, 206 Pb/ 204 Pb: 18.673 to 18.939, 208 Pb/ 204 Pb: 38.330 to 40.572) point to local contributions (sedimentary and Cenozoic magmatic rocks) to the main source from the Precambrian basement. Ore deposition occurred at a depth of about 2 km at temperatures between 80 and 250 °C. A shallow magmatic heat source was the cause of these thermal fluctuations.

The main event responsible for the deposition of tungsten at Panasqueira was closely associated with strong tourmalinization of the wall rocks. Tourmaline is coeval with a W-rich rutile (up to 8–10 wt % W), and both minerals record an early introduction of W in the system, just before the main W deposition. Uranium-Pb dating of the rutile by LA-ICP-MS yielded an age of 305.2 ± 5.7 Ma, which is 6 to 10 m.y. older than the K-Ar age of 296.3 ± 1.2 Ma obtained on muscovite, which was therefore not coeval with wolframite. Major and trace element concentration variations in tourmaline record fluid mixing between two end members, both considered to be of metamorphic derivation on the basis of rare earth element profiles. We report evidence for a fluid rich in Co, Cu, Pb, Sc, Sr, V, Cr, Nb, Ta, and Sn interpreted to be of local origin—e.g., well equilibrated with the host formations—and a fluid rich in Li, F, Fe, Mn, and W inferred to be of deep origin and related to biotite dehydration. The second fluid carried the metals (in particular Fe and Mn) that were necessary for wolframite deposition and that were not necessarily inherited from the wall rocks through fluid-rock interaction. Micrometer-scale variations in tourmaline and rutile crystal chemistry are indicative of pulsatory fluid input during tourmalinization.

A Correction to this paper has been published: https://doi.org/10.1007/s12517-021-06960-4

The Puy-les-Vignes W deposit, located in the northwestern French Massif Central (FMC), is a rare occurrence of a wolframite-mineralized hydrothermal breccia pipe hosted in high-grade metamorphic gneisses. We present an integrated study of this deposit aiming to characterize the ore-forming hydrothermal system in link with the Variscan late-orogenic evolution of the FMC. Based on a set of representative samples from the host rocks and mineralization, we describe a detailed paragenetic sequence and we provide the major and trace element geochemistry of the granitic rocks and W–Nb–Ta–Sn–Ti oxide minerals, in situ U/Pb and 40 Ar/ 39 Ar geochronology, and a fluid inclusion study of quartz and wolframite. We demonstrate that the formation of this W-mineralized breccia pipe results from a multistage development related to four major episodes during the late Carboniferous. The first episode corresponds to the emplacement of an unexposed peraluminous granite at ca. 324 Ma, which generated microgranite dykes exposed at the present-day surface. The second episode is the formation of the quartz-supported breccia pipe and wolframite mineralization at ca. 318 Ma at a paleodepth of 7 km. The mineralizing fluids have a H 2 O–NaCl–CO 2 –CH 4 –N 2 composition, a moderate-salinity (< 9 wt.% NaCl eq) and were trapped at high-temperatures (> 400 °C) during lithostatic to hydrostatic pressure variations caused by hydrofracturing of the host rocks. Wolframite deposition is interpreted to result from a W-rich intermediate-density magmatic fluid that exsolved from an evolved leucogranite and interacted with volatile-rich metasedimentary country rocks and/or possibly mixed with low-salinity metamorphic fluids of deep origin. The third episode corresponds to magmatic-hydrothermal Nb–Ta mineralization overprinting the W-mineralized system interpreted to be related to the intrusion at ca. 311 Ma of a rare-metal granite, which is part of a regional peraluminous rare-metal magmatism during the 315–310 Ma period. Finally, the last episode corresponds to disseminated Bi ± Au–Ag mineralization emplaced at ca. 300 Ma, which shares similar mineralogical features with late Carboniferous orogenic gold deposits in the FMC. The Puy-les-Vignes W deposit records, therefore, a multistage and long-lived development that extends over a timespan of 25 million years in a regional setting dominated by protracted peraluminous magmatism and high-temperature and low-pressure metamorphism. Although the local environment of ore deposition is atypical, our results show that the mineral assemblages, alteration styles, and fluid characteristics of the Puy-les-Vignes breccia pipe are similar to those of other peri-granitic W deposits in the FMC.

Wolframite has been proposed as a U/Pb geochronometer for direct dating of W mineralisation events, but its isotopic analysis may be hampered by highly variable and low U contents (<200 ppm) and low (206)pb/(204)pb ratios ((300), heterogenous common Pb compositions, post-crystallisation alteration, and the presence of non-cogenetic mineral and fluid inclusions. In situ U/Pb dating of wolframite by laser ablation - inductively coupled plasma - mass spectrometry (LA-ICP-MS) can avoid these analytical challenges but requires reference materials to properly correct for matrix and instrumental effects on measured U/Pb ratios. This study presents the U/Pb systematics by LA-ICP-MS of a wolframite sample (MTM-1) from the French Massif Central (FMC) which has been considered for normalisation and validation purposes of U/Pb LA-ICP-MS wolframite data in previous studies. We demonstrate that the MTM-1 wolframite is chemically and isotopically heterogeneous, and more importantly, we show that the previously defined ID-TIMS U/Pb age (334.4 +/- 1.7 Ma, (2 sigma) is invalid due to an inappropriate common Pb correction. We calculate a new U/Pb crystallisation age of 316.7 +/- 5.8 Ma (2 sigma). Based on our new calibration, we also present the U-Th-Pb trace element and U/Pb ages of six W deposits from the FMC, also previously studied by ID-TIMS. We show that U/Pb ages determined by LA-ICP-MS are more robust and geological plausible compared to ID-TIMS ages obtained on the same samples. The concentrations of U (ca 0.1-150 ppm) and Pb (ca 0.01-90 ppm) in FMC wolframite are highly variable and do not ubiquitously correlate to major element composition (such as the Fe/(Fe + Mn) ratio). The chemical variability and isotopic heterogeneity observed in wolframite from the FMC highlights the importance of pre-screening imaging methods (e.g., SEM, EPMA, mu XRF) prior to LA-ICP-MS U/Pb analyses. Based on our results, we propose new guidelines for U/Pb LA-ICP-MS wolframite geochronology to increase accuracy and reproducibility in age determinations, as well as improving interlaboratory comparisons.

The Djilouet complex forms a cupola made up of leucocratic granites associated with Sn-W mineralization. It could represent the Hoggar’s easternmost rare metal granite (RMG) comparatively to those of the Taourirt province in the central Hoggar. It is located in the Djanet terrane, 12 km NE of the town of the same name in the far east of the Tuareg shield in Algeria. The Djanet terrane is made of a thick low-grade (greenschist facies) sedimentary sequence which was intruded by several generations of granitic rocks. The subcircular Djilouet body is made of leucocratic granites with progressive mutual transitions. Most of the outcrop is occupied by a porphyritic coarse-grained biotite granite. A muscovite granite is found in the center of the cupola, whereas a garnet (almandine—spessartite) granite forms a discontinuous rim all around it. Black micas from the biotite granite are lithian annite (“protolithionite”). The white micas from the muscovite granite and the garnet granite are classified as Fe-Li muscovite. The muscovite granite and the garnet granite contain accessory minerals as rutile, xenotime, monazite, zircon, and minerals that may be members of the pyrochlore supergroup. All the facies are leucogranite with high SiO2 content and high K2O-Na2O ratio. They are poor in calcium and in mafic components and have very low phosphorus content (P2O5 ~ 0.1%). The peraluminous composition is low to mild (1.08 < A/CNK > 1.46). The evolved granites of the Djilouet suite are enriched in Th and U, but the tantalum and the niobium are not highly concentrated (Ta + Nb = 10.4–17.1). The total REE content is low (57–84 ppm), and the patterns are typically wing shaped with a strong negative Eu anomaly and a small tetrad effect. The Sn-W mineralization consists two systems of veins: large quartz veins with ferberite (H/F ~ 0.8) and quartz veinlets or stockworks with homogeneous cassiterite and minor wolframite (H/F ~ 48). The iso-content contours of tin and tungsten, as produced from a sampling covering the whole cupola, overlap very little. The differences which were noted throughout the study between the Taourirt granites and those of the Djilouet suite are to be related to the lithological nature of the crust rather than to a difference in the geodynamic environment.

•W and Sn mineralization in the Nanling Range formed during a fluid event at 160 Ma.•Deposits formed during four hydrothermal events over 30 m.y. (160–130 Ma).•Hydrothermal fluid circulations result in partial to complete isotopic resetting.

The Variscan vein-type Panasqueira W-Sn(Cu) deposit, one of the main tungsten deposits in Western Europe, has a long and complicated geological history. The first vein infillings, which consist of the quartz-wolframite association as well as the first generation of topaz, underwent significant deformation. As a consequence, most fluid inclusions of the earliest hydrothermal event are deformed and destroyed. Two preserved fluid inclusion assemblages are, however, found in the topaz overgrowth band and are dense aqueous-carbonic inclusions as well as dense CO2 dominated fluid inclusions. The P-T conditions of fluid trapping are constrained by using the intersection between isochores, as well as graphite-water equilibrium data and yield the following trapping conditions: 500 20 degrees C and 250 +/- 20 MPa. These P-T conditions are incompatible with fluid unmixing. Fluid chemistry results from water-graphite equilibrium, probably in metapelites, at two distinct temperatures: around 450-500 degrees C for the predominant aqueous-carbonic fluid, and higher temperatures of maximal550 degrees C for the CO(2)rich fluid enriched in N-2. These P-T estimates are consistent with deep crustal levels around 8-10 km depth and a high geothermal gradient around c. 60 degrees C/km(-1). The ascending non-magmatic fluids, enriched in volatiles, are essential in the ore genesis. The high thermal gradients may be related either to new magma pulse after the formation of the Panasqueira granite intrusion or to anomalous heat flux produced by the hot fluids ascending from migmatitic levels present at greater depth. This hypothesis necessitates to consider the role of a crustal weakness, which is attested both by the successive intrusions of several granitic magmas at the same place, and the presence of inherited quartz filled structures so-called Seixo-Bravo found only in the Panasqueira area.

Elucidation of time-space relationships between a given wolframite deposit and the associated granites, the nature of the latter, and their alterations, is a prerequisite to establishing a genetic model. In the case of the world-class Panasqueira deposit, the problem is complicated because the associated granites are concealed and until now poorly known. The study of samples from a recent drill hole and a new gallery allowed a new approach of the Panasqueira granite system. Detailed petrographic, mineralogical, and geochemical studies were conducted, involving bulk major and trace analyses, BSE and CL imaging, EPMA, and SEM-EDS analyses of minerals. The apical part of the Pansqueira pluton consisted of a layered sequence of separate granite pulses, strongly affected by polyphase alteration. The use of pertinent geochemical diagrams (major and trace elements) facilitated the discrimination of magmatic and alteration trends. The studied samples were representative of a magmatic suite of the high-phosphorus peraluminous rare-metal granite type. The less fractionated members were porphyritic protolithionite granites (G1), the more evolved member was an albite-Li-muscovite rare metal granite (G4). Granites showed three types of alteration processes. Early muscovitisation (Ms0) affected the protolithionite in G1. Intense silicification affected the upper G4 cupola. Late muscovitisation (Fe–Li–Ms1) was pervasive in all facies, more intense in the G4 cupola, where quartz replacement yielded quartz-muscovite (pseudo-greisen) and muscovite only (episyenite) rocks. These alterations were prone to yield rare metals to the coeval quartz-wolframite veins.