# Cld-St-And-Bearing Assemblages in the Central Southalpine Basement: Markers of an Evolving Thermal Regime during Variscan Convergence

Marco Filippi, Maria Iole Spalla, Nicola Pigazzini, Valeria Diella, Jean-Marc Lardeaux, Davide Zanoni

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Marco Filippi, Maria Iole Spalla, Nicola Pigazzini, Valeria Diella, Jean-Marc Lardeaux, et al., Cld-St-And-Bearing Assemblages in the Central Southalpine Basement: Markers of an Evolving Thermal Regime during Variscan Convergence. Minerals, 2021, 11 (10), pp.1124. 10.3390/min11101124 hal-03578562

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# Cld-St-And-Bearing Assemblages in the Central Southalpine Basement: Markers of an Evolving Thermal Regime during Variscan Convergence

Marco Filippi <fnref n="1" />,<fnref n="2" />,*, Maria Iole Spalla <fnref n="1" /> ID, Nicola Pigazzini <fnref n="1" />, Valeria Diella <fnref n="3" /> ID, Jean-Marc Lardeaux <fnref n="2" />,<fnref n="4" /> and Davide Zanoni <fnref n="1" />

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**Citation:** Filippi, M.; Spalla, M.I.; Pigazzini, N.; Diella, V.; Lardeaux, J.-M.; Zanoni, D. Cld-St-And-Bearing Assemblages in the Central Southalpine Basement: Markers of an Evolving Thermal Regime during Variscan Convergence. *Minerals* **2021**, *11*, 1124. https://doi.org/10.3390/min11101124

Academic Editor: José Francisco Molina

Received: 24 August 2021
Accepted: 7 October 2021
Published: 13 October 2021

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**Copyright:** © 2021 by the authors. Licensee MDPI, Basel, Switzerland. This article is an open access article distributed under the terms and conditions of the Creative Commons Attribution (CC BY) license (https://creativecommons.org/licenses/by/4.0/).

**Abstract:** Multiscale structural analysis is carried out to explore the sequence of superposed pre-Alpine chloritoid-staurolite-andalusite metamorphic assemblages in the polydeformed Variscan basement of the upper Val Camonica, in the central Southalpine domain. The dominant fabric in the upper Val Camonica basement is the late-Variscan S2 foliation, marked by greenschist facies minerals and truncated by the base of Permian siliciclastic sequences. The intersection with the sedimentary strata defines a Permian age limit on the pre-Alpine tectono-metamorphic evolution and exhumation of the Variscan basement. The detailed structural survey revealed that the older S1 foliation was locally preserved in low-strained domains. S1 is a composite fabric resulting from combining S1a and S1b: in the metapelites, S1a was supported by chloritoid, garnet, and biotite and developed before S1b, which was marked by staurolite, garnet, and biotite. S1a and S1b developed at intermediate pressure amphibolite facies conditions during the Variscan convergence, S1a at T = 520–550 °C and P ≃ 0.8 GPa, S1b at T = 550–650 °C and P = 0.4–0.7 GPa. The special feature of the upper Val Camonica metapelites is andalusite, which formed between the late D1b and early D2 tectonic events. Andalusite developed at T = 520–580 °C and P = 0.2–0.4 GPa in pre-Permian times, after the peak of the Variscan collision and before the exhumation of the Variscan basement and the subsequent deposition of the Permian covers. It follows that the upper Val Camonica andalusite has a different age and tectonic significance as compared to that of other pre-Alpine andalusite occurrences in the Alps, where andalusite mostly developed during exhumation of high-temperature basement rocks in Permian–Triassic times.

**Keywords:** Variscan subduction/collision; pre-Alpine andalusite; chloritoid-staurolite metapelites

## 1. Introduction

Andalusite is an indicator of high thermal regimes, such as those characterizing contact metamorphism or regional Buchan/Abukuma-type metamorphism in the metapelites of the continental crust [1,2]. High T/P ratios accountable for andalusite development are envisaged in various convergent and divergent settings, including late-orogenic thinning and lithospheric delamination in the mature stages of continental collision, as well as lithospheric thinning announcing continental rifting in post-orogenic settings [3,4].

Andalusite is quite common in the pre-Alpine continental crust of the Alps, even if the age of the andalusite-bearing assemblages and the geological context in which they formed are various (Figure 1, Table 1). Andalusite-bearing rocks are associated with late-Variscan aplites, pegmatites, granitoids, and cordierite-bearing migmatites in the Helvetic

<footnote n="1">¹ Dipartimento di Scienze della Terra “A. Desio”, Università degli Studi di Milano, 20133 Milano, Italy; iole.spalla@unimi.it (M.I.S.); n.pigazzini@arpalombardia.it (N.P.); davide.zanoni@unimi.it (D.Z.)</footnote>

<footnote n="2">² UMR Géoazur, Observatoire de la Côte d'Azur, CNRS, IRD, Université Côte d'Azur, 06560 Valbonne, France; lardeaux@unice.fr</footnote>

<footnote n="3">³ Instituto di Geologia Ambientale e Geoingegneria (IGAG), Sezione di Milano, Consiglio Nazionale delle Ricerche, 20133 Milano, Italy; valeria.diella@cnr.it</footnote>

<footnote n="4">⁴ Centre for Lithospheric Research, Czech Geological Survey, 118 21 Prague, Czech Republic</footnote>

<footnote>* Correspondence: marco.filippi@unimi.it</footnote>
Argentera-Mercantour and Aiguilles Rouges massifs and often found in the contact zone of the Permian-Carboniferous intrusives [5-8]. Similarly, andalusite relics are found in the surroundings of late-Variscan granitoids in the Penninic Gran Paradiso massif [9] and in the pre-Permian metapelites of the Grand St. Bernard [10,11]. In the Penninic Briançon Basement, andalusite is instead related to a Permian thermal rise [12,13].

Different geological and chronological settings for andalusite development are envisaged in the Austroalpine and Southalpine domains, where andalusite-bearing assemblages testifying to Permian-Triassic lithospheric thinning are described together with older Permian-Carboniferous andalusite in the contact zone of late-Variscan intrusives [14-49]. In the Southalpine domain, andalusite mostly occurs in high-temperature basement rocks that include sillimanite, cordierite, and/or spinel that reflect Permian-Triassic Buchan/Abukuma-type metamorphism. In the upper Val Camonica, andalusite is instead found in chloritoid-staurolite-garnet-bearing metapelites, which suggest higher P/T conditions as characteristic of Barrovian/Dalradian metamorphism [1,2]. This case study thus represents an excellent opportunity to improve our understanding of the Variscan basement exhumation path, from the Variscan convergence to the Permian-Triassic lithospheric thinning. To this purpose, we present new multiscale structural data integrated with a detailed mineral-chemical and petrologic analysis, including thermodynamic modeling, aimed at identifying the geodynamic significance of the chloritoid-staurolite-andalusite transition in the upper Val Camonica basement.

<figure><img src="image_4.png" /><figcaption>**Figure 1.** Tectonic map of the Alps redrawn after [50]. The red stars locate andalusite-bearing metapelites in the pre-Alpine basements; the orange star refers to the andalusite described in this work. Keys are coded in Table 1, where assemblages, inferred P-T conditions, and ages are listed with references. The grey shaded area locates the tectonic scheme of the central Southalpine domain proposed in Figure 2.</figcaption></figure>
<table><caption>**Table 1.** Pre-Alpine andalusite-bearing assemblages in the continental crust of the Alps. Labels correspond to those of Figure 1. Mineral abbreviations follow [51]. When the radiometric method is not specified, the age is deduced from geological evidence or represents the average of results by different methods.</caption><thead><tr><th>Tectonic System</th><th>Key</th><th>Location</th><th>Assemblage</th><th>T (°C)</th><th>P (GPa)</th><th>Age (Ma)</th><th>Method</th><th>Refs.</th></tr></thead><tbody><tr><td>Helvetic—<br>Dauphinois—<br>Provençal</td><td>HDP 1</td><td>Argentera Massif<br>Gesso Valley</td><td>And + Bt ± Sil<br>± Pl</td><td>-</td><td>-</td><td>292 ± 10, 299–296</td><td>Rb/Sr,<br>Ar/Ar</td><td>[5,6,8]</td></tr><tr><td>Helvetic—<br>Dauphinois—<br>Provençal</td><td>HDP 2</td><td>Aiugilles Rouges<br>Mieville</td><td>And + Ms +<br>Tur ± Tpz ±<br>Crd</td><td>-</td><td>-</td><td>Carboniferous–<br>Permian</td><td>-</td><td>[7]</td></tr><tr><td>Penninic</td><td>P1</td><td>Gran Paradiso<br>Pian Teleccio</td><td>Bt, Sil, Crn, Qz,<br>Kfs, Pl, And?</td><td>-</td><td>-</td><td>Carboniferous–<br>Permian</td><td>-</td><td>[9]</td></tr><tr><td>Penninic</td><td>P2</td><td>Briançon<br>basement</td><td>And</td><td>450–550</td><td>0.1–0.3</td><td>Permian–Triassic<br>(295–245)</td><td>Rb/Sr,<br>K/Ar</td><td>[12,13]</td></tr><tr><td>Penninic</td><td>P3</td><td>Briançon<br>Basement Mont<br>Mort</td><td>Grt + Bt +<br>Sil/And</td><td>550–600</td><td>0.5–0.8</td><td>332–328</td><td>U/Pb</td><td>[10,11]</td></tr><tr><td>Austroalpine</td><td>A1</td><td>Mont Mary<br>Nappe</td><td>And + Ms</td><td>-</td><td>-</td><td>Permian</td><td>-</td><td>[23,28]</td></tr><tr><td>Austroalpine</td><td>A2</td><td>Silvretta<br>Pischahorn</td><td>Qz + Ms + And</td><td>600</td><td>0.2</td><td>353–280, 353–295</td><td>Rb/Sr,<br>K/Ar</td><td>[31]</td></tr><tr><td>Austroalpine</td><td>A3</td><td>Languard–<br>Campo<br>Sondalo</td><td>And + Crd</td><td>540</td><td>0.3–0.4</td><td>290–260</td><td>U/Pb</td><td>[39,46,47]</td></tr><tr><td>Austroalpine</td><td>A4</td><td>Languard–<br>Campo</td><td>And + Ms</td><td>&lt;500</td><td>&lt;0.5</td><td>&lt;250</td><td>U/Pb</td><td>[38,41,43,48]</td></tr><tr><td>Austroalpine</td><td>A5</td><td>Matsch Nappe</td><td>Grt + Sil/And<br>+ Bt ± Crd + Pl<br>+ Qz</td><td>570–640</td><td>0.30–0.55</td><td>Permian</td><td>Rb/Sr,<br>U/Pb,<br>Sm/Nd</td><td>[15,17,18]</td></tr><tr><td>Austroalpine</td><td>A6</td><td>Jenig Complex</td><td>And + Bt + Ms<br>+ Chl + Qz</td><td>450–530</td><td>0.24–0.42</td><td>254 ± 8</td><td>Sm/Nd</td><td>[19,20,37]</td></tr><tr><td>Austroalpine</td><td>A7</td><td>Kreuzeck<br>Strieden<br>Complex</td><td>And + Bt + Qz<br>± Pl ± Ms</td><td>500–570</td><td>&lt;0.35</td><td>230–200</td><td>Ar/Ar</td><td>[24,37,40]</td></tr><tr><td>Austroalpine</td><td>A8</td><td>Deferegger Alps<br>Uttenheim</td><td>And + Qz</td><td>-</td><td>-</td><td>&gt;260, &gt;290</td><td>Rb/Sr,<br>Ar/Ar</td><td>[21,37]</td></tr><tr><td>Austroalpine</td><td>A9</td><td>Rappold<br>Complex</td><td>(ex-) And</td><td>-</td><td>-</td><td>288 ± 4, 262 ± 2</td><td>Sm/Nd</td><td>[37,40]</td></tr><tr><td>Austroalpine</td><td>A10</td><td>Koralpe</td><td>(ex-) And</td><td>-</td><td>-</td><td>Permian–Triassic</td><td>-</td><td>[37,40]</td></tr><tr><td>Austroalpine</td><td>A11</td><td>Stralleg</td><td>And + Bt + Qz<br>± Pl ± Ms</td><td>550–600</td><td>0.32–0.48</td><td>Permian–Triassic</td><td>-</td><td>[37,40]</td></tr><tr><td>Austroalpine</td><td>A12</td><td>Sieggraben</td><td>(ex-) And</td><td>-</td><td>-</td><td>Permian–Triassic</td><td>-</td><td>[14,37,40]</td></tr><tr><td>Austroalpine</td><td>A13</td><td>Grobgneiss—<br>Sopron</td><td>And + Bt ± Spl<br>± Ilm</td><td>575–620</td><td>0.18–0.25</td><td>330–320</td><td>K/Ar</td><td>[29,30,37,40]</td></tr><tr><td>Southalpine</td><td>S1</td><td>Strona–Ceneri<br>Zone</td><td>Sill, And, Crd</td><td>-</td><td>-</td><td>Permian</td><td>-</td><td>[32,35]</td></tr><tr><td>Southalpine</td><td>S2</td><td>Dervio–Olgiasca<br>Zone</td><td>And</td><td>&lt; 600</td><td>&lt;0.3</td><td>Triassic</td><td>-</td><td>[25,27,34,41,<br>45]</td></tr><tr><td>Southalpine</td><td>S3</td><td>Val Biandino</td><td>And + Crd</td><td>500–600</td><td>&lt;0.35</td><td>312 ± 48, 286 ± 20</td><td>Rb/Sr,<br>K/Ar</td><td>[22,26,49]</td></tr><tr><td>Southalpine</td><td>S4</td><td>Val Camonica</td><td>And + Bt + Qz<br>± St</td><td>-</td><td>-</td><td>pre-Permian</td><td>-</td><td>[36], this work</td></tr><tr><td>Southalpine</td><td>S5</td><td>Isarco Valley</td><td>And + Bt + Crd</td><td>&lt;670</td><td>0.25–0.35</td><td>282 ± 14</td><td>Rb/Sr</td><td>[16,33,42,44]</td></tr></tbody></table>
## 2. Geological Setting

The Variscan basement of the central Southalpine domain (i.e., the Orobic basement) comprises metapelites, gneisses, and quartzites, with minor metagranitoids, amphibolites, and marbles ([41,49,52–54] and refs. therein). The protoliths of these rocks mostly derive from Silurian–Ordovician sedimentary sequences and intrusives [55–57].

The dominant S2 foliation in the basement rocks is supported by greenschist facies minerals, which developed mainly during the late-collisional exhumation of the Variscan basement (>280 Ma, [49] and refs. therein), with few exceptions (e.g., [58,59] and refs. therein). S2 is truncated by siliciclastic Permian sequences, including conglomerates, arenites, and volcaniclastites, which are divided by unconformity in two cycles, dated lower- and mid-upper Permian, respectively [54,60–62]. The basement and sedimentary rocks were subsequently deformed and poorly metamorphosed during Alpine convergence (e.g., [63–65]), which was responsible for the development of D3 and D4 structures [56,66–69].

Mineral assemblages supporting precollisional and collisional Variscan structures (D1a, and D1b) are occasionally preserved in the Orobic basement, where five pre-Alpine Tectono–Metamorphic Units (TMUs) are distinguished [45,58] and shown in Figure 2:

1. the Val Vedello (VVB) and Monte Muggio Basements (MMB), in which kyanite-staurolite-bearing metapelites record the metamorphic peak of the Variscan collision under amphibolite facies conditions [25,53,70];

2. the Passo CavalcAfiche Basement (PCB) and Domaso–Cortafò Zone (DCZ), which record a prograde metamorphic evolution: syn-D1a chloritoid–garnet-bearing assemblages in metapelites testify to precollisional piling of cold lithospheric sheets under epidote–amphibolite facies conditions [71], whereas Syn-D1b staurolite–garnet-bearing assemblages formed during the subsequent Variscan collision [71];

3. the Aprica Basement (AB), which records two stages of the Variscan tectono–metamorphic evolution both under greenschist facies conditions, but marked by different P/T ratios [68]. A similar tectono–metamorphic evolution is also recorded in a small segment of Variscan basement immediately north of the Alpine Sellero line [55,58,72];

4. the Dervio–Olgiasca Zone (DOZ), which is the only TMU that records the high thermal state relatable to the “Tethyan rifting” at intermediate crustal depth [25,27]. Andalusite replacing sillimanite testifies to exhumation under high T/P ratio [25,52,73,74]. The Triassic age of this event is constrained by syn-D2 pegmatite ages [25,34,70,75];

5. the Tre Valli Bresciane (TVB) massif, where peak epidote–amphibolite facies conditions are recorded by chloritoid–garnet-bearing assemblages in metapelites [72,76].

In addition, P-T trajectories obtained from metamorphic pebbles from conglomerates of the lower Permian sedimentary cycle have been compared with the P-T evolutions inferred in different units of the Variscan basement [49,72,77]. In particular, metamorphic conditions retained by staurolite–garnet-bearing pebbles of basement rocks in the Aga and Vedello Conglomerates (AVC) (Figure 2) are similar to those characterizing the neighboring VVB and AB [77]. In the same way, metamorphic conditions retained by garnet–chloritoid-bearing pebbles in the Dosso dei Galli Conglomerate (DGC) (Figure 2) match those of the closest TVB [72].

In the siliciclastic Ponteranica Formation (POC, Figure 2), two types of pebbles are distinguished: the first type is similar to those found in the Aga and Vedello conglomerates, whereas, the second type contains andalusite-bearing assemblages interpreted either as developed during late-Variscan contact metamorphism, as induced by the emplacement of Val Biandino pluton, or during late-orogenic thermal relaxation [49].
<figure><img src="image_5.png" /></figure>

**Figure 2.** Geologic sketch of the central Southalpine domain modified from [49] and refs. therein. The present study area is shown as a black polygon indicated by a black arrow (cfr. Figure 3). Variscan Tectono-Metamorphic Units: AB = Aprica Basement; DCZ = Domaso—Cortafò Zone; DOZ = Dervio—Olgiasca Zone; MMZ = Monte Muggio Zone; PCB = Passo Cavalcafiche Basement; TVB = Tre Valli Bresciane massif; VVB = Val Vedello Basement. Permian conglomerates with pebbles deriving from the Variscan TMUs: POC = Ponteranica Formation; AVC = Aga and Vedello Conglomerates; DGC = Dosso dei Galli Conglomerate. Main tectonic lines: GSL = Gallinera e Sellero Lines; ML = Musso Line; OL = Orobic Line; VGL = Val Grande Line. Inset with the tectonic sketch of the Alps after [78]. A = Variscan basement rocks in the Alpine subduction complex; B = Variscan basement rocks in the Alpine external domains (Ag: Aar-Gotthard Massif, Ar: Argentera-Mercantour Massif, Bd: Belledonne Massif, Mb: Mont Blanc Massif, Px: Pelvoux Massif, wSa: western Southern Alps, cSa: central Southern Alps, eSa: eastern Southern Alps); C = Variscan basement rocks external to the Alpine fronts (Mt: Maures-Tanneron Massif, Vs: Vosges); D = lithospheric-scale structures delimiting the axial zone of the Alps (Pf: Penninic Front, Pl: Periadriatic Lineament); E: Alpine fronts.

The mid-upper Permian Verrucano Lombardo is part of the second sedimentary cycle capping most of the Orobic basement; it consists of poorly stratified fluvial conglomerates and sandstones ([62] and refs. therein) that grade into shallow sea deposits (Servino Formation) in early Triassic times [79]. This contribution focuses on a segment of the Orobic basement just below the Gallinera Line footwall (Figure 2), in upper Val Camonica. Here, the Verrucano Lombardo formation truncates late-collisional S2 in the exhumed Variscan basement.

**3. Lithostratigraphy and Deformation History**

Structural mapping was carried out on the right sloping bank of the Oglio river in upper Val Camonica, west of Cedegolo and Sellero villages (Figure 3). The aim was to constrain the intersection relationship between different types of pre-D2 structures in the Variscan basement. The Sellero-Cedegolo Basement, hereafter named SCB, mostly consists of chloritoid-staurolite-bearing metapelites, with minor lenses of garnet-bearing metagranitoids, paragneisses, and amphibolites, and is capped by the mid-upper Permian
Verrucano Lombardo. The relevance of this area in the Orobic basement is the outstanding occurrence of pre-Permian andalusite in the metapelites (Figure 3).

Four generations of superposed structures are distinguished in the SCB. In the metapelites, S2 foliation is supported by white mica, chlorite, ±albite (Figure 4). S2 dips from northwest to southeast, due to successive Alpine folding and thrusting (D3). Alpine D3 folds are characterized by southwest trending axes and steeply dipping axial planes (Figure 5).

Pre-D2 foliations, S1a and S1b, are occasionally preserved in the area, even if mostly transposed into S2 (Figure 5). S1a is supported by white mica, garnet, biotite, and ± chloritoid, and S1b is supported by white mica, garnet, biotite, and ± staurolite (Figure 4). Overprinting relationships between S1a and S1b were not observed at the outcrop scale. On the basis of chloritoid or staurolite, S1 is demarcated as S1a or S1b, respectively. Where both intersection relationships and contrasting assemblages are absent, pre-D2 fabrics have been simply labeled S1.

<figure><img src="image_6.png" /><figcaption>**Figure 3.** Interpretative structural map of the area west of Cedegolo and Sellero villages in the upper Val Camonica (location in Figure 2). Orientations of fabric elements synthesized in this foliation trajectory map are analytically shown in Figure 5. Urban areas are bounded by grey polygons.</figcaption></figure>
<figure><img src="image_7.png" /></figure>

**Figure 4.** Mesoscale representative structures and mineral assemblages in the Sellero-Cedegolo basement. Metapelites: (A) Alpine D3 folding overprints Variscan S2 foliation marked by greenschist facies minerals. D3 axial plane dips to NW; (B) overprinting relationships between S1 and S2. S2 dips to S; (C) garnet (Grt) and chloritoid (Cld) grains supporting S1a foliation; (D) aggregates of staurolite (St) grains lying with garnet (Grt) on S1b foliation. Metagranitoids: (E) mylonitic S2 marked by chlorite and white mica. The red line is the lens lanyard, here used as scale.

In the metagranitoids, K-feldspar relics were wrapped by two superposed foliations: S1 was supported by biotite, white mica, plagioclase, and quartz and wraps rare garnet porphyroclasts. New white mica, chlorite, and rare plagioclase grains marked pervasive S2 (Figure 4E). Metric lenses of amphibolites were hosted within the staurolite-bearing metapelites in the northern part of the area (Figure 3). In the amphibolites, pervasive S2 was supported by amphibole, chlorite, quartz, epidote, and plagioclase; relict S1 was supported by amphibole, epidote, and biotite. Rare garnet porphyroclasts were found in the amphibolites.

The mid-upper Permian Verrucano Lombardo Formation unconformably covers the basement rocks and cuts S2 at the western boundary of the mapped area (Figure 3). D3 folds affect the basement rocks together with the Permian-Mesozoic sedimentary sequences. In both Variscan basement rocks and covers, D3 folds were characterized by a disjunctive axial plane foliation S3. S3 was marked by chlorite, white mica, and opaque minerals.
<figure><img src="image_8.png" /><figcaption>**Figure 5.** Schmidt stereographic projections (equal-area, lower hemisphere) of structural data, including Variscan (S1, S2) and Alpine (S3) poles to foliations, Variscan (A2) and Alpine (A3) fold axes and axial planes (AP3), and Permian sedimentary bedding (SL). Data are distinguished on relative chronology. Dotted lines and poles represent cylindrical best fits.</figcaption></figure>

**4. Microstructure and Mineral Chemistry**

Deformation versus mineral growth relationships were determined for metapelites and metagranitoids that well preserved pre-D2 structures (Figure 6). The aim is to investigate the relationships between mineral growth and superposed fabrics and infer a robust P–T–d–t (Pressure–Temperature–deformation–time) path. The above described and regionally valid deformation history has been useful to individuate the site for investigating mineral compositional variations, taking into account: (a) the timing of mineral growth with respect to superposed fabric elements and (b) deformation mechanisms acting during the same deformation stage (e.g., [80–82]).

Mineral chemical analyses and backscattered electron (BSE) images were performed with the JEOL JXA-8200 electron microprobe in wavelength dispersion mode (EMPA) at the laboratory of the Department of Earth Sciences of the University of Milan, Italy, under the following conditions: 15 kV accelerating voltage, 5 nA beam current, and a count time of 60 s on peak and 30 s on the background, with a 1 µm diameter beam. Natural minerals were used as standards and the rough data corrected for matrix effects using a conventional φφZ routine in the JEOL software. Compositional parameters of the analyzed minerals in metapelites and metagranitoids are reported in Table 2. The mineral chemical dataset is attached in Table S1 (Supplementary Materials).

4.1. *Metapelites*

S1a and S1b are well preserved in the selected metapelites. S1a is supported by shape-
preferred orientation (SPO) of white mica (WmI, Si > 6.20 apfu), chloritoid (X<sub>Mg</sub> = 0.04–0.11),
biotite (BtI, X<sub>Mg</sub> = 0.19–0.29), quartz, rutile, and ilmenite. These minerals, with rare grains
of plagioclase (PlI, An<sub>4–5</sub>), mark the internal foliation of millimeter- to centimeter-sized gar-
net porphyroblasts (GrtI, Alm<sub>81</sub>Grs<sub>14</sub>Prp<sub>5</sub>). Inclusion patterns in GrtI are usually straight,
slightly curved at garnet rims, and continuous with the external S1a foliation. Similarly,
millimeter-sized chloritoid grains included S1a as internal foliation (Figure 7A).
<figure><img src="image_9.png" /><figcaption>**Figure 6.** Deformations stages versus mineral growth in metapelites (A) and metagranitoids (B). Mineral abbreviations are from [51].</figcaption></figure>

S1a is crenulated by D1b and, where S1b is well developed, decussate and plastically deformed WmI and BtI crystals are preserved in microlithons and/or as rotated grains in the cleavage domains. GrtI cores contain internal S1a, discordant with external S1b (Figure 7B), and show thin inclusion-free rims (GrtII, Alm<sub>89</sub>Grs<sub>6</sub>Prp<sub>4</sub>). S1b is marked by white mica (WmII, $6.10 \le Si \le 6.20$ apfu with Pg < 0.20), staurolite ($X_{Mg} = 0.06-0.15$), biotite (BtII, $X_{Mg} = 0.30-0.40$), and ilmenite; quartz and plagioclase (PlII, $An_{21-22}$) occupy the microlithons. Skeletal GrtII grains are in trails along S1b together with staurolite. Overprinting of staurolite-bearing S1b on chloritoid-bearing S1a is exceptionally preserved (Figure 7A); in addition, staurolite includes S1b foliation deflected into strain caps around GrtI porphyroclasts (Figure 7B), or it fills the necks of microboudinaged chloritoid grains (Figure 7C).

S1b is crenulated by D2 or microfaulted along localized shear bands. S2 is outlined by chlorite, white mica (WmIII, Si = 5.91–5.94 apfu, Pg = 0.09–0.10), ilmenite, tourmaline, and rare biotite (BtIII). Plastically deformed grains of biotite and white mica were re-oriented along S2. Centimeter-sized plagioclase crystals (PlII, $An_{1-3}$) retain S2 as internal foliation. Plagioclase porphyroclasts are statically replaced by epidote and sericite, whereas chlorite overgrew garnet, chloritoid, and staurolite.

Andalusite crystals of millimeter to centimeter size include S1b as internal foliation, either straight, curved, or gently folded by D2 (Figure 7D,E), but continuous with external S1b. Andalusite was microboudinaged during D2, with WmIII, BtIII, and chlorite filling the boudin necks, and wrapped by coronae of very fine-grained WmIII. These features suggest that andalusite growth took place during the final stages of S1b development and ceased during early-D2. Staurolite inclusions are recurrent in andalusite grains and display sharp grain boundaries (Figure 7F). Andalusite locally forms aggregates with small corundum grains. In most cases, corundum is rimmed by diaspore (Figure 7G,H).

The following mineral compositional evolutions are here summarized and highlighted in Figure 8 and Table 2: (1) replacement of Ca by $Fe^{2+}$ from GrtI to GrtII; (2) decrease in Si and Mg + Fe content from WmI to WmII to WmIII; (3) increase in $X_{Mg}$ from BtI to BtII; (4) increase in An component from PlI to PlII and decreasing from PlII to PlIII. Chlorite composition seems to be controlled by the microstructural site: chlorite replacing andalusite and staurolite has $X_{Mg} = 0.34-0.36$, chlorite replacing chloritoid has $X_{Mg} = 0.17-0.29$, chlorite rimming garnet shows $X_{Mg} = 0.09-0.37$ and the lowest Al content (Figure 8).
<figure><img src="image_10.png" /><figcaption>**Figure 7.** Variscan metapelites. (A) S1a supported by shape-preferred orientation of millimeter-sized chloritoid porphyroblasts (BSE image). Internal foliation in chloritoid is continuous with external S1a. S1b is supported by submillimeter sized staurolite grains and cuts S1a. (B) Porphyroclast of GrtI wrapped by S1b. S1b is marked by WmII and BtII. GrtI retains a straight internal foliation discontinuous with the external one. Staurolite in the strain caps around GrtI encloses deflected S1b (PPL image). (C) S1a supported by chloritoid. Chloritoid is included in GrtI, and the internal foliation in both GrtI and chloritoid is deflected but continuous with the external foliation S1a. Chloritoid grains are boudinaged and staurolite grew in the boudin-neck (PPL image). (D) Andalusite with internal foliation continuous with external S1b: the internal foliation is straight at the grain core and curved at the rim. S1b is marked by BtII. Decussate grains of biotite are preserved in cleavage domains and as inclusions in andalusite (PPL image). (E) Post-kinematic andalusite porphyroblast overprints D2 folds (PPL image). (F) Andalusite porphyroblast includes staurolite with equilibrium grain boundaries (PPL image). (G,H) Andalusite porphyroblasts include corundum grains and are replaced by diaspore and WmIII (BSE and XPL images).</figcaption></figure>
<figure><img src="image_11.png" /><figcaption>**Figure 8.** Compositional variations of the main rock-forming minerals in metapelites and meta-granitoids as a function of rock-type (triangle: garnet-bearing metapelites, circle: chloritoid-bearing metapelites, square: staurolite-bearing metapelites) and microstructural site (D1a—blue, D1b—yellow, D2—red).</figcaption></figure>

## 4.2. *Metagranitoids*

S2 is the dominant foliation in metagranitoids. S1a and S1b are locally preserved in low strained domains and wrap relics of igneous K-feldspar. S1b is supported by biotite (BtII, $X_{Mg}$ = 0.33, Ti < 0.21 apfu), quartz, plagioclase (PIII, $An_{2-6}$), minor white mica (WmII, Si = 6.20–6.47 apfu, Pg < 0.12), and ilmenite. S1a is the internal foliation in skeletal garnet grains ($Alm_{51}Grs_{31}Prp_{3}Sps_{16}$) and is supported by elongated inclusions of quartz. In the garnet porphyryclasts, S1a is discontinuous with respect to the external foliation S1b. Decussate grains of biotite (BtI, $X_{Mg}$ = 0.30–0.34, Ti = 0.28–0.38 apfu) and white mica (WmI, Si = 6.11–6.27 apfu, Pg < 0.11) were found in the microlithons, with an early generation of plagioclase (PII, $An_{13-42}$) that is extensively replaced by white mica and epidote ($Fe^{3+}$/$Al^{VI}$ + $Fe^{3+}$) = 0.16–0.17). BtI, WmI, PII, garnet, and quartz are considered stable during S1a development. Finally, S2 is supported by white mica, ilmenite, and chlorite ($X_{Mg}$ = 0.36–0.40), which pervasively replace biotite and garnet.
<table><caption>**Table 2.** Synthesis of mineral chemical analyses. Stoichiometric formulae are calculated as follows: garnet at 8 cations and 12 oxygen atoms, epidote at 8 cations and 12.5 oxygen atoms, biotite and white mica at 22 oxygen atoms, chloritoid at 12 oxygen atoms, staurolite at 46 oxygen atoms, chlorite at 7 oxygen atoms, and plagioclase at 4 oxygen atoms. Average values are in brackets.</caption><thead><tr><th>Rock Type</th><th>Stage</th><th>Mineral</th><th>Alm</th><th>Prp</th><th>Grs</th><th>Si</th><th>Al</th><th>Pg</th><th>Fe + Mg</th><th>Ti</th><th>X<sub>Mg</sub></th><th>An</th><th>Ab</th></tr></thead><tbody><tr><td rowspan="10">Metapelites</td><td rowspan="5">D1a</td><td>Grt I</td><td>0.75–0.90<br>(0.81)</td><td>0.01–0.10<br>(0.05)</td><td>0.05–0.20<br>(0.14)</td><td></td><td>6.21–6.38</td><td>5.39–5.72</td><td>0.03–0.20</td><td>0.13–0.43</td><td></td><td>0.17–0.25</td><td>0.19–0.29</td><td>4–5</td><td>94–96</td></tr><tr><td>Wm I</td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td></tr><tr><td>Bt I</td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td></tr><tr><td>Pl I</td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td></tr><tr><td>Cld</td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td></tr><tr><td rowspan="5">D1b</td><td>Grt II</td><td>0.86–0.94<br>(0.89)</td><td>0.02–0.10<br>(0.06)</td><td>0.02–0.07<br>(0.04)</td><td></td><td>6.10–6.20</td><td>5.67–5.90</td><td>0.08–0.28</td><td>0.07–0.23</td><td></td><td>0.10–0.23</td><td>0.30–0.40</td><td>21–22</td><td>77–78</td></tr><tr><td>Wm II</td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td></tr><tr><td>Bt II</td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td></tr><tr><td>Pl II</td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td></tr><tr><td>St</td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td></tr><tr><td rowspan="10">Meta-granitoids</td><td rowspan="5">D2</td><td>Wm III</td><td></td><td></td><td></td><td></td><td>5.91–5.94</td><td>5.95–6.02</td><td>0.09–0.10</td><td>0.05–0.06</td><td></td><td></td><td></td><td>1–3</td><td>97–98</td></tr><tr><td>Pl III</td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td></tr><tr><td>Chl (And)</td><td></td><td></td><td></td><td></td><td>2.44–2.53</td><td>2.98–3.18</td><td></td><td></td><td></td><td></td><td>0.36–0.38</td><td></td><td></td></tr><tr><td>Chl (Cld)</td><td></td><td></td><td></td><td></td><td>2.53–2.69</td><td>2.90–3.11</td><td></td><td></td><td></td><td></td><td>0.17–0.29</td><td></td><td></td></tr><tr><td>Chl (Grt)</td><td></td><td></td><td></td><td></td><td>2.44–3.01</td><td>2.44–3.05</td><td></td><td></td><td></td><td></td><td>0.09–0.37</td><td></td><td></td></tr><tr><td>Chl (St)</td><td></td><td></td><td></td><td></td><td>2.49–2.64</td><td>2.93–3.05</td><td></td><td></td><td></td><td></td><td>0.34–0.46</td><td></td><td></td></tr><tr><td rowspan="5">D1a</td><td>Grt</td><td>0.58–0.62<br>(0.60)</td><td>0.03</td><td>0.35–0.39<br>(0.37)</td><td></td><td>6.11–6.27</td><td>5.22–5.38</td><td>0.08–0.11</td><td>0.34–0.48</td><td></td><td>0.28–0.38</td><td>0.30–0.34</td><td>13–42</td><td>56–86</td></tr><tr><td>Wm I</td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td></tr><tr><td>Bt I</td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td></tr><tr><td>Pl I</td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td><td></td></tr><tr><td>D1b</td><td>Wm II</td><td></td><td></td><td></td><td></td><td>6.20–6.47</td><td>4.88–5.42</td><td>0.08–0.12</td><td>0.33–0.69</td><td></td><td>0.21</td><td>0.33</td><td>2–6</td><td>92–97</td></tr></tbody></table>
**5. Metamorphic Evolution vs. Deformation History**

This section constrains the P-T conditions under which D1a, D1b, and D2 structures developed in the Variscan basement. The Permian sedimentary sequences overlying the SCB define a Permian age limit for the exhumation of the Variscan basement in upper Val Camonica.

Metamorphic conditions for the subsequent deformation stages recorded in the metapelites were estimated by means of thermobarometers and pseudosections. Temperatures were constrained using different Fe–Mg cationic exchange between mineral pairs in textural equilibrium. Chloritoid–biotite and chloritoid–garnet thermometry [83,84] was applied on mineral grains supporting S1a foliation and gave a temperature interval of 490–580 °C. Staurolite–garnet thermometry [80] on minerals marking S1b provided a temperature interval of 580–610 °C. The result was fully consistent with the upper stability of chloritoid in the FeO–Al₂O₃–SiO₂–H₂O (FASH) system, which reacted to form staurolite and/or almandine by increasing the temperature above 550 °C ([85] and refs. therein). Garnet–biotite thermometry [86–89] coherently indicated that S1a developed at T = 480–540 °C and S1b at T = 510–630 °C. Pressure conditions were estimated by garnet–plagioclase–biotite–muscovite–quartz [90] and garnet–plagioclase–muscovite–quartz barometers [91]: S1a developed at P = 0.8–1.0 GPa and S1b at P = 0.4–0.6 GPa.

Pseudosections were calculated by the Theriak/Domino program [92] to better constrain the P-T intervals accountable for D1a, D1b, and early D2 events in metapelites and metagranitoids (Figure 9). We adopted a converted version of the self-consistent thermodynamic database ds55 [93] in the CaO–Na₂O–K₂O–FeO–MgO–Al₂O₃–SiO₂–H₂O (CNKF-MASH) system, including the following mineral activity-composition (a-x) relations: garnet [94], biotite [94], chlorite [95], white mica [96], chloritoid [95], and staurolite [95].

The selected bulk compositions were acquired from metapelite and metagranitoid samples from the lithostratigraphic unit in the Orobic basement that included the rocks analyzed in this work [93]. Mn was excluded, because it is negligible in the metapelites and only fractionated in garnet in the metagranitoids; P content is almost entirely contained in apatite and thus removed from the system together with stoichiometric Ca. Water was considered in excess except where indicated.

In the metapelites, the syn-D1a assemblage plagioclase + garnet + biotite + white mica + chloritoid + quartz was stable at T = 530–560 °C and P = 0.6–0.8 GPa (Figure 9A). The resulting stability field was delimited at low temperature and high pressure by chlorite-in and chloritoid-out curves, at high temperature by chloritoid-out and staurolite-in (T = 560 °C) curves, and at low-pressure by garnet-out curves. Within the D1a field, the garnet composition changed from Alm₇₉Grs₁₆Prp₅ to Alm₈₇Grs₈Prp₅ under increasing of the T/P ratio. The Si content in white mica is 6.20 apfu and consistent with P ≃ 0.8 GPa. The computed compositions matched those of GrtI (Alm₈₁Grs₁₄Prp₅) and WmI (Si ≥ 6.20 apfu) in the metapelites for T = 530–550 °C and P ≃ 0.8 GPa.

The syn-D1b assemblage garnet + biotite + white mica + staurolite + quartz was stable at T = 560–650 °C and P = 0.5–0.7 GPa. The predicted stability field was delimited at high pressure by staurolite-out, at high temperature by univariant sillimanite-in/staurolite-out, and at low pressure by garnet-out. In this field, garnet is characterized by almandine content at around 0.90 and grossular at around 0.05, as in GrtII (Alm₈₉Grs₆Prp₄). This portion of the P-T space likely represents the main stage of S1b development, which was followed by further decompression and exhumation out of the garnet stability field, as suggested by the Si content in WmII (6.10 ≤ Si ≤ 6.20 apfu).

Andalusite was stable together with staurolite at T = 520–580 °C and P = 0.2–0.4 GPa (Figure 9B). These metamorphic conditions characterized the transition between D1b and D2 deformation stages. A further exhumation of metapelites towards shallower levels is testified to by the replacement of corundum by diaspore at T ≤ 400 °C and P ≤ 0.2 GPa [95].
<figure><img src="image_12.png" /><figcaption>**Figure 9.** P-T and P-X pseudosections calculated in the CNKFMASH system for metapelites (A,B) and metagranitoids (C,D) in the SCB. Bulk compositions are from [97]. Fields are colored as function of variance. Si-in white mica, Ca-in garnet, and Fe-in garnet isopleths are added. P-T accountable for D1a to D2 deformation stages are highlighted by dotted ellipses and lines.</figcaption></figure>

In the metagranitoids, the stability and composition of garnet was mostly controlled by the amount of water in the system (Figure 9C). Increasing water content, garnet was stable towards higher pressure at the same temperature. The analyzed garnet (Alm₆₀Grs₃₇Prp₃) was predicted in the Pl + Grt + Bt + Wm + Kfs + Qz field if considered in slightly undersaturated conditions (~3% mol of H₂O). The P-T conditions accountable for garnet development
vary from 450 °C and 0.65 GPa to 530 °C and 1.00 GPa (Figure 9D). In this wide P-T interval, biotite $X_Mg$ (0.30–0.38) matched with the analysis on Bt I (0.30–0.34) and the Si content in white mica (6.14–6.34 apfu) was comparable to that of Wm I (6.11–6.27 apfu). This modeling suggests that garnet stability in the metagranitoids is only possible at P-T conditions (T = 450–530 °C, P = 0.7–1.0 GPa), slightly cooler but comparable with those determined for D1a in the metapelites (T = 520–550 °C, P ≈ 0.8 GPa), and not during D1b, in agreement with the microstructural relationships.

**6. Discussion and Conclusions**

Multiscale structural analysis integrated with petrology in the SCB rocks allowed the reconstruction of the Variscan P–T–d–t evolution, predating the deposition of the Permian–Triassic sedimentary sequences (Figures 3 and 10, [54]). The Variscan structural evolution is testified by the superposition of three groups of structures developed under different metamorphic conditions: D1a structures formed at the boundary between epidote amphibolite- and amphibolite-facies conditions (at T = 450–570 °C and P = 0.7–1.0 GPa), D1b under amphibolite-facies conditions, at higher temperature and slightly lower pressure (T = 550–650 °C and P = 0.4–0.7 GPa), whereas D2 structures are marked by mineral assemblages testifying to the transition towards greenschist-facies conditions (T ≤ 400 °C and P ≤ 0.3 GPa). Overprinting relationships between chloritoid–garnet-bearing S1a and staurolite–garnet-bearing S1b confirmed that the development of the various mineral assemblages was controlled by different thermal states during successive deformation stages.

The textural relationship between staurolite and andalusite in some of the SCB rocks suggests local equilibrium between the two minerals. Andalusite–staurolite assemblages developed at T = 520–580 °C and P = 0.2–0.4 GPa, during the transition from late D1b to early D2 stages. This is in contrast with the textural relationships in metamorphic clasts of the Lower Permian Ponteranica Formation that shows andalusite replacing staurolite [49].

The thermal state obtained by the syn-D1a P-T conditions (Figure 10) was characterized by a T/depth ratio of 15–18 °C·km⁻¹ and plots between those of warm subduction zones, plate interior, and continental collision zones [98] and is compatible with tectonic piling of cold lithospheric sheets during the Variscan convergence, as already suggested in other portions of the Orobic basement and interpreted as an effect of the Variscan continental subduction and collision (e.g., PCB, DCZ, TVB [71,72]).

D1b structures developed under P-Tmax conditions indicated a T/depth ratio of 25–30 °C·km⁻¹ and suggested a thermal state compatible with that of plate interior [98]. This thermal state is compatible with those of the Variscan continental collision, in agreement with other tectono–metamorphic units in the Southalpine domain (e.g., VVB, MMB, PCB, and DCZ [25,49,53,59,68,70,71,77]).

Andalusite–staurolite-bearing assemblages developed under T/depth ratio comprised between 40 and 70 °C·km⁻¹ in between late-D1b and early-D2 indicate that a high thermal state was already effective at the end of the exhumation trajectory of the SCB rocks. The stratigraphic contact with the Verrucano Lombardo Formation in the area, and with lower Permian sequences few kilometers north of SCB, makes the greenschist-facies D2 structures older than Permian ([49,54] and refs. therein). Any relationship with the Permian–Triassic high thermal state that characterized the DOZ [25,52,73,74] is precluded since the SCB was already exhumed at that time. The identified high thermal state is thus interpreted as related to a Variscan late-orogenic thinning, associated with lithospheric delamination. This interpretation is supported by the predictions of 2D numerical models (Figure 10) performed for simulating a subduction and collision process, whose convergence rate is set by paleogeographic constraints on the Variscan belt [99–101].
<figure><img src="image_13.png" /></figure>

**Figure 10.** Comparison between the P-T path inferred for the SCB rocks (yellow line with arrow), metamorphic field gradients, and P-T predictions obtained during different stages of a 2D numerical model of Variscan convergence (subduction/post-collisional stages ([99] and refs. therein). Cross signs refer to the P-T conditions attained by the SCB rocks during D1a to D2 deformation stages. Dashed geotherms "Arcs, Ridges", "Plate Interior", "Warm Subduction Zones", and "Cold Subduction Zones" follow [98]. D1a, D1b, and D2 refer to the metamorphic conditions related to the successive groups of structures in SCB. Ages referred to D1b and D2 are inferred from radiometric and stratigraphic data ([49,62,102] and refs. therein).

The inferred evolution makes unique this portion of the Southalpine basement with respect to the other units, where the thermal record of the late-collisional evolution is instead registered at deeper crustal levels, as testified by sillimanite and/or cordierite with andalusite [42,44,49,103,104]. This contribution indicates that the high thermal regime affecting Southalpine basement rocks during pre-Alpine times may also result from late-Variscan orogenic collapse and not only by Permian–Triassic lithospheric thinning. The superimposition of such an elevated thermal state in the pre-Alpine basement suggests that the thermal softening of the continental lithosphere at the end of the Variscan convergence may have led to the localization of Permian–Triassic weakened zones in the Alpine area.

**Supplementary Materials:** The following are available online at https://www.mdpi.com/article/10.3390/min11101124/s1, Table S1: Mineral chemical analysis.

**Author Contributions:** Conceptualization, M.F. and M.I.S.; fieldwork and microstructure, M.F., N.P., M.I.S. and D.Z.; mineral chemistry, M.F., N.P., V.D. and M.I.S.; petrologic modeling, M.F. and J.-M.L.; visualization, M.F., M.I.S., V.D.; writing–original draft, M.F., M.I.S., V.D., J.-M.L. and D.Z. All authors have read and agreed to the published version of the manuscript.

**Funding:** This research was funded by GECT (CTE_INT16DZANO_M) and Università di Milano—Linea B (PSR2020_MRODA).

**Data Availability Statement:** Not Applicable.

**Acknowledgments:** We acknowledge Curzio Malinverno for thin section preparation and Andrea Risplendente for support with the electron microprobe. We thank G. Gosso and G.B. Siletto for fruitful discussion and suggestions. The authors acknowledge the editors and the insightful suggestions by the anonymous reviewers that improved the text.
**Conflicts of Interest:** The authors declare no conflict of interest.

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