Neolithic artefacts in ‘Jade’ from Rocca di Cavour (Northwestern-Italy): archaeometric characterization, geologic contextualization and provenance

Neolithic artefacts in ‘Jade’ from Rocca di Cavour (Northwestern-Italy): archaeometric characterization, geologic contextualization and provenance | Research Square window.SnipcartSettings = { analytics: { enabled: false } }; (function() { var accessVector = localStorage.getItem('access_vector') || ''; window.dataLayer = window.dataLayer || []; if (accessVector) { window.dataLayer.push({ user: { profile: { profileInfo: { snid: accessVector } } } }); } })(); (function(w,d,s,l,i){w[l]=w[l]||[];w[l].push({'gtm.start':new Date().getTime(),event:'gtm.js'});var f=d.getElementsByTagName(s)[0],j=d.createElement(s),dl=l!='dataLayer'?'&l='+l:'';j.async=true;j.src='https://www.googletagmanager.com/gtm.js?id='+i+dl;f.parentNode.insertBefore(j,f);})(window,document,'script','dataLayer','GTM-K279D39R'); Browse Preprints In Review Journals COVID-19 Preprints AJE Video Bytes Research Tools Research Promotion AJE Professional Editing AJE Rubriq About Preprint Platform In Review Editorial Policies Our Team Advisory Board Help Center Sign In Submit a Preprint Cite Share Download PDF Article Neolithic artefacts in ‘Jade’ from Rocca di Cavour (Northwestern-Italy): archaeometric characterization, geologic contextualization and provenance Roberto Giustetto, Michele Borgogno, Luca Barale, Ursula Perrone, and 1 more This is a preprint; it has not been peer reviewed by a journal. https://doi.org/ 10.21203/rs.3.rs-9051667/v1 This work is licensed under a CC BY 4.0 License Status: Under Revision Version 1 posted 11 You are reading this latest preprint version Abstract Artefacts in presumed ‘ jade ’ were used all over Europe during Neolithic. Their archaeometric investigation, due to this geo-resource scarcity, allows extrapolating info about supply sources and/or trades. The greenstone industry of the Rocca di Cavour settlement was characterized and compared to geologic ‘jades’ from circumscribed – yet mostly unmapped – outcrops on the Monviso Massif and adjoining valleys. Most tools are made of eclogite, jadeitite and omphacitite – a distribution found also in natural samples. The systematic detection of peculiar petrographic features confirms that all artefacts derive from the Monviso and highlights that these rocks form after metasomatic processes in shear-zones rich in aqueous fluids, typical of Western Alps – justifying their actual location and scarceness. Despite this, they were specifically sought after due to their technological potential, producing tools whose distribution expanded far beyond their sources. Relict surfaces suggest these artefacts were shaped by pebbles/cobbles from the Pellice or Po Rivers alluvial deposits. Greenstone Eclogite Jadeitite Omphacitite Neolithic implement Figures Figure 1 Figure 2 Figure 3 Figure 4 Figure 5 Figure 6 Figure 7 Figure 8 Figure 9 Introduction The Neolithic period can be considered the first technological era of mankind [ 1 ]. In Europe, humans abandoned their nomadic life and began to settle in the flat lands to the South of the Alpine chain (close to the present towns of Alessandria, Asti and Alba of the Piedmont region, Northwestern Italy), dedicating to agriculture and breeding. This innovative lifestyle required apt tools to be forged and used, in order to satisfy new circumstances and necessities, e.g., logging, house building and agriculture. From the early Neolithic (VI millennium BC) until the Bronze Age (II millennium BC), the industry of ceramics and polished stone flourished, both in production and trades. The latter, in particular, was represented by implements (e.g., axeheads, chisels) and ornamental tools (e.g., disc-rings and pendants) requiring both toughness and eye-appeal. They are mostly made of greenstone , a heterogeneous group of rocks – including ‘ jades ’ – which derive from the high-pressure metamorphic ophiolites (hereafter referred to as High-Pressure – HP – meta-ophiolites ) of the Internal Piemonte Zone in the Western Alps (e.g., [ 2 , 3 ]). Under the term ‘ jade ’, both ‘ jadeite-jade ’ (pyroxenes of the jadeite/diopside/aegirine solid solution) and ‘ nephrite-jade ’ [amphiboles of the tremolite/ferro-actinolite solid solution] are comprised; however, only the former will be considered hereafter [ 4 – 7 ]. Neolithic implements similar to those found in the Western Po plain were widespread throughout continental Europe and beyond: polished tools in greenstone were retrieved along a large stripe roughly oriented North-to-South, from Great Britain to Malta (e.g., [ 8 – 11 ]) and extending also westwards (in Southern and Northern France) and eastwards (Northeastern Italy and beyond). Sporadically, these tools have also been retrieved as far as Slovakia, Czech Republic and Hungary (e.g., [ 12 – 15 ]). These HP meta-ophiolites – with green colour, remarkable hardness and toughness – are aptly described in the literature (e.g., [ 16 ], with references therein) and classified in two groups . The first one includes Na-pyroxenites (commonly referred to as ‘ jades ’), consisting of pyroxene solid solutions between Na and Ca end-members, whose composition is represented in the ternary diagram including jadeite (Jd: NaAlSi 2 O 6 ), aegirine (Aeg: NaFe 3+ Si 2 O 6 ), and calcium components Q (Wo + En + Fs) (Morimoto et al., 1988). The most widespread rocks of this group are named jadeitite , if jadeite > 95 vol. %, omphacitite , if omphacite [(Na,Ca)(Al,Mg)Si 2 O 6 ] > 95 vol. %, and mixed Na-pyroxenite , if both jadeite and omphacite occur in similar amounts. The second group , which includes Na-pyroxene + garnet rocks , comprehends eclogite if the modal omphacite/garnet ratio % is in the 25–75 range and garnet-omphacitite if the modal amount of garnet is < 25 vol. % [ 17 ]. These greenstones sensu stricto ( s.s .) occur in HP meta-ophiolite units derived from the Liguria-Piemonte oceanic domain (e.g., [ 18 ]), which underwent Alpine metamorphism under eclogite-facies conditions (e.g., [ 2 ]). In the field, they outcrop either as small (few m 3 ), rare and mostly unmapped boulders at high altitude in the Monviso or Voltri meta-ophiolitic massifs [ 19 – 25 ], or as pebbles/cobbles in secondary Oligocene conglomerates of the Tertiary Piemonte Basin and Quaternary alluvial deposits, derived from the dismantling of the primary outcrops [ 26 – 31 ]. As such, greenstones s.s. represent very important archeometric markers, useful for identifying these artefacts supply sources and tracing trade routes. However, under the generic term ‘ greenstone’ , other lithotypes (e.g., serpentinite, amphibolite and prasinite) are also included by archeologists, since sharing the same colour. Seldom, also glaucophanite – a HP-rock mainly consisting of blue-amphibole – is inserted. These rocks, also used for producing Paleolithic and Neolithic implements, are – with few exceptions – less significant from an archeometric point of view, due to their ubiquitous distribution in the Western Alps (e.g., [ 31 ]). This study concerns the characterization – with non- or micro-destructive archaeometric techniques – of the polished greenstones tools from the archeological site of Rocca di Cavour , currently held in the Archeological Museum of Turin. These outcomes are compared to those of similar geological specimens collected during a geologic survey of the right orographic side of the upper Po valley and alluvial sediments, considered as the most probable source area for the raw materials. Methods Archaeological context The Rocca di Cavour (10061 Cavour, Metropolitan City of Turin, Piedmont region, Northwestern Italy: Fig. 1, redrawn after Cinquetti, [32,33]) is a typical Inselberg , i.e., an isolated hill (432 m a.s.l.) standing up ca. 130 m above the surrounding alluvial plain. Geologically, the Rocca is a remnant of metamorphic rocks that escaped fluvial erosion and glacial exaration at the mouth of the Pellice Valley. Geophysical data [34] show that it is connected under the Quaternary cover with the eastern margin of the continental Dora-Maira Massif. The Rocca is made up of a foliated leucogranite (protolith age: 304 ± 2 Ma [35]) exposed in the central and southern area of the hill, where dark mafic microgranular enclaves and pegmatitic dykes are recognizable in spite of the Alpine tectono-metamorphic overprint. The original intrusive contact with the host micaschists of the Dora-Maira pre-granitic basement, exposed at the northwestern top of the hill, has been completely transposed, but xenoliths of the country rocks and aplitic dykes are still identified. Despite an important anthropization, significant traces of a prehistoric attendance are still evident, especially on the Northern and Western sides. Surface prospections, performed under the supervision of the Archaeological Superintendence of Piedmont and the ‘ Centro Studi e Museo di Arte Preistorica ’ (Center of Studies and Museum of Prehistoric Art) of Pinerolo, brought to the retrieval of several artefacts, splinters and an axe-shaped pebble made in greenstone . The recovered polished stone industry of the Rocca consists of 98 objects – mainly fragmented axehead roughouts, chisels and splinters in greenstone – found in three different areas (Western, Southeastern and Northern slopes [36]), together with ceramics and splintered stone items [37]. The archaeologic surveys showed that a preliminary shaping of the greenstone raw materials was presumably performed on site. All steps of the production chain were carried out on site, except the choice of pebbles and boulders with proper shape and lithology and gross splintering/shaping, presumably performed on the collection site. The retrieved axehead roughouts (and other tools) testify that a consolidated production chain existed, including finer splintering (performed by using spheroidal pebbles as strikers), bush-hammering (to eliminate sharp edges) and polishing (to smoothen the tool surface). Splintering is justified by 50 (out of 98) samples from decortexing of the lithic support; on 17 of these, traces of percussion with a striker are evident [38]. Few are the polished objects – namely 2 cutting-edges, in which polishing is observed close to the blade, with bush-hammered borders presumably to facilitate grip. Several fragmented axe heels and unpolished cutting edges are present, with 3 sub-circular strikers and a single chisel (Fig. 2). The Rocca di Cavour must therefore be considered an atelier site, in which only the initial steps of the production chain were performed, forming several scraps and wastes that were left in place, eventually to be reworked for other purposes (Zamagni, 1996). The Monviso meta-ophiolite Complex A quick examination of the archaeological finds revealed that they consist of greenstone ; as such, they cannot derive from the Rocca substratum. The research for the supply sources was thus shifted to the nearby Monviso massif (Fig. 3, redrawn after Blake et al., 1995 [39]). The Monviso Meta-ophiolite (MMM) Complex is a geological body elongated N-S for 35 km, from the Val Varaita to Val Pellice , with a maximum thickness of 6-7 km. The Complex is bounded by two main tectonic contacts, which separate it to the W from the blueschist-facies calc-schists (“schistes lustrés”) of the internal Piemonte Zone and to the E from the eclogite-facies continental basement of the Dora-Maira Massif [40]. The Monviso complex belongs to the eclogite-facies Internal Piemonte Zone and consists of several tectonometamorphic units, some of which re-equilibrated at Ultra-High-Pressure (UHP) conditions in the coesite stability field ([41], with refs. therein). In spite of the Alpine polyphase tectono-metamorphic overprint, the westernmost unit (Fig. 3) best preserves a complete oceanic sequence consisting of basal isotropic and locally layered gabbros, intermediate massive and pillowed basalts, capped by a sedimentary quartz-rich cover [42]. The most interesting unit from an archaeometric point of view is the easternmost basal serpentinite ( s in Fig. 3), containing small outcrops – specifically indicated here – of fine-grained jadeitite (blue dots in Fig. 3) and eclogite (red dots in Fig. 3), [22,24,25,30,43]. For comparison with the Rocca di Cavour archaeological implements, 10 greenstone s.s geological samples were collected in the basal serpentinite from both primary outcrops in the upper Po Valley and alluvial conglomeratic deposits exposed at its mouth on the Po plain [44]. Also, six fine-grained eclogite-facies samples from the Quaternary alluvial sediments of the Po were collected and kindly provided by Dino Delcaro. Two fine-grained eclogites from the Val Carbonieri (Fig. 3), whose preliminary petrology and chemistry appeared in a previous paper [45], were also considered. Analytical methods A preliminary rock identification of all 98 lithic implements from the Rocca di Cavour site, previously classified by archaeologists on morphological and stylistic basis [38], was carried out by means of two non-invasive methods : i) Stereo-microscopic observations , which allowed performing a preliminary greenstone screening, discriminating eclogites through the identification of garnets and recognizing primary and secondary compositional heterogeneities and/or peculiar microstructures (e.g., [46,47]). Since a classification solely based on optical observation can be misleading for the fine to very-fine grain-size of minerals, ii) density determination was also performed, which is very useful for homogeneous rocks devoid of retrogression. Moreover, some artefacts (selected among incomplete tools) were analyzed through more in-depth micro-invasive coring methods . From each drill core sample (10 mm across) – representative of the rock composition, since the grain-size is systematically fine to very fine (e.g., [16,26,48]) – a petrographic thin section was obtained and the rest powdered in an agate mortar. Thin sections were examined under an optical polarized-light microscope Zeiss WL Pol to recognize rock microstructure and mineralogy. After carbon-coating, the chemical composition of major, minor and accessory minerals was studied by Scanning Electron Microscopy with Energy-Dispersive-Spectrometry (SEM-EDS), using a Cambridge Stereoscan 360 SEM equipped with an EDS Energy 200 and a Pentafet detector (Oxford Instruments). The operating conditions were: 50 s counting time, 15 kV accelerating voltage, 25 mm working distance, 300 pA beam current. SEM-EDS quantitative data (spot size = 2 μ m) were acquired and managed using the Microanalysis Suite Issue 12, INCA Suite version 4.08; the raw data were calibrated on natural mineral standards and the ΦρZ correction [49] was applied. The Fe 3+ ⁄ Fe ratio in garnet and omphacite has been estimated by stoichiometry from the SEM-EDS analyses. Since eclogites consist of coexisting garnet and omphacite, the calibration of Powell (1985) [50] of the geothermometer based on the Mg/Fe partitioning (K D ) between these minerals was applied. Powders were analyzed with X-ray powder diffraction (XRPD), capable of evaluating the relative mineral modal amounts in fine-grained rocks. Data were collected in the 5°-50° 2q range on an automated Siemens D-5000 diffractometer with q/2q setup in Bragg-Brentano geometry, with Cu-Ka radiation and a zero-background sample holder, and processed with the Diffrac Plus (2005) [51] software (EVA 11,00,3). Results Stereo-microscopy and density measure Since these artefacts rocks are systematically fine to very fine-grained, stereo-microscopy can allow recognizing small garnets, whose presence indicates eclogite and garnet-omphacitite. The density of 97 (out of 98) archaeological implements was determined (Fig. 4.a). As expected, two groups are observed. The one with density > 3 g/cm 3 includes greenstones s.s. (namely jadeitite, omphacitite, mixed Na-pyroxenite, Grt-bearing omphacitite and eclogite – roughly listed in order of increasing density). The other, with density > 2.7 g/cm 3 , includes only serpentinite. A single prasinite is also observed (3.1 g/cm 3 ). These artefacts are thus mainly composed of greenstones s.s. (83 %; Fig. 4.b), in which e clogites (54 %) predominate over Na-pyroxenites (16 %); serpentinites are quite scarce (6 %). For a limited number of specimens (3) no clear lithological attribution is achieved, for lack of useful information. All data, including inventory code and typological descriptions, are listed in the Supplementary Material, Table S1. X-ray powder diffraction Archaeological tools Table 1. Variation of cell parameters of pyroxenes (jadeite and omphacite), as determined from XRPD data collected on 45 Neolithic greenstone implements from Rocca di Cavour similar geological samples from primary outcrops of the upper Po valley and from secondary alluvial deposits. Cell parameters Jadeite NaAlSi 2 O 6 Omphacite (Na,Ca)(Al,Fe,Mg)Si 2 O 6 a 0 9.425(3) – 9.482(4) Å 9.512(3) – 9.631(2) Å b 0 8.573(3) – 8.650(2) Å 8.674(2) – 8.811(3) Å c 0 5.223(1) – 5.262(2) Å 5.252(2) – 5.283(1) Å b 107.42°(4) – 107.75°(4) 106.61°(3) – 107.42°(2) Volume 403(2) – 410(2) Å 3 415(2) – 428(3) Å 3 XRPD data were collected on 37 representative samples (Supplementary Material, Table S2), which allowed identifying the nature of the major/minor minerals of the rocks, as well as the average composition of Na-pyroxenes based on their unit-cell parameters (Table 1), sensitive to chemical variations (c.f., [16]). Few implements are made of rocks with pyroxene compositions close to either pure jadeite or omphacite (Fig. 5.a). In most, a jadeitic pyroxene coexists with a more omphacitic one, as suggested by the splitting of related reflections (Fig. 5.b). This accounts for finer variations in the cell parameters, especially for a 0 and b 0 (Table 1). In omphacite, a 0 is usually > 9.52 Å – the lower values being determined by a higher content in Aeg (a Fe 3+ -richer end-member of the same solid solution: NaFeSi 2 O 6 ). Eclogites also show the garnet peaks, in addition to omphacite. The estimated pyroxene compositions based on XRPD data proved to be consistent with the SEM-EDS results. Geologic samples XRPD was also performed on 16 geologic greenstones s.s. akin to the archaeological finds, namely: 7 Na-pyroxenites (2 jadeitites, 4 omphacitites and 1 mixed Na-pyroxenite) and 9 Na-pyroxene + garnet rocks (8 eclogites, 1 garnet omphacitite). Calculation of the Na-pyroxenes unit-cell parameters gave values consistent with those of the Neolithic tools (Table 1). Also, the compositions estimated from the d hkl values were in good agreement with those obtained by SEM-EDS. On the Morimoto et al. (1988) ternary diagram ([52], Fig. 6.a), these compositions (red spots) plot very close to those of the archeological implements (green spots in Fig. 6.b). For each sample, the unit-cell parameters, d hkl values and estimated pyroxene composition (in terms of Jd, (Wo+En+Fs) and Aeg wt %) are reported in Supplementary Material, Table S3. Petrographic study This method, to be implemented by SEM-EDS, is essential to describe and interpret the complex tectono-metamorphic history experienced by HP-greenstones s.s. (e.g., [46]). Archaeological tools 18 thin sections were obtained from small drill-cores of splinters/uncomplete tools, namely: 5 Na-pyroxenites (3 jadeitites and 2 omphacitites) 13 Na-pyroxene + garnet rocks (7 eclogites and 6 garnet omphacitites) Their qualitative/quantitative compositions – integrated also by XRPD and SEM-EDS (when available), are reported in the Supplementary Material, Table S4. Eclogite Five out of seven eclogite samples (PIEM77/80/84/86/87) are medium- to fine-grained. Locally, a weak foliation is evident, marked by the dimensional preferred orientation of omphacite, rutile and titanite, as well as by the alignment of smaller garnets. In two samples (PIEM86 and 87), a more pervasive foliation turning into a mylonitic fabric is wrapping around omphacite porphyroclasts, which are zoned with a greenish more omphacitic rim, richer in Wo+En+Fs and Aeg, surrounding a colourless Jd-richer core that includes drop-like exsolutions of a higher-relief Na-pyroxene (akin to the one at the rim) and tiny rutile/titanite inclusions. Garnet occurs as small- to medium-grained idioblastic zoned poikiloblasts, with a pinkish core and a colourless rim, locally with atoll-like habit (e.g., in PIEM 80, 84 and 87; Fig. 7.a). Clinozoisite, zoisite and white-mica aggregates with euhedral shape and murky borders are interpreted as pseudomorphs after former lawsonite porphyroblasts (e.g., in PIEM86; Fig. 7.b). Rutile, ilmenite and titanite are the most common accessories, the latter deriving from alteration of the formers. Rutile occurs as skeletal aggregates, single grains or tiny acicular crystals. Rare zircon (PIEM87), apatite (PIEM86) and opaque ores are locally observed. A weak greenschist-facies retrogression is testified by the partial replacement of Na-pyroxene by a symplectitic aggregate of actinolite and albite (e.g., PIEM 77, 80 and 87). Other accessories include small xenoblasts of glaucophane, locally replaced by a Ca-richer amphibole, and aggregates of chlorite together with epidote, white mica and interstitial albite (PIEM87) often with polysynthetic twinning (PIEM77). Two more samples (PIEM76/88) are glaucophane eclogites, characterized by a medium- to fine-grained matrix consisting of relict omphacite and subordinate glaucophane, strongly retrogressed to symplectitic aggregates of actinolite and albite. The fragmented garnet poikiloblasts include opaque ores in the rim and omphacite, rutile, titanite and epidote in the core. Apatite and iron-sulfides are accessories. Garnet-omphacitite The six samples consist of a fine-grained omphacite matrix (» 70 vol. %) that includes euhedral (PIEM90) to subhedral (PIEM85) scattered poikiloblasts of zoned garnets, with a pinkish core and a colourless rim. Tiny rutile crystals define a weak foliation. In PIEM85, the foliation is also highlighted by omphacite micro-crystals and acicular rutile (Fig. 7.c), which are wrapping around bigger pyroxene crystals. In four other samples (PIEM75/78/91/92), the rock consists of two intimately associated pleochroic pyroxenes with different appearance and composition, which define an almost mylonitic foliation: one, bright-greenish in colour, presumably richer in Aeg (> Fe 3+ ); the other, pale green, is more omphacitic. Locally, a few bigger zoned pyroxenes occur with a greener Ca-richer core including rutile needles and a colourless, more jadeitic, inclusion-free rim. Aggregates of euhedral zoisite, clinozoisite and white mica (e.g., in PIEM75 and 78) are interpreted as pseudomorphs after former lawsonite, which are surrounded by a Na-pyroxene corona, mostly retrogressed to an albite+actinolite intergrowth. Titanite, zircon, allanite, chlorite and opaque ores are accessory phases. Omphacitite The two studied samples (PIEM79/89) have fine- to very fine-grained omphacite matrices (» 70 vol. %), with minor rutile, titanite, ilmenite, allanite, quartz and scarce epidote, albite and pyrite. In PIEM89, a strongly zoned omphacite exists with a deeper green core (presumably Fe 3+ -richer) and a colourless, more jadeitic rim (Al 3+ -richer). The cores are often dusty, due to tiny rutile needles oriented parallel to the pyroxene elongation, interpreted as the product of unmixing from an original igneous Ti-rich pyroxene. Rutile also occurs as skeletal aggregates of anhedral crystals, partly retrogressed to titanite. Large irregular aggregates of zoned epidote, with yellowish to dark-blueish anomalous interference colours, are observed. Large sub-idioblasts of opaque ore occur, often associated with albite. In PIEM79 a weak foliation is defined by the alignment of ilmenite porphyroclasts and tiny pale-green omphacite micro-crystals. Small roundish domains are also observed, consisting of fine-grained aggregates of omphacite and chlorite (plus tiny quartz crystals at the border), possibly derived from the alteration of original garnet poikiloblasts. Ilmenite, the second most abundant phase, forms xenomorphic porphyroblasts either stout or elongated, oriented parallel to the foliation. Jadeitite The 3 analyzed samples (PIEM81/82/83) exhibit a granoblastic structure and consist of jadeite (> 90 vol. %) with minor amounts of epidote + titanite (PIEM82 and 83), albite + glaucophane (PIEM83) or paragonite (PIEM82). Rutile and zircon are common accessories. Jadeite blasts have variable size and heterogeneous grain-size, even within the same sample. Usually, jadeite is zoned with a colourless core (> Al 3+ ) and a pale green rim (> Fe 3+ ). The jadeite core is murky, due to inclusions of acicular rutile parallel to the pyroxene elongation and tiny exsolution droplets of a more omphacitic pyroxene (Fig. 7.d). Fine-grained rutile may also form skeletal aggregates, occasionally retrogressed to titanite. Albite occurs as interstitial domains including idioblastic omphacite with prismatic habit (PIEM83). Minor phases are acicular glaucophane and red-to-brown pleochroic allanite locally including zircon. Geologic samples 16 thin sections were obtained from meta-ophiolites of primary outcrops and alluvial deposits of the upper Po valley, namely: 6 Na-pyroxene rocks (4 jadeitites, 2 omphacitites) 10 Na-pyroxene + garnet rocks (all eclogites) Their qualitative/quantitative compositions – integrated also by XRPD and SEM-EDS (when available), are reported in the Supplementary Material, Table S5. Eclogite The ten samples studied are fine- to medium-grained rocks that essentially consist of omphacite and garnet, with accessory epidote, chlorite, glaucophane, white mica, albite, quartz, rutile, apatite and opaque ores. Omphacite occurs as medium- to fine-grained elongated nematoblasts, whose colour varies from colourless or pale green (bigger crystals) to bright green (fine-grained aggregates). The bigger crystals are often zoned with a green to turquoise core and a colourless, more jadeitic rim (e.g., OF2780 and 2765; Fig. 7.e). Most omphacite blasts have a core containing tiny drop-like exsolutions of a pyroxene with different chemistry and acicular rutile. Small- to medium-sized subidioblastic garnets may occur up to about 50 % of the rock volume (e.g., OF2779). The biggest poikiloblastic garnets include omphacite, rutile, chlorite, quartz and epidote. The omphacite inclusions in atoll-like garnets have the same optical properties (and probably the same composition) of the external one. Some garnets are zoned with a pinkish core and a colourless rim. A marked planar anisotropy is often visible, due to the alternation of nematoblastic omphacite-rich domains and granoblastic garnet-rich ones. In some cases (OF2675), a compositional layering is observed, with alternating pyroxene- and epidote-rich layers. Local foliation is defined by the dimensional preferred orientation of omphacite nematoblasts and aggregates of opaque ores (OF2779) and rutile (OF2771). Some samples are crossed by sets of late fractures, along which a greenschists-facies retrogression appears (OF2758, 2771, 2779 and 2780, as well as in the Val Carbonieri samples – e.g., OF2702 [45]). Rutile, the most abundant accessory, occurs as either small random blasts (OF2765) or aggregates parallel to foliation (OF2761, 2764, 2781). Large randomly oriented pleochroic glaucophane idioblasts (OF2764 and 2765; Fig. 7.f) occur, locally almost completely replaced by a Na/Ca- bluish green amphibole (OF2779 and 2780). Pale greenish epidote xenoblasts (e.g., OF2758, 2765, 2781) or colourless clinozoisite with yellow-to-blueish anomalous interference colours locally fill veins in association with opaque ores (OF2781). Chlorite forms pale-green to colourless domains (OF2779, 2780). Only in one case (OF2781), an omphacite + garnet + chlorite assemblage is observed, where the sharp contacts between chlorite and garnet crystals indicate that these minerals are in equilibrium. White mica, usually scarce and fine-grained (OF2764, 2779), occurs in OF2781 as medium-size lepidoblasts. Two samples (OF2775 and 2785) with porphyroblastic structure and planar foliation consist of typical eclogitic/garnet-omphacite layers, alternating with others enriched in garnet, epidote, chlorite and albite. In the latter layers, zoisite/clinozoisite + white mica pseudomorphs after former lawsonite are surrounded by a mylonitic foliation, defined by fine-grained omphacite with tiny garnets. The rock foliation is crossed by a set of late fractures, along which omphacite is replaced by a darker albite + Na/Ca-amphibole symplectite. Chlorite and rutile are accessories. Omphacitite The two samples have fine (OF2760) or fine-to-medium grain-size (OF2763), consisting of omphacite and accessory white mica, epidote, chlorite and rutile. OF2760 contains omphacite domains alternating with others where white mica, epidote and minor rutile are observed. OF2763 has a marked foliation, defined by the dimensional preferred orientation of white mica flakes and pyroxene nematoblasts, alternating with domains of granoblastic omphacite. Coarser-grained omphacite crystals are slightly pleochroic (green-to-yellowish), with a core more coloured than the rim. The omphacite core is often dusty due to tiny inclusions of acicular rutile, parallel to the elongation of the host crystals. In OF2763, white mica (probably paragonite) occurs as medium-grained euhedral lepidoblasts. In OF2760, white mica occurs as small xenoblasts associated to epidote. Zoisite and clinozoisite form xenoblastic aggregates, while chlorite occurs as domains (OF2760). In OF2763, accessory allanite is observed. Jadeitite The four specimens are fine-to-medium grained and mainly consist of jadeite (³ 75 vol. %), with minor albite and amphibole. Zircon, rutile and allanite are ubiquitous accessory minerals. The microstructure is either granoblastic (OF2772 and 2788) or porphyroblastic (OF2774). In some cases, a weak foliation is observed, defined by the dimensional preferred orientation of jadeite blasts (OF2767 and 2774). Colourless jadeite occurs as xenoblasts of variable dimensions; the bigger crystals (» 2 mm across) exhibit either a radial to fibrous habit or subgrain microstructure (OF2774). Some jadeite crystals are evidently zoned, with small light-green exsolution droplets of omphacitic pyroxene included at the core. Occasionally, jadeite porphyroblasts are surrounded by fine-grained aggregates, rimmed by a thin film of retrograde albite, biotite and acicular amphibole (OF2774). Idioblastic to subidioblastic zircons, rutile and allanite are ubiquitous accessory phases. SEM-EDS Besides allowing observation at higher magnifications (Fig. 8), this approach also defines the chemistry of pyroxene and garnet solid solutions. Chemical data (Fig. 9) are plotted on the Jd/Aeg/Q diagram of Morimoto et al . (1988) [52], Fig. 6.a) for pyroxenes and [almandine (Alm) + spessartine (Sps)] – grossular (Grs) – pyrope (Prp) ternary diagram for garnets; mineral symbols follow Warr (2021) [53]. EDS analyses of pyroxenes and garnets are reported in the Supplementary Material (Tables S6-S21). Archaeological tools 9 thin sections were analyzed, namely: 5 Na-pyroxene rocks (3 jadeitites and 2 omphacitites) 4 Na-pyroxene + garnet rocks (3 eclogites and 1 garnet omphacitite). Eclogite Two eclogites (PIEM77 and 80) show different microstructures. In the former, a weakly-zoned omphacite matrix has an average Jd 40 , (Wo+En+Fs) 45 , Aeg 15 composition, with Q decreasing from the rim (60 wt %) to the core (40 wt %) at constant Jd/Aeg ratio. Presence of albite, Mg-chlorite, clinozoisite and titanite-rich areas indicates a weak greenschist-facies overprint (Fig. 8.a). Omphacite included in garnet has the same composition as the matrix core (Fig. 9.a). Garnet , often with atoll-like structure (Fig. 8.b), is a weakly zoned almandine with Grs component slightly increasing from core to rim (Fig. 9.a). In the latter, a more marked pyroxene zoning is observed: a more jadeite-rich core (up to Jd 90 ) decreases towards the rim reaching Jd 70 and Jd 50 (A and B in Fig. 9.a, respectively). Omphacite exsolutions in the jadeite core have an average composition Jd 60 , (Wo+En+Fs) 25 , Aeg 15 (C in Fig. 9.a). Garnet shows a weak zoning, with the grossular decreasing from core (Grs 20 ) to rim, enriched in Alm (Fig. 9.a). In PIEM76, a retrogressed glaucophane eclogite , relict omphacite has an average composition Jd 35 (Wo+En+Fs) 50 Aeg 15 , with Q slightly decreasing from core to rim. Pyroxenes included in garnet and in the matrix have the same composition. Garnet is an almandine with low Prp and Grs (» 10 wt %) (Fig. 9.a). Garnet-omphacitite PIEM75 is characterized by a banded structure with alternating garnet-bearing and -free layers. In the latter, a fine-grained Na-pyroxene matrix with mylonitic fabric includes clinozoisite + paragonite aggregates with a geometric shape, interpreted as pseudomorphs after former lawsonite porphyroblasts. Two distinct pyroxene compositions emerge from BSE images: i) strongly zoned and with finer grain-size, with average composition: Jd 45 (Wo+En+Fs) 40 Aeg 15 ; ii) with bigger, zoned and Fe-richer relict crystals, whose Q component varies from 30 to 55 wt % at a constant Jd/Aeg ratio (A and B in Fig. 9.a). In the garnet-bearing layers, the little poikiloblastic garnets that overgrows the mylonitic foliation include small rutile, titanite and omphacite. Garnet composition is quite homogeneous (average: Alm+Sps 75 Grs 15 Prp 10 ). Omphacitite In PIEM79, omphacite represents about 75 vol. % of the rock and is slightly zoned, with the jadeite end-member decreasing core-to-rim from Jd 45 to Jd 35 , at constant aegirine content (Aeg 20 ) (Fig. 9.a). Two roughly round-shaped portions, consisting of Mg-chlorite with relict pyroxene, are interpreted as pseudomorphs after former poikiloblastic garnet. In PIEM89, omphacite is strongly zoned with jadeite increasing from Jd 15 in the core to Jd 40 in the rim (Fig. 9.a). Tiny oriented rutile inclusions in the omphacite core suggest its derivation from exsolution of an original magmatic pyroxene. Jadeitite PIEM81 and PIEM82 consist of > 90 vol. % of fine-grained, almost pure jadeite (³ Jd 95 ), which locally contain at the core drop-like omphacitic exsolutions and acicular rutile (Fig. 8.c). Jadeite is surrounded by an omphacite rim with composition Jd 50-35 (Wo+En+Fs) 30-45 and Aeg 20 (Fig. 8.d; 9.a), similar to the exsolutions in the jadeite core. In PIEM82, a darker sub-circular domain is observed (similar to PIEM79), consisting of epidote, albite, paragonite and relict Na-pyroxene (Fig. 8.d). In PIEM83, the pyroxene occurs as big, irregularly zoned and sub-idioblastic crystals, usually Jd-richer at the core (Jd 100-70 ) than the rim Jd 50 (Wo+En+Fs) 30 Aeg 20 (B in Fig. 9.a). The core includes tiny inclusions of acicular rutile and drop-like exsolved omphacite (A in Fig. 9.a). Late domains of albite also appear, which frequently include euhedral prismatic Na-pyroxene with aegirin-augite composition (C in Fig. 8.a). Geologic samples 4 thin sections were analyzed, namely: 1 Na-pyroxenite (jadeitite) 3 Na-pyroxene + garnet rocks (all eclogites). Eclogite The eclogite OF2780 is medium- to fine-grained, with grano-nematoblastic structure and a weak foliation. Omphacite crystals are zoned, with an aegirine-augite richer core (Aeg 30-40 ) and a more omphacitic rim (Jd 40 , Wo+En+Fs 35 and Aeg 25 ). Idioblastic garnets with atoll-like habitus are also zoned, with Grs increasing from core [(Alm+Sps) 80 , Prp 15 , Grs 5 ] to rim (up to » 20 wt %) (Fig. 9.b). The other two eclogites come from the Val Carbonieri [45]. OF2671 is fine-grained, with small garnets that seldom show an atoll-like aspect; they are contoured by a pyroxene matrix with a homogeneous omphacite composition (Jd 40 , Wo+En+Fs 40 and Aeg 20 ). Garnets are zoned and rich in almandine (75 to 85 wt %), with grossular decreasing from core to rim (» 20 to 0 wt %). OF2702 is formed by omphacite porphyroclasts, wrapped by a finer matrix of both omphacite and garnets. The pyroxene has quite a homogeneous chemistry (Jd 25-50 and Aeg 10-25 ), with garnets very similar to the previous sample (Fig. 9.b). Jadeitite OF2788 is a fine-grained granoblastic rock with almost pure jadeite (>95 wt.%) (group A in Fig. 9.b), containing accessory rutile and zircon. In the core, jadeite crystals have small, drop-like omphacite exsolutions with composition Jd 50 , (Wo+En+Fs) 25 , Aeg 25 (group B in Fig. 9.b). These crystals are surrounded by a rim (Fig. 8.f) in which the jadeite content decreases from Jd 55 to Jd 75 , at a constant (Wo+En+Fs)/Aeg ratio (group C in Fig. 9.b). Geothermometry In petrology, an estimate of the temperature peak of an eclogite-facies rock can be achieved from the garnet-omphacite, Fe/Mg exchange geothermometer. This is based on the partitioning of Fe and Mg between coexisting garnet and omphacite, whose amounts vary as a function of temperature. By applying the Ellis and Green (1979) calibration [54] for a nominal pressure of 15 kb, the T estimates were found to vary between 350 and 600 °C (Table 2) – with most samples in the 400-500 °C range, which is consistent with the literature data for the Monviso meta-ophiolite (e.g., [55]). However, unlike the coarse-grained eclogites – already mapped and analyzed in the geologic literature [42], two distinct temperature groups were obtained for each fine-grained eclogite of archaeological interest. This anomaly was interpreted as a consequence of the complex metamorphic history of these scarce and peculiar rocks, which experienced a polyphase mylonitic deformation in the presence of active aqueous fluids that produced a significant metasomatism, evidenced by the complex chemical zoning of both garnet and Na-pyroxene. Due to this, geothermometry is unfit to be used for identifying their provenance. Table 2. Geothermometry results on the Fe-Mg partitioning in coexisting omphacite/garnet couples. Temperatures were computed at the nominal pressure of 15 kb. Analytical code Lithotype T -range T-clusters PIEM 77 Eclogite 390 – 540 °C 520 ± 20 °C PIEM 80 Eclogite 310 – 470 °C None PIEM 76 Eclogite 355 – 405 °C 383 ± 30 °C PIEM 75 garnet-omphacitite 330 – 690 °C None OF2780 Eclogite 375 – 625 °C None Discussion Polished greenstone axes have always been considered by archaeologists as typical of Neolithic. The Neolithic site of the Rocca di Cavour , in spite of its position (in front of the meta-ophiolitic complex of the Monviso Massif – the main area of origin, together with the Voltri Massif, of most archaeological greenstone tools spread throughout all Europe), had never been the object of a detailed archaeometric study so far. Although in this case the origin of the raw materials, as far as greenstones are concerned, is quite straightforward (i.e., from local eclogite-facies meta-ophiolites), the performed archaeometric survey still provides useful information about the mineralogy and petrology of the investigated lithologies, especially in light of the comparative study on geological samples from the primary outcrops of the Monviso Complex and related secondary deposits. Although it is well-known that these rocks belong to the calc-schists with greenstones Piemonte Zone (e.g., [24]), the vastness of this area and their limited distribution in a wide reservoir such as the Western Alps cause this knowledge to still be unsatisfactory. Natural, fine-grained ‘ jade ’ samples similar to the archaeological finds were unknown to geologists until recently, since the primary outcrops are extremely scattered, small (few m 3 ) and heterogeneous – thus hardly traceable even by expert petrologists focused on the study of eclogite-facies meta-ophiolites. These rocks can also be found in secondary deposits, where they tend to concentrate due to their higher hardness and lower erodibility, if compared to other rocks. Here, these deposits are represented by the Quaternary alluvial surrounding the Monviso Massif and the Oligocene post-orogenic conglomerates. The 98 studied polished-stone implements of the Rocca di Cavour settlement are mostly made of eclogite (54 %) and garnet-omphacitite (13 %), with subordinate jadeitite (5 %) and omphacitite (8 %; Fig. 4). Predominance of eclogite is consistent with several coeval sites of Northwestern Italy (e.g., Alba, Castello di Annone, Gaione, Ponte Ghiara, Rivanazzano, Sammardenchia, San Lazzaro di Savena and Valgrana/Tetto Chiappello [10,45,56-66]). In eclogite and garnet-omphacitite , the modally prevalent pyroxene (i.e., mostly omphacite) is characterized by a wide compositional range. Moreover, it is frequently zoned with complex and variable patterns. Garnets are also highly heterogeneous, both structurally and compositionally. The widespread atoll-like garnets, which locally contain remnants of the original core, indicate that these minerals experienced at least two main types of growth, under different P-T conditions: i) at first, multiple nucleation and coalescence processes allowed the poikiloblastic growth of small garnets; ii) later, their cores became unstable and in the presence of an abundant influx of hydrous fluids, they were easily corroded through replacement and re-crystallization reactions [67-72]. In most cases, garnets show an almandine-rich (i.e., Alm ³70) average composition, either homogeneous (e.g., in PIEM76, where Alm 87-93 -Prp 9-5 -Grs 9-2 ) or with an appreciable zoning (e.g., in PIEM75, where Grs grows from 5-to-21 % from core to rim). Also, in most eclogites and garnet-omphacitites lozenge-shaped aggregates of zoisite + clinozoisite + white mica exist, interpreted as pseudomorphs after an original porphyroblastic lawsonite, which grew at high-pressure conditions but broke down during later exhumation. Jadeitite and omphacitite are monomineralic rocks, since Na-pyroxene is modally prevalent (> 90 vol. %). In jadeitites , crystals of almost pure jadeite (Jd ³ 90 ) are often contoured by omphacitic rims and include, at their core, tiny drop-like exsolutions with akin omphacitic composition. Such an occurrence has already been described in the literature [73-75]. Accessory rutile (TiO 2 : see Supplementary Material, Table S4) indicates that these rocks belong to the internal Piemonte Zone, i.e., from the Monviso Massif (in the external Piemonte Zone, titanite [CaTi(SiO 4 )O] would have appeared instead). Omphacitites have quite a homogeneous chemistry, being mostly made of weakly zoned omphacite. The performed geologic survey allowed collecting and analyzing several greenstone specimens akin to the rocks of the prehistoric tools. In both instances, an intimate association of various omphacites with a modest zoning and variable Aeg contents is consistent with the variability described in the literature [76,77], which supports the possible existence of a miscibility gap between Aeg-poorer and Aeg-richer omphacites. Another systematic prospection of the Monviso Massif, aimed at locating primary outcrops of jadeitite-jades, was carried out quite recently [23,78]. In that instance, however, the archaeometric recognitions were achieved by using a completely different protocol – namely visual identification and spectro-radiometry [79,80]. These approaches, unfortunately, may not always allow a thorough and reliable characterization of these lithotypes (not only jadeitites, but all greenstones s.s. ), which possess both compositional and micro-structural complexities hardly extrapolable without recurring to in-depth mineral/petrographic approaches. The comparative study performed here by using rigorous methods unequivocally proves that most eclogites are very similar in archaeological and geologic samples, both marked by fine grain often with mylonitic structure. Other common issues are: i) the typical atoll-like structure and zoning of garnets (e.g., in OF2780, with Alm up to 84 % and Grs varying from ≈ 0-20 % between core and rim, respectively; the two geologic samples from the Val Carbonieri show moderate zoning, but with an opposite trend, i.e., Grs decreasing from core to rim.); ii) the recurrence of pluri-millimetric zoisite + clinozoisite + white mica pseudomorphs on original lawsonite; iii) the persistence of regressed areas in greenschist-facies and v) a lack or scarcity of white mica (muscovite, paragonite and/or phengite). The last feature is an undisputable clue indicating provenance from the Monviso Massif [3,47,66] – whereas the abundance of white mica is instead an issue typical of greenstones from the Beigua district, in the Voltri Massif (e.g., in the tools from Brignano Frascata, Villaromagnano and Momperone and related geological samples [31,46]). In these fine grained eclogites, veins or irregular omphacite domains lacking garnets are also observed, with features at times similar to those appreciable in Neolithic tools qualified as ‘Na-pyroxenites’. It is therefore possible that some omphacitites, classified as such in Neolithic tools, might indeed result from considering restricted omphacitic domains in larger, garnet-bearing rocks. This is confirmed by that fact that, in some artefacts (e.g., PIEM75), vast different portions with and/or without garnets are detected. Similarly, in other archaeological tools classified differently based on said parameters (i.e, presence/absence of garnets), pyroxenes with similar chemistry and features are observed. For example, in PIEM90 (a garnet-omphacitite , due to presence of scarce garnets) a light-green, anhedral and non-pleochroic omphacite exists, whose optical properties are very similar to that of PIEM79 (classified instead as an omphacitite, after an apparent lack of garnets). All these aspects account for the petrologic/petrographic complexity of these rocks, which must be considered any time an in-depth study should be attempted. Such a complexity, which involves both the micro-structure and composition of pyroxenes and garnets, is synergic to the geological context in which these rocks are located and formed. In fact, they are confined in small boudins (few dm 3 to m 3 ) within shear zones, which underwent a polyphasic evolution marked by circulation of fluids with variable composition in time, as certified by the peculiar zoning of such minerals. In garnets, for example, this zoning, rather than being related to T/P variations (i.e., the metamorphic degree), depends on a metasomatic process in which the fluid (aqueous) phase had variable composition in different sites and moments in time and space, with direct consequences on their chemistry. For what concern jadeitites , several interesting clues emerge by comparing archaeological and geologic samples. The four metaophiolites from the alluvial sediments of the Po River – all fine grained with mylonitic fabric and accessory rutile – are very similar to most of their Neolithic counterparts. This suggests a provenance from the internal Piemonte Zone, marked by an Alpine eclogite-facies overprint. Other similarities concern specific features observed at SEM in BSE images – i.e., the clear-cut zoning of Na-pyroxenes and the coexistence of two distinct pyroxene phases, jadeite and omphacite, the latter confined in drop-like omphacite exsolutions hosted at the core of the jadeite crystals, in turn contoured by omphacitic rims (e.g., in OF2788 and PIEM81/82/83; see Fig. 8.d and f). Also, in the prospected area, nodules of omphacitites crop out within extended chloritic-carbonatic schists, with compositional signatures very similar to some archaeological tools. Any attempt to determine the thermal peak of the high-pressure metamorphic event by applying the Fe/Mg partitioning between coexisting Na-pyroxene and garnets in eclogites did not yield satisfactory results, due to the recurring presence of two Na-pyroxenes with different compositions, coupled to mostly zoned garnets. Despite this, most of the obtained values are consistent with the literature data estimated for the Monviso eclogites [42,55]. As stated above, the rocks of the Neolithic tools are all fine grained, with typically zoned pyroxenes and garnets. Thus, their mineral/petrographic features and chemistry should be compared only with geologic samples having similar features (particularly, the fine grain-size). Unfortunately, the analyses of pyroxenes and garnets available in the geologic literature so far often refer to coarse-grained meta-gabbros, exposed in large outcrops (e.g., [40,42,81]). In fact, two different kinds of eclogite exist: i) coarse-grained lithologies, whose microstructure is indicative of a magmatic protolith; ii) fine-grained lithologies, located in scarce and tiny (few dm-to-m 3 ) outcrops – yet mostly unmapped – scattered along shear zones and affected by metasomatic processes. Only the latter – the rarest one – is of archaeologic interest. Fine-grained eclogites deriving from metasomatic events can also be recognized by the extreme compositional variability of the sodic pyroxene, ranging from jadeite to omphacite. These features, which are typical of most archaeologic tools, are geologically observed only in the metaophiolites of the Monviso and Voltri massifs (e.g., in Brignano Frascata: see Figs. 9 and 10 in [46]). These metasomatic processes brought to variations in the bulk chemical composition of the rocks, a phenomenon occurring only along shear zones, where repeated influxes of aqueous fluids with different compositions enter the system. Such an occurrence also justifies the extreme scattering and scarceness of these ‘ jades ’ on a geologic level. Despite this, these lithologies were extremely suitable for the preparation of implements, due their technological features (e.g., density, hardness, toughness, workability and appeal) – and thus painstakingly sought after by our Neolithic ancestors (possibly, the first ‘petrologists’) even in impervious places, for the manufacture of artefacts then to be traded all over Europe. Therefore, basing on their mineral-petrographic features and chemistry, several clues confirm that the HP -metaophiolites used to produce the prehistoric tools from the Rocca di Cavour originate from analogous lithotypes of the Monviso metamorphic complex – which is consistent, under logical deduction, with the proximity of this supply source. Our results also confirm the conclusions of a previous archaeologic survey [38], claiming that a preliminary shaping of the greenstone raw materials was performed on site by using ophiolitic pebbles and cobbles from the Quaternary alluvial deposits of the Pellice stream or a palaeo-bed of the Po River (in which they concentrate, being more resistant to erosion). Several tools, in fact, still preserve relict surfaces traceable to their original pebble/cobble shapes. Declarations Data availability Data reported in the manuscript or in the Supplementary Information will be rendered available on request. Acknowledgements This article is dedicated to the memory of Dino Delcaro , a friend and experimental archaeologist who sadly passed away in 2022, with whom we exchanged over the years samples and information about greenstones from the Monviso Massif. Six of his samples are discussed here. 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Also discoverable on Platform About Our Team In Review Editorial Policies Advisory Board Help Center Resources Author Services Accessibility API Access RSS feed Manage Cookie Preferences © Research Square 2026 | ISSN 2693-5015 (online) Privacy Policy Terms of Service Do Not Sell My Personal Information {"props":{"pageProps":{"initialData":{"identity":"rs-9051667","acceptedTermsAndConditions":true,"allowDirectSubmit":false,"archivedVersions":[],"articleType":"Article","associatedPublications":[],"authors":[{"id":604947413,"identity":"31661985-9a2b-4e7b-9c76-081aa55c3249","order_by":0,"name":"Roberto Giustetto","email":"data:image/png;base64,iVBORw0KGgoAAAANSUhEUgAAAZAAAAAyAQMAAABI0h/eAAAABlBMVEX///8AAABVwtN+AAAACXBIWXMAAA7EAAAOxAGVKw4bAAABBElEQVRIie2RMUvEMBSA31FIl4ddX+C4/oWUQrp0928EDjp1Pk4QCRzo4uEs/gzBuaHgFG72uEVxdai4nCBiDtpBaXurQ77lwZd8vEAAPJ5/CbYz6ESoAZSbbDRRbVKBIMDKCWfYYNMl0CWkYHRNdrU2r2f7HOJTTD+a5ddFxN/k84szJ7HuTaZ2M0+sKiCpUVJlBfG7MhPKmaGHEZWSa1VDskIJ5lKQ2JWSlDMjSfbZJmljvl2ytUcTOTkkcYCCjHbJEx5JcDPnuihQBGxB9jHlt9fFgpQzjKn+JFybd53ns/imvm+W57MoCusHvj+YVdW/pgXF33Psu/aLgU/weDweD8APUINP/xfBmY4AAAAASUVORK5CYII=","orcid":"","institution":"University of Turin","correspondingAuthor":true,"prefix":"","firstName":"Roberto","middleName":"","lastName":"Giustetto","suffix":""},{"id":604947414,"identity":"3b274792-16a4-485f-9f6e-d6534fb680a9","order_by":1,"name":"Michele Borgogno","email":"","orcid":"","institution":"University of Turin","correspondingAuthor":false,"prefix":"","firstName":"Michele","middleName":"","lastName":"Borgogno","suffix":""},{"id":604947415,"identity":"9db754ad-c5c6-4eec-871c-17bf75f22881","order_by":2,"name":"Luca Barale","email":"","orcid":"","institution":"National Research Council","correspondingAuthor":false,"prefix":"","firstName":"Luca","middleName":"","lastName":"Barale","suffix":""},{"id":604947416,"identity":"1ed8f065-f600-4f19-8428-b21d08c3c496","order_by":3,"name":"Ursula Perrone","email":"","orcid":"","institution":"University of Turin","correspondingAuthor":false,"prefix":"","firstName":"Ursula","middleName":"","lastName":"Perrone","suffix":""},{"id":604947417,"identity":"f993df6a-5fe7-4afa-baaa-d5f7883a8290","order_by":4,"name":"Roberto Compagnoni","email":"","orcid":"","institution":"University of Turin","correspondingAuthor":false,"prefix":"","firstName":"Roberto","middleName":"","lastName":"Compagnoni","suffix":""}],"badges":[],"createdAt":"2026-03-06 14:38:34","currentVersionCode":1,"declarations":"","doi":"10.21203/rs.3.rs-9051667/v1","doiUrl":"https://doi.org/10.21203/rs.3.rs-9051667/v1","draftVersion":[],"editorialEvents":[],"editorialNote":"","failedWorkflow":false,"files":[{"id":104781360,"identity":"acf8381b-42a3-4e1b-abc8-6814d727b642","added_by":"auto","created_at":"2026-03-17 07:55:31","extension":"png","order_by":1,"title":"Figure 1","display":"","copyAsset":false,"role":"figure","size":2556154,"visible":true,"origin":"","legend":"\u003cp\u003eThe \u003cem\u003eRocca di Cavour\u003c/em\u003e topographic map (redrawn after Cinquetti, 1985 [32,33]), with location of the archaeological finds. The small inset on the right shows the geographical position of the \u003cem\u003eRocca\u003c/em\u003e(yellow star) in the Piedmont Region (in red), Northwestern Italy.\u003c/p\u003e","description":"","filename":"Fig1.png","url":"https://assets-eu.researchsquare.com/files/rs-9051667/v1/13e7834d278ec85421e4fbd3.png"},{"id":105033749,"identity":"5d3fb31c-878b-4369-8335-314861c77cb6","added_by":"auto","created_at":"2026-03-20 07:21:33","extension":"png","order_by":2,"title":"Figure 2","display":"","copyAsset":false,"role":"figure","size":2143045,"visible":true,"origin":"","legend":"\u003cp\u003eSelected implements representative of the Rocca di Cavour polished \u003cem\u003egreenstone\u003c/em\u003eindustry: 1) axehead fragment (inv. code: 1327/25); 2) axehead fragment (inv. code: 1327/1); 3) axehead (inv. code: 69232; analytical code: PIEM81; 4) cutting-edge (inv. code: 1327/16); 5) striker (inv. code: 69233/180) (from Zamagni, 1996 [38]).\u003c/p\u003e","description":"","filename":"Fig2.png","url":"https://assets-eu.researchsquare.com/files/rs-9051667/v1/fe00583cdcdb7921853f2be9.png"},{"id":104569925,"identity":"948a93db-f566-4f80-b672-8cb47a705a8e","added_by":"auto","created_at":"2026-03-13 12:33:33","extension":"png","order_by":3,"title":"Figure 3","display":"","copyAsset":false,"role":"figure","size":3619767,"visible":true,"origin":"","legend":"\u003cp\u003eSimplified geotectonic sketch-map of the central portion of the Monviso Massif Meta-ophiolite Complex between Varaita and Pellice valleys (redrawn after Blake et al., 1995 [39], and updated with data from Scaramuzzo et al., 2026 [40]). The basal \u003cem\u003eserpentinite \u003c/em\u003e(\u003cstrong\u003es\u003c/strong\u003e: yellow-green) is the tectonic unit that includes most of the primary outcrops of fine-grained \u003cem\u003ejadeitite\u003c/em\u003e + \u003cem\u003eomphacitite\u003c/em\u003e + \u003cem\u003eNa-pyroxenite\u003c/em\u003e (named jadeitite by most archeologists) and \u003cem\u003eeclogite, \u003c/em\u003ethe Neolithic man's favorite rocks to build on the tools. The rectangle bounded by a white dashed line corresponds to the area mapped in detail by Pétrequin et al. (2006) [22] and partly by Forno et al. (2015) [30].\u003c/p\u003e","description":"","filename":"Fig3.png","url":"https://assets-eu.researchsquare.com/files/rs-9051667/v1/bdabede744b743e78e9c36e2.png"},{"id":104781875,"identity":"652a9e01-a375-4d8d-8415-72dcaea53a5d","added_by":"auto","created_at":"2026-03-17 07:56:30","extension":"png","order_by":4,"title":"Figure 4","display":"","copyAsset":false,"role":"figure","size":3421826,"visible":true,"origin":"","legend":"\u003cp\u003e(a) Density histogram of the \u003cem\u003egreenstone\u003c/em\u003earchaeological artefacts of the Rocca di Cavour; (b) Pie chart showing the percentage of all lithologies found in archaeological artefacts.\u003c/p\u003e","description":"","filename":"Fig4.png","url":"https://assets-eu.researchsquare.com/files/rs-9051667/v1/44bc59c26dba9d2ced343e01.png"},{"id":104781566,"identity":"431e8c1a-577f-4e4d-ada0-9d136713ed60","added_by":"auto","created_at":"2026-03-17 07:55:55","extension":"png","order_by":5,"title":"Figure 5","display":"","copyAsset":false,"role":"figure","size":668284,"visible":true,"origin":"","legend":"\u003cp\u003eXRPD patterns of selected \u003cem\u003eRocca di Cavour\u003c/em\u003e implements: (\u003cstrong\u003ea\u003c/strong\u003e) jadeitite (green; invent. code: 69232 – analyt. code: PIEM81), omphacitite (red; invent. code: V11 – analyt. code: PIEM89) and mixed Na-pyroxenite (blue; invent. code: 1327/A10). The reflections of Na-pyroxenes are unique – though slightly shifted – when a single phase exists with a given chemistry (either jadeite or omphacite: green and red patterns, respectively). Instead, most reflections are split [including (‑221), (310) and (002)] when both jadeite and omphacite are present in significant amounts (blue pattern). (\u003cstrong\u003eb\u003c/strong\u003e) Enlargement of a mixed Na-pyroxenite pattern in the 29 to 38 2θ-degrees range, which is enhancing the splitting of the 3 peaks sensitive to composition.\u003c/p\u003e","description":"","filename":"Fig5.png","url":"https://assets-eu.researchsquare.com/files/rs-9051667/v1/472df2b02b4552198d557bf7.png"},{"id":104569918,"identity":"80932499-d34f-4800-8c3d-c48c9554bf5f","added_by":"auto","created_at":"2026-03-13 12:33:33","extension":"png","order_by":6,"title":"Figure 6","display":"","copyAsset":false,"role":"figure","size":498033,"visible":true,"origin":"","legend":"\u003cp\u003e(\u003cstrong\u003ea\u003c/strong\u003e) Classification diagram of Na-pyroxenes based on Jd (jadeite), Aeg (aegirine) and Q (Wo+En+Fs) end-members [52]; (\u003cstrong\u003eb\u003c/strong\u003e) Average chemical composition of the archaeologic \u003cem\u003egreenstone Na-pyroxenes\u003c/em\u003e from Rocca di Cavour (green spots) and from geologic samples from the upper Po valley (red spots), as estimated from the XRPD data (cf., [16]).\u003c/p\u003e","description":"","filename":"Fig6.png","url":"https://assets-eu.researchsquare.com/files/rs-9051667/v1/17c2e1ad14c6fbf0fd95c2e6.png"},{"id":104781586,"identity":"aebcd437-023f-49ed-a526-74ddb71ae5cd","added_by":"auto","created_at":"2026-03-17 07:55:58","extension":"png","order_by":7,"title":"Figure 7","display":"","copyAsset":false,"role":"figure","size":31177964,"visible":true,"origin":"","legend":"\u003cp\u003ePhotomicrographs of representative samples observed under the optical microscope at plane-polarized light (PPL) [\u003cstrong\u003e(a)\u003c/strong\u003e to \u003cstrong\u003e(d)\u003c/strong\u003e: \u003cem\u003eRocca di Cavour\u003c/em\u003eNeolithic implements; \u003cstrong\u003e(e)\u003c/strong\u003e and \u003cstrong\u003e(f)\u003c/strong\u003e: Geologic samples from the upper Po valley and alluvial deposits]. Mineral symbols follow Warr (2021). (\u003cstrong\u003ea\u003c/strong\u003e) \u003cem\u003eEclogite\u003c/em\u003ewith atoll-like garnets (Grt) in a fine-grained omphacite (Omp) matrix (PIEM80). (\u003cstrong\u003eb\u003c/strong\u003e) \u003cem\u003eEclogite\u003c/em\u003e with mylonitic structure and zoisite/clinozoisite+white mica pseudomorph (blackish area) after original lawsonite (PIEM86). (\u003cstrong\u003ec\u003c/strong\u003e) \u003cem\u003eGarnet-omphacitite\u003c/em\u003e, with a very fine-grained omphacite matrix (Omp) including euhedral garnets (Grt) with tiny inclusions of omphacite and zircon at the core; an allanite grain (Aln) and two zircons (Zrn) are also observed; a rough foliation is highlighted by preferred orientation of rutile (Rt) (PIEM85). (\u003cstrong\u003ed\u003c/strong\u003e) \u003cem\u003eJadeitite\u003c/em\u003e with granoblastic microstructure; acicular rutile crystals and tiny omphacite exsolutions cause the jadeite core to be murky (PIEM81). (\u003cstrong\u003ee\u003c/strong\u003e) \u003cem\u003eEclogite\u003c/em\u003e with fine grain-size; Na-pyroxenes are zoned with a greenish core and a paler rim (OF2780). (\u003cstrong\u003ef\u003c/strong\u003e) Fine-grained \u003cem\u003eeclogite\u003c/em\u003e crossed by long nematoblasts of zoned glaucophane (Gln) (OF2764).\u003c/p\u003e","description":"","filename":"Fig7.png","url":"https://assets-eu.researchsquare.com/files/rs-9051667/v1/9397967bc218bd45dd04ee5a.png"},{"id":104569921,"identity":"030f22c7-6c55-490d-9e27-9170fbc4a067","added_by":"auto","created_at":"2026-03-13 12:33:33","extension":"png","order_by":8,"title":"Figure 8","display":"","copyAsset":false,"role":"figure","size":11341745,"visible":true,"origin":"","legend":"\u003cp\u003eBack-Scattered Electron (BSE) images of representative thin sections observed at SEM. [(\u003cstrong\u003ea\u003c/strong\u003e) to (\u003cstrong\u003ed\u003c/strong\u003e): \u003cem\u003eRocca di Cavour\u003c/em\u003eNeolithic implements; (\u003cstrong\u003ee\u003c/strong\u003e) and (\u003cstrong\u003ef\u003c/strong\u003e): Meta-ophiolite samples from primary outcrops and secondary alluvial deposits of the Monviso massif along the upper Po valley. (\u003cstrong\u003ea\u003c/strong\u003e) \u003cem\u003eEclogite\u003c/em\u003e: Greenschist-facies retrogressed portion with clinozoisite (Czo), Mg-chlorite (Chl) and albite (Ab) preserving small relics of omphacite (Omp) (PIEM77). (\u003cstrong\u003eb\u003c/strong\u003e) \u003cem\u003eEclogite\u003c/em\u003e: Atoll-like garnets (Grt) in a matrix of zoned omphacite (Omp) (PIEM80; cfr. Fig. 6.a). (\u003cstrong\u003ec\u003c/strong\u003e) \u003cem\u003eJadeitite\u003c/em\u003e: detail of a jadeite crystal (dark grey) with drop-like omphacite exsolutions at the core and surrounded by a thin omphacite rim (light grey) (PIEM81). (\u003cstrong\u003ed\u003c/strong\u003e) \u003cem\u003eJadeitite\u003c/em\u003e with different portions: on the left side, jadeite blasts (Jd: dark grey) cemented by interstitial omphacite (Omp: light grey); on the right side, retrogressed portion with Na-pyroxene mostly replaced by albite (Ab) and epidote (Ep) (PIEM82). (\u003cstrong\u003ee\u003c/strong\u003e) \u003cem\u003eEclogite\u003c/em\u003e: weakly oriented grano-nematoblastic structure, due to the alignment of a zoned pyroxene (Omp) and ilmenite nematoblasts (Ilm); garnets, at times with atoll-like structure (Grt), are also observed (OF2780). (\u003cstrong\u003ef\u003c/strong\u003e) \u003cem\u003eJadeitite\u003c/em\u003ewith granoblastic microstructure; jadeite crystals (Jd: dark grey), with drop-like omphacite exsolutions in the core, are surrounded by interstitial omphacite (Omp: light grey) (OF2788).\u003c/p\u003e","description":"","filename":"Fig8.png","url":"https://assets-eu.researchsquare.com/files/rs-9051667/v1/452c30a377473da6b7de2ab2.png"},{"id":104569923,"identity":"2ca64c14-7a66-425a-a1d2-0edc846fb30e","added_by":"auto","created_at":"2026-03-13 12:33:33","extension":"png","order_by":9,"title":"Figure 9","display":"","copyAsset":false,"role":"figure","size":8986364,"visible":true,"origin":"","legend":"\u003cp\u003eSEM-EDS analyses of Na-pyroxenes and garnets, plotted on the Morimoto et al. (1988) [52] and Grs, (Alm+Sps), Prp ternary diagrams, respectively) (\u003cstrong\u003ea\u003c/strong\u003e) Neolithic implements from the \u003cem\u003eRocca di Cavour\u003c/em\u003e archaeological site; (\u003cstrong\u003eb\u003c/strong\u003e) HP-meta-ophiolites from the Monviso Complex (C: core composition; R: rim composition). The red dot indicates the average composition of coexisting Na-pyroxenes, as inferred from XRPD data (cf., [16]).\u003c/p\u003e","description":"","filename":"Fig9.png","url":"https://assets-eu.researchsquare.com/files/rs-9051667/v1/579da88276e2e079398668ad.png"},{"id":105036514,"identity":"07da1f4d-4a5b-4ce8-9c99-333743a3050f","added_by":"auto","created_at":"2026-03-20 07:33:55","extension":"pdf","order_by":0,"title":"","display":"","copyAsset":false,"role":"manuscript-pdf","size":60712120,"visible":true,"origin":"","legend":"","description":"","filename":"manuscript.pdf","url":"https://assets-eu.researchsquare.com/files/rs-9051667/v1/205691bf-c03c-4816-9a83-ee1fa796507f.pdf"},{"id":104569919,"identity":"d971004b-f829-4b88-abe8-f607ae9d08b7","added_by":"auto","created_at":"2026-03-13 12:33:33","extension":"docx","order_by":1,"title":"","display":"","copyAsset":false,"role":"supplement","size":158828,"visible":true,"origin":"","legend":"","description":"","filename":"GiustettoetalGreenstoneCavourSupplMat.docx","url":"https://assets-eu.researchsquare.com/files/rs-9051667/v1/9d0eefac6d81bc8e0253d6ac.docx"},{"id":104569916,"identity":"d2afc8d0-d269-4ef4-b092-565725c7d1e8","added_by":"auto","created_at":"2026-03-13 12:33:33","extension":"png","order_by":2,"title":"","display":"","copyAsset":false,"role":"supplement","size":3284388,"visible":true,"origin":"","legend":"\u003cp\u003e\u003cstrong\u003eGraphical abstract\u003c/strong\u003e\u003c/p\u003e","description":"","filename":"GraphicalAbstract.png","url":"https://assets-eu.researchsquare.com/files/rs-9051667/v1/ec86df867a3aee19add9660b.png"}],"financialInterests":"No competing interests reported.","formattedTitle":"Neolithic artefacts in ‘Jade’ from Rocca di Cavour (Northwestern-Italy): archaeometric characterization, geologic contextualization and provenance","fulltext":[{"header":"Introduction","content":"\u003cp\u003eThe Neolithic period can be considered the first technological era of mankind [\u003cspan citationid=\"CR1\" class=\"CitationRef\"\u003e1\u003c/span\u003e]. In Europe, humans abandoned their nomadic life and began to settle in the flat lands to the South of the Alpine chain (close to the present towns of Alessandria, Asti and Alba of the Piedmont region, Northwestern Italy), dedicating to agriculture and breeding. This innovative lifestyle required apt tools to be forged and used, in order to satisfy new circumstances and necessities, e.g., logging, house building and agriculture. From the early Neolithic (VI millennium BC) until the Bronze Age (II millennium BC), the industry of ceramics and polished stone flourished, both in production and trades. The latter, in particular, was represented by implements (e.g., axeheads, chisels) and ornamental tools (e.g., disc-rings and pendants) requiring both toughness and eye-appeal. They are mostly made of \u003cem\u003egreenstone\u003c/em\u003e, a heterogeneous group of rocks \u0026ndash; including \u0026lsquo;\u003cem\u003ejades\u003c/em\u003e\u0026rsquo; \u0026ndash; which derive from the high-pressure metamorphic ophiolites (hereafter referred to as \u003cem\u003eHigh-Pressure \u0026ndash; HP \u0026ndash; meta-ophiolites\u003c/em\u003e) of the Internal Piemonte Zone in the Western Alps (e.g., [\u003cspan citationid=\"CR2\" class=\"CitationRef\"\u003e2\u003c/span\u003e, \u003cspan citationid=\"CR3\" class=\"CitationRef\"\u003e3\u003c/span\u003e]). Under the term \u0026lsquo;\u003cem\u003ejade\u003c/em\u003e\u0026rsquo;, both \u0026lsquo;\u003cem\u003ejadeite-jade\u003c/em\u003e\u0026rsquo; (pyroxenes of the jadeite/diopside/aegirine solid solution) and \u0026lsquo;\u003cem\u003enephrite-jade\u003c/em\u003e\u0026rsquo; [amphiboles of the tremolite/ferro-actinolite solid solution] are comprised; however, only the former will be considered hereafter [\u003cspan additionalcitationids=\"CR5 CR6\" citationid=\"CR4\" class=\"CitationRef\"\u003e4\u003c/span\u003e\u0026ndash;\u003cspan citationid=\"CR7\" class=\"CitationRef\"\u003e7\u003c/span\u003e]. Neolithic implements similar to those found in the Western Po plain were widespread throughout continental Europe and beyond: polished tools in \u003cem\u003egreenstone\u003c/em\u003e were retrieved along a large stripe roughly oriented North-to-South, from Great Britain to Malta (e.g., [\u003cspan additionalcitationids=\"CR9 CR10\" citationid=\"CR8\" class=\"CitationRef\"\u003e8\u003c/span\u003e\u0026ndash;\u003cspan citationid=\"CR11\" class=\"CitationRef\"\u003e11\u003c/span\u003e]) and extending also westwards (in Southern and Northern France) and eastwards (Northeastern Italy and beyond). Sporadically, these tools have also been retrieved as far as Slovakia, Czech Republic and Hungary (e.g., [\u003cspan additionalcitationids=\"CR13 CR14\" citationid=\"CR12\" class=\"CitationRef\"\u003e12\u003c/span\u003e\u0026ndash;\u003cspan citationid=\"CR15\" class=\"CitationRef\"\u003e15\u003c/span\u003e]).\u003c/p\u003e \u003cp\u003eThese HP meta-ophiolites \u0026ndash; with green colour, remarkable hardness and toughness \u0026ndash; are aptly described in the literature (e.g., [\u003cspan citationid=\"CR16\" class=\"CitationRef\"\u003e16\u003c/span\u003e], with references therein) and classified in \u003cem\u003etwo groups\u003c/em\u003e. The \u003cem\u003efirst one\u003c/em\u003e includes \u003cb\u003eNa-pyroxenites\u003c/b\u003e (commonly referred to as \u0026lsquo;\u003cem\u003ejades\u003c/em\u003e\u0026rsquo;), consisting of pyroxene solid solutions between Na and Ca end-members, whose composition is represented in the ternary diagram including \u003cem\u003ejadeite\u003c/em\u003e (Jd: NaAlSi\u003csub\u003e2\u003c/sub\u003eO\u003csub\u003e6\u003c/sub\u003e), \u003cem\u003eaegirine\u003c/em\u003e (Aeg: NaFe\u003csup\u003e3+\u003c/sup\u003eSi\u003csub\u003e2\u003c/sub\u003eO\u003csub\u003e6\u003c/sub\u003e), and \u003cem\u003ecalcium components\u003c/em\u003e Q (Wo\u0026thinsp;+\u0026thinsp;En\u0026thinsp;+\u0026thinsp;Fs) (Morimoto et al., 1988). The most widespread rocks of this group are named \u003cem\u003ejadeitite\u003c/em\u003e, if jadeite\u0026thinsp;\u0026gt;\u0026thinsp;95 vol. %, \u003cem\u003eomphacitite\u003c/em\u003e, if \u003cem\u003eomphacite\u003c/em\u003e [(Na,Ca)(Al,Mg)Si\u003csub\u003e2\u003c/sub\u003eO\u003csub\u003e6\u003c/sub\u003e]\u0026thinsp;\u0026gt;\u0026thinsp;95 vol. %, and \u003cem\u003emixed Na-pyroxenite\u003c/em\u003e, if both \u003cem\u003ejadeite\u003c/em\u003e and \u003cem\u003eomphacite\u003c/em\u003e occur in similar amounts. The \u003cem\u003esecond group\u003c/em\u003e, which includes \u003cb\u003eNa-pyroxene\u0026thinsp;+\u0026thinsp;garnet rocks\u003c/b\u003e, comprehends \u003cem\u003eeclogite\u003c/em\u003e if the modal omphacite/garnet ratio % is in the 25\u0026ndash;75 range and \u003cem\u003egarnet-omphacitite\u003c/em\u003e if the modal amount of garnet is \u0026lt;\u0026thinsp;25 vol. % [\u003cspan citationid=\"CR17\" class=\"CitationRef\"\u003e17\u003c/span\u003e]. These \u003cem\u003egreenstones sensu stricto\u003c/em\u003e (\u003cem\u003es.s\u003c/em\u003e.) occur in HP meta-ophiolite units derived from the Liguria-Piemonte oceanic domain (e.g., [\u003cspan citationid=\"CR18\" class=\"CitationRef\"\u003e18\u003c/span\u003e]), which underwent Alpine metamorphism under eclogite-facies conditions (e.g., [\u003cspan citationid=\"CR2\" class=\"CitationRef\"\u003e2\u003c/span\u003e]). In the field, they outcrop either as small (few m\u003csup\u003e3\u003c/sup\u003e), rare and mostly unmapped boulders at high altitude in the Monviso or Voltri meta-ophiolitic massifs [\u003cspan additionalcitationids=\"CR20 CR21 CR22 CR23 CR24\" citationid=\"CR19\" class=\"CitationRef\"\u003e19\u003c/span\u003e\u0026ndash;\u003cspan citationid=\"CR25\" class=\"CitationRef\"\u003e25\u003c/span\u003e], or as pebbles/cobbles in secondary Oligocene conglomerates of the Tertiary Piemonte Basin and Quaternary alluvial deposits, derived from the dismantling of the primary outcrops [\u003cspan additionalcitationids=\"CR27 CR28 CR29 CR30\" citationid=\"CR26\" class=\"CitationRef\"\u003e26\u003c/span\u003e\u0026ndash;\u003cspan citationid=\"CR31\" class=\"CitationRef\"\u003e31\u003c/span\u003e]. As such, \u003cem\u003egreenstones s.s.\u003c/em\u003e represent very important archeometric markers, useful for identifying these artefacts supply sources and tracing trade routes. However, under the generic term \u0026lsquo;\u003cem\u003egreenstone\u0026rsquo;\u003c/em\u003e, other lithotypes (e.g., serpentinite, amphibolite and prasinite) are also included by archeologists, since sharing the same colour. Seldom, also glaucophanite \u0026ndash; a HP-rock mainly consisting of blue-amphibole \u0026ndash; is inserted. These rocks, also used for producing Paleolithic and Neolithic implements, are \u0026ndash; with few exceptions \u0026ndash; less significant from an archeometric point of view, due to their ubiquitous distribution in the Western Alps (e.g., [\u003cspan citationid=\"CR31\" class=\"CitationRef\"\u003e31\u003c/span\u003e]).\u003c/p\u003e \u003cp\u003eThis study concerns the characterization \u0026ndash; with non- or micro-destructive archaeometric techniques \u0026ndash; of the polished \u003cem\u003egreenstones\u003c/em\u003e tools from the archeological site of \u003cem\u003eRocca di Cavour\u003c/em\u003e, currently held in the Archeological Museum of Turin. These outcomes are compared to those of similar geological specimens collected during a geologic survey of the right orographic side of the upper Po valley and alluvial sediments, considered as the most probable source area for the raw materials.\u003c/p\u003e"},{"header":"Methods","content":"\u003cp\u003e\u003cem\u003eArchaeological context\u003c/em\u003e\u0026nbsp;\u003c/p\u003e\n\u003cp\u003eThe \u003cem\u003eRocca di Cavour\u003c/em\u003e (10061 Cavour, Metropolitan City of Turin, Piedmont region, Northwestern Italy: Fig. 1, redrawn after Cinquetti, [32,33]) is a typical \u003cem\u003eInselberg\u003c/em\u003e, i.e., an isolated hill (432 m a.s.l.) standing up ca. 130 m above the surrounding alluvial plain. Geologically, the \u003cem\u003eRocca\u003c/em\u003e is a remnant of metamorphic rocks that escaped fluvial erosion and glacial exaration at the mouth of the Pellice Valley. Geophysical data [34] show that it is connected under the Quaternary cover with the eastern margin of the continental Dora-Maira Massif. The \u003cem\u003eRocca\u003c/em\u003e is made up of a foliated leucogranite (protolith age: 304 \u0026plusmn; 2 Ma [35]) exposed in the central and southern area of the hill, where dark mafic microgranular enclaves and pegmatitic dykes are recognizable in spite of the Alpine tectono-metamorphic overprint. The original intrusive contact with the host micaschists of the Dora-Maira pre-granitic basement, exposed at the northwestern top of the hill, has been completely transposed, but xenoliths of the country rocks and aplitic dykes are still identified.\u003c/p\u003e\n\u003cp\u003eDespite an important anthropization, significant traces of a prehistoric attendance are still evident, especially on the Northern and Western sides. Surface prospections, performed under the supervision of the Archaeological Superintendence of Piedmont and the \u0026lsquo;\u003cem\u003eCentro Studi e Museo di Arte Preistorica\u003c/em\u003e\u0026rsquo; (Center of Studies and Museum of Prehistoric Art) of Pinerolo, brought to the retrieval of several artefacts, splinters and an axe-shaped pebble made in \u003cem\u003egreenstone\u003c/em\u003e.\u003c/p\u003e\n\u003cp\u003eThe recovered polished stone industry of the \u003cem\u003eRocca\u003c/em\u003e consists of 98 objects \u0026ndash; mainly fragmented axehead roughouts, chisels and splinters in \u003cem\u003egreenstone\u003c/em\u003e \u0026ndash; found in three different areas (Western, Southeastern and Northern slopes [36]), together with ceramics and splintered stone items [37]. The archaeologic surveys showed that a preliminary shaping of the \u003cem\u003egreenstone\u003c/em\u003e raw materials was presumably performed on site. All steps of the production chain were carried out on site, except the choice of pebbles and boulders with proper shape and lithology and gross splintering/shaping, presumably performed on the collection site. The retrieved axehead roughouts (and other tools) testify that a consolidated production chain existed, including finer splintering (performed by using spheroidal pebbles as strikers), bush-hammering (to eliminate sharp edges) and polishing (to smoothen the tool surface). Splintering is justified by 50 (out of 98) samples from decortexing of the lithic support; on 17 of these, traces of percussion with a striker are evident [38]. Few are the polished objects \u0026ndash; namely 2 cutting-edges, in which polishing is observed close to the blade, with bush-hammered borders presumably to facilitate grip. Several fragmented axe heels and unpolished cutting edges are present, with 3 sub-circular strikers and a single chisel (Fig. 2). The \u003cem\u003eRocca di Cavour\u003c/em\u003e must therefore be considered an \u003cem\u003eatelier\u003c/em\u003e site, in which only the initial steps of the production chain were performed, forming several scraps and wastes that were left in place, eventually to be reworked for other purposes (Zamagni, 1996).\u003c/p\u003e\n\u003cp\u003e\u003cem\u003eThe Monviso meta-ophiolite Complex\u003c/em\u003e\u0026nbsp;\u003c/p\u003e\n\u003cp\u003eA quick examination of the archaeological finds revealed that they consist of \u003cem\u003egreenstone\u003c/em\u003e; as such, they cannot derive from the Rocca substratum. The research for the supply sources was thus shifted to the nearby Monviso massif (Fig. 3, redrawn after Blake et al., 1995 [39]). The Monviso Meta-ophiolite (MMM) Complex is a geological body elongated N-S for 35 km, from the \u003cem\u003eVal\u003c/em\u003e \u003cem\u003eVaraita\u003c/em\u003e to \u003cem\u003eVal\u003c/em\u003e \u003cem\u003ePellice\u003c/em\u003e, with a maximum thickness of 6-7 km. The Complex is bounded by two main tectonic contacts, which separate it to the W from the blueschist-facies calc-schists (\u0026ldquo;schistes lustr\u0026eacute;s\u0026rdquo;) of the internal Piemonte Zone and to the E from the eclogite-facies continental basement of the Dora-Maira Massif [40]. The Monviso complex belongs to the eclogite-facies Internal Piemonte Zone and consists of several tectonometamorphic units, some of which re-equilibrated at Ultra-High-Pressure (UHP) conditions in the coesite stability field ([41], with refs. therein).\u003c/p\u003e\n\u003cp\u003eIn spite of the Alpine polyphase tectono-metamorphic overprint, the westernmost unit (Fig. 3) best preserves a complete oceanic sequence consisting of basal isotropic and locally layered gabbros, intermediate massive and pillowed basalts, capped by a sedimentary quartz-rich cover [42]. The most interesting unit from an archaeometric point of view is the easternmost \u003cem\u003ebasal serpentinite\u003c/em\u003e (\u003cstrong\u003es\u003c/strong\u003e in Fig. 3), containing small outcrops \u0026ndash; specifically indicated here \u0026ndash; of fine-grained \u003cem\u003ejadeitite\u003c/em\u003e (blue dots in Fig. 3) and \u003cem\u003eeclogite\u003c/em\u003e (red dots in Fig. 3), [22,24,25,30,43].\u0026nbsp;\u003c/p\u003e\n\u003cp\u003eFor comparison with the \u003cem\u003eRocca di Cavour\u003c/em\u003e archaeological implements, 10 \u003cem\u003egreenstone s.s\u003c/em\u003e geological samples were collected in the basal serpentinite from both primary outcrops in the upper Po Valley and alluvial conglomeratic deposits exposed at its mouth on the Po plain [44]. Also, six fine-grained eclogite-facies samples from the Quaternary alluvial sediments of the Po were collected and kindly provided by Dino Delcaro. Two fine-grained eclogites from the Val Carbonieri (Fig. 3), whose preliminary petrology and chemistry appeared in a previous paper [45], were also considered.\u0026nbsp;\u003c/p\u003e\n\u003cp\u003e\u003cem\u003eAnalytical methods\u003c/em\u003e\u0026nbsp;\u003c/p\u003e\n\u003cp\u003eA preliminary rock identification of all 98 lithic implements from the \u003cem\u003eRocca di Cavour\u003c/em\u003e site, previously classified by archaeologists on morphological and stylistic basis [38], was carried out by means of \u003cem\u003etwo non-invasive methods\u003c/em\u003e: \u003cem\u003ei)\u003c/em\u003e \u003cem\u003eStereo-microscopic observations\u003c/em\u003e, which allowed performing a preliminary \u003cem\u003egreenstone\u003c/em\u003e screening, discriminating eclogites through the identification of garnets and recognizing primary and secondary compositional heterogeneities and/or peculiar microstructures (e.g., [46,47]). Since a classification solely based on optical observation can be misleading for the fine to very-fine grain-size of minerals, \u003cem\u003eii)\u003c/em\u003e \u003cem\u003edensity determination\u003c/em\u003e was also performed, which is very useful for homogeneous rocks devoid of retrogression. Moreover, some artefacts (selected among incomplete tools) were analyzed through more in-depth \u003cem\u003emicro-invasive coring\u003c/em\u003e \u003cem\u003emethods\u003c/em\u003e. From each drill core sample (10 mm across) \u0026ndash; representative of the rock composition, since the grain-size is systematically fine to very fine (e.g., [16,26,48]) \u0026ndash; a petrographic thin section was obtained and the rest powdered in an agate mortar.\u003c/p\u003e\n\u003cp\u003eThin sections were examined under an \u003cstrong\u003e\u003cem\u003eoptical polarized-light microscope\u003c/em\u003e\u003c/strong\u003e \u003cstrong\u003e\u003cem\u003eZeiss WL Pol\u003c/em\u003e\u003c/strong\u003e to recognize rock microstructure and mineralogy. After carbon-coating, the chemical composition of major, minor and accessory minerals was studied by \u003cstrong\u003e\u003cem\u003eScanning Electron Microscopy with Energy-Dispersive-Spectrometry\u003c/em\u003e\u003c/strong\u003e\u003cem\u003e\u0026nbsp;\u003c/em\u003e(SEM-EDS), using a Cambridge Stereoscan 360 SEM equipped with an EDS Energy 200 and a Pentafet detector (Oxford Instruments). The operating conditions were: 50 s counting time, 15 kV accelerating voltage, 25 mm working distance, 300 pA beam current. SEM-EDS quantitative data (spot size = 2 \u003cem\u003e\u0026mu;\u003c/em\u003em) were acquired and managed using the Microanalysis Suite Issue 12, INCA Suite version 4.08; the raw data were calibrated on natural mineral standards and the \u0026Phi;\u0026rho;Z correction [49] was applied. The Fe\u003csup\u003e3+\u0026nbsp;\u003c/sup\u003e\u0026frasl; Fe ratio in garnet and omphacite has been estimated by stoichiometry from the SEM-EDS analyses. Since eclogites consist of coexisting garnet and omphacite, the calibration of Powell (1985) [50] of the \u003cstrong\u003e\u003cem\u003egeothermometer\u003c/em\u003e\u003c/strong\u003e based on the Mg/Fe partitioning (K\u003csub\u003eD\u003c/sub\u003e) between these minerals was applied.\u003c/p\u003e\n\u003cp\u003ePowders were analyzed with \u003cstrong\u003e\u003cem\u003eX-ray powder diffraction\u003c/em\u003e\u003c/strong\u003e\u003cstrong\u003e\u003cem\u003e\u0026nbsp;\u003c/em\u003e\u003c/strong\u003e(XRPD), capable of evaluating the relative mineral modal amounts in fine-grained rocks. Data were collected in the 5\u0026deg;-50\u0026deg; 2q range on an automated Siemens D-5000 diffractometer with q/2q setup in Bragg-Brentano geometry, with Cu-Ka radiation and a zero-background sample holder, and processed with the Diffrac Plus (2005) [51] software (EVA 11,00,3).\u003c/p\u003e"},{"header":"Results","content":"\u003cp\u003e\u003cem\u003eStereo-microscopy and density measure\u0026nbsp;\u003c/em\u003e\u003c/p\u003e\n\u003cp\u003eSince these artefacts rocks are systematically fine to very fine-grained, stereo-microscopy can allow recognizing small garnets, whose presence indicates eclogite and garnet-omphacitite. The density of 97 (out of 98) archaeological implements was determined (Fig. 4.a). As expected, two groups are observed. The one with density \u0026gt; 3 g/cm\u003csup\u003e3\u003c/sup\u003e includes \u003cem\u003egreenstones s.s.\u0026nbsp;\u003c/em\u003e(namely jadeitite, omphacitite, mixed Na-pyroxenite, Grt-bearing omphacitite and eclogite \u0026ndash; roughly listed in order of increasing density). The other, with density \u0026gt; 2.7 g/cm\u003csup\u003e3\u003c/sup\u003e, includes only serpentinite. A single prasinite is also observed (3.1 g/cm\u003csup\u003e3\u003c/sup\u003e). These artefacts are thus mainly composed of \u003cem\u003egreenstones s.s.\u0026nbsp;\u003c/em\u003e(83 %; Fig. 4.b), in which e\u003cem\u003eclogites\u003c/em\u003e (54 %) predominate over \u003cem\u003eNa-pyroxenites\u003c/em\u003e (16 %); \u003cem\u003eserpentinites\u003c/em\u003e are quite scarce (6 %). For a limited number of specimens (3) no clear lithological attribution is achieved, for lack of useful information. All data, including inventory code and typological descriptions, are listed in the Supplementary Material, Table S1.\u0026nbsp;\u003c/p\u003e\n\u003cp\u003e\u003cem\u003eX-ray powder diffraction\u003c/em\u003e\u0026nbsp;\u003c/p\u003e\n\u003cp\u003e\u003cem\u003eArchaeological tools\u003c/em\u003e\u003c/p\u003e\n\u003cp\u003e\u003cem\u003e\u003cstrong\u003eTable 1.\u0026nbsp;\u003c/strong\u003eVariation of cell parameters of pyroxenes (jadeite and omphacite), as determined from XRPD data collected on 45 Neolithic \u003cem\u003egreenstone\u003c/em\u003e implements from \u003cem\u003eRocca di Cavour\u003c/em\u003e similar geological samples from primary outcrops of the upper Po valley and from secondary alluvial deposits.\u003c/em\u003e\u003c/p\u003e\n\u003cdiv align=\"\"\u003e\n \u003ctable border=\"1\" cellspacing=\"0\" cellpadding=\"0\"\u003e\n \u003ctbody\u003e\n \u003ctr\u003e\n \u003ctd valign=\"top\" style=\"width: 92px;\"\u003e\n \u003cp\u003e\u003cstrong\u003eCell parameters\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd valign=\"top\" style=\"width: 151px;\"\u003e\n \u003cp\u003e\u003cstrong\u003eJadeite\u0026nbsp;\u003c/strong\u003e\u003c/p\u003e\n \u003cp\u003e\u003cstrong\u003eNaAlSi\u003csub\u003e2\u003c/sub\u003eO\u003csub\u003e6\u003c/sub\u003e\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd valign=\"top\" style=\"width: 152px;\"\u003e\n \u003cp\u003e\u003cstrong\u003eOmphacite\u003c/strong\u003e\u003c/p\u003e\n \u003cp\u003e\u003cstrong\u003e(Na,Ca)(Al,Fe,Mg)Si\u003csub\u003e2\u003c/sub\u003eO\u003csub\u003e6\u003c/sub\u003e\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd valign=\"top\" style=\"width: 92px;\"\u003e\n \u003cp\u003e\u003cstrong\u003ea\u003csub\u003e0\u003c/sub\u003e\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd valign=\"top\" style=\"width: 151px;\"\u003e\n \u003cp\u003e9.425(3) \u0026ndash; 9.482(4) \u0026Aring;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd valign=\"top\" style=\"width: 152px;\"\u003e\n \u003cp\u003e9.512(3) \u0026ndash; 9.631(2) \u0026Aring;\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd valign=\"top\" style=\"width: 92px;\"\u003e\n \u003cp\u003e\u003cstrong\u003eb\u003csub\u003e0\u003c/sub\u003e\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd valign=\"top\" style=\"width: 151px;\"\u003e\n \u003cp\u003e8.573(3) \u0026ndash; 8.650(2) \u0026Aring;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd valign=\"top\" style=\"width: 152px;\"\u003e\n \u003cp\u003e8.674(2) \u0026ndash; 8.811(3) \u0026Aring;\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd valign=\"top\" style=\"width: 92px;\"\u003e\n \u003cp\u003e\u003cstrong\u003ec\u003csub\u003e0\u003c/sub\u003e\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd valign=\"top\" style=\"width: 151px;\"\u003e\n \u003cp\u003e5.223(1) \u0026ndash; 5.262(2) \u0026Aring;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd valign=\"top\" style=\"width: 152px;\"\u003e\n \u003cp\u003e5.252(2) \u0026ndash; 5.283(1) \u0026Aring;\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd valign=\"top\" style=\"width: 92px;\"\u003e\n \u003cp\u003e\u003cstrong\u003eb\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd valign=\"top\" style=\"width: 151px;\"\u003e\n \u003cp\u003e107.42\u0026deg;(4) \u0026ndash; 107.75\u0026deg;(4)\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd valign=\"top\" style=\"width: 152px;\"\u003e\n \u003cp\u003e106.61\u0026deg;(3) \u0026ndash; 107.42\u0026deg;(2)\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd valign=\"top\" style=\"width: 92px;\"\u003e\n \u003cp\u003e\u003cstrong\u003eVolume\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd valign=\"top\" style=\"width: 151px;\"\u003e\n \u003cp\u003e403(2) \u0026ndash; 410(2) \u0026Aring;\u003csup\u003e3\u003c/sup\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd valign=\"top\" style=\"width: 152px;\"\u003e\n \u003cp\u003e415(2) \u0026ndash; 428(3) \u0026Aring;\u003csup\u003e3\u003c/sup\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003c/tbody\u003e\n \u003c/table\u003e\n\u003c/div\u003e\n\u003cp\u003eXRPD data were collected on 37 representative samples (Supplementary Material, Table S2), which allowed identifying the nature of the major/minor minerals of the rocks, as well as the average composition of Na-pyroxenes based on their unit-cell parameters (Table 1), sensitive to chemical variations (c.f., [16]). Few implements are made of rocks with pyroxene compositions close to either pure jadeite or omphacite (Fig. 5.a). In most, a jadeitic pyroxene coexists with a more omphacitic one, as suggested by the splitting of related reflections (Fig. 5.b). This accounts for finer variations in the cell parameters, especially for \u003cem\u003ea\u003csub\u003e0\u003c/sub\u003e\u003c/em\u003e and \u003cem\u003eb\u003csub\u003e0\u003c/sub\u003e\u003c/em\u003e (Table 1). In omphacite, \u003cem\u003ea\u003csub\u003e0\u003c/sub\u003e\u003c/em\u003e is usually \u0026gt; 9.52 \u0026Aring; \u0026ndash; the lower values being determined by a higher content in Aeg (a Fe\u003csup\u003e3+\u003c/sup\u003e-richer end-member of the same solid solution: NaFeSi\u003csub\u003e2\u003c/sub\u003eO\u003csub\u003e6\u003c/sub\u003e). Eclogites also show the garnet peaks, in addition to omphacite. The estimated pyroxene compositions based on XRPD data proved to be consistent with the SEM-EDS results.\u0026nbsp;\u003c/p\u003e\n\u003cp\u003e\u003cem\u003eGeologic samples\u003c/em\u003e\u003c/p\u003e\n\u003cp\u003eXRPD was also performed on 16\u003cstrong\u003e\u0026nbsp;geologic\u0026nbsp;\u003c/strong\u003e\u003cstrong\u003egreenstones s.s.\u003c/strong\u003e akin to the archaeological finds, namely: \u003cstrong\u003e7 Na-pyroxenites\u003c/strong\u003e (2 jadeitites, 4 omphacitites and 1 mixed Na-pyroxenite) and \u003cstrong\u003e9 Na-pyroxene + garnet rocks\u003c/strong\u003e (8 eclogites, 1 garnet omphacitite). Calculation of the Na-pyroxenes unit-cell parameters gave values consistent with those of the Neolithic tools (Table 1). Also, the compositions estimated from the d\u003csub\u003ehkl\u003c/sub\u003e values were in good agreement with those obtained by SEM-EDS. On the Morimoto et al. (1988) ternary diagram ([52], Fig. 6.a), these compositions (red spots) plot very close to those of the archeological implements (green spots in Fig. 6.b). For each sample, the unit-cell parameters, d\u003csub\u003ehkl\u003c/sub\u003e values and estimated pyroxene composition (in terms of Jd, (Wo+En+Fs) and Aeg wt %) are reported in Supplementary Material, Table S3.\u003c/p\u003e\n\u003cp\u003e\u003cem\u003ePetrographic study\u003c/em\u003e\u0026nbsp;\u003c/p\u003e\n\u003cp\u003eThis method, to be implemented by SEM-EDS, is essential to describe and interpret the complex tectono-metamorphic history experienced by \u003cem\u003eHP-greenstones s.s.\u003c/em\u003e (e.g., [46]).\u003c/p\u003e\n\u003cp\u003e\u003cem\u003eArchaeological tools\u003c/em\u003e\u0026nbsp;\u003c/p\u003e\n\u003cp\u003e\u003cstrong\u003e18 thin sections\u003c/strong\u003e were obtained from small drill-cores of splinters/uncomplete tools, namely:\u003c/p\u003e\n\u003cul\u003e\n \u003cli\u003e\u003cstrong\u003e5\u003c/strong\u003e Na-pyroxenites (3 jadeitites and 2 omphacitites)\u003c/li\u003e\n \u003cli\u003e\u003cstrong\u003e13\u003c/strong\u003e Na-pyroxene + garnet rocks (7 eclogites and 6 garnet omphacitites)\u003c/li\u003e\n\u003c/ul\u003e\n\u003cp\u003eTheir qualitative/quantitative compositions \u0026ndash; integrated also by XRPD and SEM-EDS (when available), are reported in the Supplementary Material, Table S4.\u0026nbsp;\u003c/p\u003e\n\u003cp\u003e\u003cem\u003eEclogite\u003c/em\u003e\u003c/p\u003e\n\u003cp\u003eFive out of seven eclogite samples (PIEM77/80/84/86/87) are medium- to fine-grained. Locally, a weak foliation is evident, marked by the dimensional preferred orientation of omphacite, rutile and titanite, as well as by the alignment of smaller garnets. In two samples (PIEM86 and 87), a more pervasive foliation turning into a mylonitic fabric is wrapping around omphacite porphyroclasts, which are zoned with a greenish more omphacitic rim, richer in Wo+En+Fs and Aeg, surrounding a colourless Jd-richer core that includes drop-like exsolutions of a higher-relief Na-pyroxene (akin to the one at the rim) and tiny rutile/titanite inclusions. Garnet occurs as small- to medium-grained idioblastic zoned poikiloblasts, with a pinkish core and a colourless rim, locally with atoll-like habit (e.g., in PIEM 80, 84 and 87; Fig. 7.a). Clinozoisite, zoisite and white-mica aggregates with euhedral shape and murky borders are interpreted as pseudomorphs after former lawsonite porphyroblasts (e.g., in PIEM86; Fig. 7.b). \u0026nbsp; Rutile, ilmenite and titanite are the most common accessories, the latter deriving from alteration of the formers. Rutile occurs as skeletal aggregates, single grains or tiny acicular crystals. Rare zircon (PIEM87), apatite (PIEM86) and opaque ores are locally observed. A weak greenschist-facies retrogression is testified by the partial replacement of Na-pyroxene by a symplectitic aggregate of actinolite and albite (e.g., PIEM 77, 80 and 87). Other accessories include small xenoblasts of glaucophane, locally replaced by a Ca-richer amphibole, and aggregates of chlorite together with epidote, white mica and interstitial albite (PIEM87) often with polysynthetic twinning (PIEM77). Two more samples (PIEM76/88) are glaucophane eclogites, characterized by a medium- to fine-grained matrix consisting of relict omphacite and subordinate glaucophane, strongly retrogressed to symplectitic aggregates of actinolite and albite. The fragmented garnet poikiloblasts include opaque ores in the rim and omphacite, rutile, titanite and epidote in the core. Apatite and iron-sulfides are accessories.\u0026nbsp;\u003c/p\u003e\n\u003cp\u003e\u003cem\u003eGarnet-omphacitite\u003c/em\u003e\u003c/p\u003e\n\u003cp\u003eThe six samples consist of a fine-grained omphacite matrix (\u0026raquo;\u0026nbsp;70 vol. %) that includes euhedral (PIEM90) to subhedral (PIEM85) scattered poikiloblasts of zoned garnets, with a pinkish core and a colourless rim. Tiny rutile crystals define a weak foliation. In PIEM85, the foliation is also highlighted by omphacite micro-crystals and acicular rutile (Fig. 7.c), which are wrapping around bigger pyroxene crystals. In four other samples (PIEM75/78/91/92), the rock consists of two intimately associated pleochroic pyroxenes with different appearance and composition, which define an almost mylonitic foliation: one, bright-greenish in colour, presumably richer in Aeg (\u0026gt; Fe\u003csup\u003e3+\u003c/sup\u003e); the other, pale green, is more omphacitic. Locally, a few bigger zoned pyroxenes occur with a greener Ca-richer core including rutile needles and a colourless, more jadeitic, inclusion-free rim. Aggregates of euhedral zoisite, clinozoisite and white mica (e.g., in PIEM75 and 78) are interpreted as pseudomorphs after former lawsonite, which are surrounded by a Na-pyroxene corona, mostly retrogressed to an albite+actinolite intergrowth. Titanite, zircon, allanite, chlorite and opaque ores are accessory phases.\u0026nbsp;\u003c/p\u003e\n\u003cp\u003e\u003cem\u003eOmphacitite\u003c/em\u003e\u003c/p\u003e\n\u003cp\u003eThe two studied samples (PIEM79/89) have fine- to very fine-grained omphacite matrices (\u0026raquo;\u0026nbsp;70 vol. %), with minor rutile, titanite, ilmenite, allanite, quartz and scarce epidote, albite and pyrite. In PIEM89, a strongly zoned omphacite exists with a deeper green core (presumably Fe\u003csup\u003e3+\u003c/sup\u003e-richer) and a colourless, more jadeitic rim (Al\u003csup\u003e3+\u003c/sup\u003e-richer). The cores are often dusty, due to tiny rutile needles oriented parallel to the pyroxene elongation, interpreted as the product of unmixing from an original igneous Ti-rich pyroxene. Rutile also occurs as skeletal aggregates of anhedral crystals, partly retrogressed to titanite. Large irregular aggregates of zoned epidote, with yellowish to dark-blueish anomalous interference colours, are observed. Large sub-idioblasts of opaque ore occur, often associated with albite. In PIEM79 a weak foliation is defined by the alignment of ilmenite porphyroclasts and tiny pale-green omphacite micro-crystals. Small roundish domains are also observed, consisting of fine-grained aggregates of omphacite and chlorite (plus tiny quartz crystals at the border), possibly derived from the alteration of original garnet poikiloblasts. Ilmenite, the second most abundant phase, forms xenomorphic porphyroblasts either stout or elongated, oriented parallel to the foliation.\u0026nbsp;\u003c/p\u003e\n\u003cp\u003e\u003cem\u003eJadeitite\u003c/em\u003e\u003c/p\u003e\n\u003cp\u003eThe 3 analyzed samples (PIEM81/82/83) exhibit a granoblastic structure and consist of jadeite (\u0026gt; 90 vol. %) with minor amounts of epidote + titanite (PIEM82 and 83), albite + glaucophane (PIEM83) or paragonite (PIEM82). Rutile and zircon are common accessories. Jadeite blasts have variable size and heterogeneous grain-size, even within the same sample. Usually, jadeite is zoned with a colourless core (\u0026gt; Al\u003csup\u003e3+\u003c/sup\u003e) and a pale green rim (\u0026gt; Fe\u003csup\u003e3+\u003c/sup\u003e). The jadeite core is murky, due to inclusions of acicular rutile parallel to the pyroxene elongation and tiny exsolution droplets of a more omphacitic pyroxene (Fig. 7.d). Fine-grained rutile may also form skeletal aggregates, occasionally retrogressed to titanite. Albite occurs as interstitial domains including idioblastic omphacite with prismatic habit (PIEM83). Minor phases are acicular glaucophane and red-to-brown pleochroic allanite locally including zircon.\u0026nbsp;\u003c/p\u003e\n\u003cp\u003e\u003cem\u003eGeologic samples\u003c/em\u003e\u0026nbsp;\u003c/p\u003e\n\u003cp\u003e\u003cstrong\u003e16 thin sections\u003c/strong\u003e were obtained from \u003cem\u003emeta-ophiolites\u003c/em\u003e of primary outcrops and alluvial deposits of the upper Po valley, namely:\u003c/p\u003e\n\u003cul\u003e\n \u003cli\u003e6 Na-pyroxene rocks (4 jadeitites, 2 omphacitites)\u003c/li\u003e\n \u003cli\u003e10 Na-pyroxene + garnet rocks (all eclogites)\u003c/li\u003e\n\u003c/ul\u003e\n\u003cp\u003eTheir qualitative/quantitative compositions \u0026ndash; integrated also by XRPD and SEM-EDS (when available), are reported in the Supplementary Material, Table S5.\u0026nbsp;\u003c/p\u003e\n\u003cp\u003e\u003cem\u003eEclogite\u003c/em\u003e\u003c/p\u003e\n\u003cp\u003eThe \u003cstrong\u003eten\u003c/strong\u003e samples studied are fine- to medium-grained rocks that essentially consist of omphacite and garnet, with accessory epidote, chlorite, glaucophane, white mica, albite, quartz, rutile, apatite and opaque ores. Omphacite occurs as medium- to fine-grained elongated nematoblasts, whose colour varies from colourless or pale green (bigger crystals) to bright green (fine-grained aggregates). The bigger crystals are often zoned with a green to turquoise core and a colourless, more jadeitic rim (e.g., OF2780 and 2765; Fig. 7.e). Most omphacite blasts have a core containing tiny drop-like exsolutions of a pyroxene with different chemistry and acicular rutile. Small- to medium-sized subidioblastic garnets may occur up to about 50 % of the rock volume (e.g., OF2779). The biggest poikiloblastic garnets include omphacite, rutile, chlorite, quartz and epidote. The omphacite inclusions in atoll-like garnets have the same optical properties (and probably the same composition) of the external one. Some garnets are zoned with a pinkish core and a colourless rim. A marked planar anisotropy is often visible, due to the alternation of nematoblastic omphacite-rich domains and granoblastic garnet-rich ones. In some cases (OF2675), a compositional layering is observed, with alternating pyroxene- and epidote-rich layers. Local foliation is defined by the dimensional preferred orientation of omphacite nematoblasts and aggregates of opaque ores (OF2779) and rutile (OF2771). Some samples are crossed by sets of late fractures, along which a greenschists-facies retrogression appears (OF2758, 2771, 2779 and 2780, as well as in the Val Carbonieri samples \u0026ndash; e.g., OF2702 [45]). Rutile, the most abundant accessory, occurs as either small random blasts (OF2765) or aggregates parallel to foliation (OF2761, 2764, 2781). Large randomly oriented pleochroic glaucophane idioblasts (OF2764 and 2765; Fig. 7.f) occur, locally almost completely replaced by a Na/Ca- bluish green amphibole (OF2779 and 2780). Pale greenish epidote xenoblasts (e.g., OF2758, 2765, 2781) or colourless clinozoisite with yellow-to-blueish anomalous interference colours locally fill veins in association with opaque ores (OF2781). Chlorite forms pale-green to colourless domains (OF2779, 2780). Only in one case (OF2781), an omphacite + garnet + chlorite assemblage is observed, where the sharp contacts between chlorite and garnet crystals indicate that these minerals are in equilibrium. White mica, usually scarce and fine-grained (OF2764, 2779), occurs in OF2781 as medium-size lepidoblasts. Two samples (OF2775 and 2785) with porphyroblastic structure and planar foliation consist of typical eclogitic/garnet-omphacite layers, alternating with others enriched in garnet, epidote, chlorite and albite. In the latter layers, zoisite/clinozoisite + white mica pseudomorphs after former lawsonite are surrounded by a mylonitic foliation, defined by fine-grained omphacite with tiny garnets. The rock foliation is crossed by a set of late fractures, along which omphacite is replaced by a darker albite + Na/Ca-amphibole symplectite. Chlorite and rutile are accessories.\u0026nbsp;\u003c/p\u003e\n\u003cp\u003e\u003cem\u003eOmphacitite\u003c/em\u003e\u003c/p\u003e\n\u003cp\u003eThe \u003cstrong\u003etwo\u003c/strong\u003e samples have fine (OF2760) or fine-to-medium grain-size (OF2763), consisting of omphacite and accessory white mica, epidote, chlorite and rutile. OF2760 contains omphacite domains alternating with others where white mica, epidote and minor rutile are observed. OF2763 has a marked foliation, defined by the dimensional preferred orientation of white mica flakes and pyroxene nematoblasts, alternating with domains of granoblastic omphacite. Coarser-grained omphacite crystals are slightly pleochroic (green-to-yellowish), with a core more coloured than the rim. The omphacite core is often dusty due to tiny inclusions of acicular rutile, parallel to the elongation of the host crystals. In OF2763, white mica (probably paragonite) occurs as medium-grained euhedral lepidoblasts. In OF2760, white mica occurs as small xenoblasts associated to epidote. Zoisite and clinozoisite form xenoblastic aggregates, while chlorite occurs as domains (OF2760). In OF2763, accessory allanite is observed.\u0026nbsp;\u003c/p\u003e\n\u003cp\u003e\u003cem\u003eJadeitite\u003c/em\u003e\u003c/p\u003e\n\u003cp\u003eThe \u003cstrong\u003efour\u003c/strong\u003e specimens are fine-to-medium grained and mainly consist of jadeite (\u0026sup3; 75 vol. %), with minor albite and amphibole. Zircon, rutile and allanite are ubiquitous accessory minerals. The microstructure is either granoblastic (OF2772 and 2788) or porphyroblastic (OF2774). In some cases, a weak foliation is observed, defined by the dimensional preferred orientation of jadeite blasts (OF2767 and 2774). Colourless jadeite occurs as xenoblasts of variable dimensions; the bigger crystals (\u0026raquo; 2 mm across) exhibit either a radial to fibrous habit or subgrain microstructure (OF2774). Some jadeite crystals are evidently zoned, with small light-green exsolution droplets of omphacitic pyroxene included at the core. Occasionally, jadeite porphyroblasts are surrounded by fine-grained aggregates, rimmed by a thin film of retrograde albite, biotite and acicular amphibole (OF2774). \u0026nbsp;Idioblastic to subidioblastic zircons, rutile and allanite are ubiquitous accessory phases.\u0026nbsp;\u003c/p\u003e\n\u003cp\u003e\u003cem\u003eSEM-EDS\u003c/em\u003e\u003c/p\u003e\n\u003cp\u003eBesides allowing observation at higher magnifications (Fig. 8), this approach also defines the chemistry of pyroxene and garnet solid solutions. Chemical data (Fig. 9) are plotted on the Jd/Aeg/Q diagram of Morimoto et al\u003cem\u003e.\u003c/em\u003e (1988) [52], Fig. 6.a) for pyroxenes and [almandine (Alm) + spessartine (Sps)] \u0026ndash; grossular (Grs) \u0026ndash; pyrope (Prp) ternary diagram for garnets; mineral symbols follow Warr (2021) [53]. EDS analyses of pyroxenes and garnets are reported in the Supplementary Material (Tables S6-S21). \u0026nbsp;\u0026nbsp;\u003c/p\u003e\n\u003cp\u003e\u003cem\u003eArchaeological tools\u0026nbsp;\u003c/em\u003e\u0026nbsp;\u003c/p\u003e\n\u003cp\u003e\u003cstrong\u003e9 thin sections\u003c/strong\u003e were analyzed, namely:\u003c/p\u003e\n\u003cul\u003e\n \u003cli\u003e\u003cstrong\u003e5\u003c/strong\u003e Na-pyroxene rocks (3 jadeitites and 2 omphacitites)\u003c/li\u003e\n \u003cli\u003e\u003cstrong\u003e4\u003c/strong\u003e Na-pyroxene + garnet rocks (3 eclogites and 1 garnet omphacitite).\u003cstrong\u003e\u0026nbsp;\u003c/strong\u003e\u003c/li\u003e\n\u003c/ul\u003e\n\u003cp\u003e\u003cem\u003eEclogite\u003c/em\u003e\u003c/p\u003e\n\u003cp\u003eTwo eclogites (PIEM77 and 80) show different microstructures. In the former, a weakly-zoned omphacite matrix has an average Jd\u003csub\u003e40\u003c/sub\u003e, (Wo+En+Fs)\u003csub\u003e45\u003c/sub\u003e, Aeg\u003csub\u003e15\u003c/sub\u003e composition, with Q decreasing from the rim (60 wt %) to the core (40 wt %) at constant Jd/Aeg ratio. Presence of albite, Mg-chlorite, clinozoisite and titanite-rich areas indicates a weak greenschist-facies overprint (Fig. 8.a). Omphacite included in garnet has the same composition as the matrix core (Fig. 9.a). \u003cem\u003eGarnet\u003c/em\u003e, often with atoll-like structure (Fig. 8.b), is a weakly zoned almandine with Grs component slightly increasing from core to rim (Fig. 9.a). In the latter, a more marked pyroxene zoning is observed: a more jadeite-rich core (up to Jd\u003csub\u003e90\u003c/sub\u003e) decreases towards the rim reaching Jd\u003csub\u003e70\u003c/sub\u003e and Jd\u003csub\u003e50\u003c/sub\u003e (A and B in Fig. 9.a, respectively). Omphacite exsolutions in the jadeite core have an average composition Jd\u003csub\u003e60\u003c/sub\u003e, (Wo+En+Fs)\u003csub\u003e25\u003c/sub\u003e, Aeg\u003csub\u003e15\u003c/sub\u003e (C in Fig. 9.a). Garnet shows a weak zoning, with the grossular decreasing from core (Grs\u003csub\u003e20\u003c/sub\u003e) to rim, enriched in Alm (Fig. 9.a). In PIEM76, a retrogressed \u003cem\u003eglaucophane eclogite\u003c/em\u003e, relict omphacite has an average composition Jd\u003csub\u003e35\u003c/sub\u003e (Wo+En+Fs)\u003csub\u003e50\u003c/sub\u003e Aeg\u003csub\u003e15\u003c/sub\u003e, with Q slightly decreasing from core to rim. Pyroxenes included in garnet and in the matrix have the same composition. Garnet is an almandine with low Prp and Grs (\u0026raquo; 10 wt %) (Fig. 9.a). \u0026nbsp;\u003c/p\u003e\n\u003cp\u003e\u003cem\u003eGarnet-omphacitite\u003c/em\u003e\u003c/p\u003e\n\u003cp\u003ePIEM75 is characterized by a banded structure with alternating garnet-bearing and -free layers. In the latter, a fine-grained\u0026nbsp;Na-pyroxene matrix with mylonitic fabric includes\u0026nbsp;clinozoisite + paragonite aggregates with a geometric shape, interpreted as pseudomorphs after former lawsonite porphyroblasts. Two distinct pyroxene compositions emerge from BSE images: i) strongly\u0026nbsp;zoned and with finer grain-size, with average composition: Jd\u003csub\u003e45\u003c/sub\u003e (Wo+En+Fs)\u003csub\u003e40\u003c/sub\u003e Aeg\u003csub\u003e15\u003c/sub\u003e; ii) with bigger, zoned and Fe-richer relict crystals, whose Q component varies from 30 to 55 wt % at a constant Jd/Aeg ratio (A and B in Fig. 9.a). In the garnet-bearing layers, the little poikiloblastic garnets that overgrows the mylonitic foliation include small rutile, titanite and omphacite. Garnet composition is\u0026nbsp;quite homogeneous (average:\u0026nbsp;Alm+Sps\u003csub\u003e75\u003c/sub\u003e Grs\u003csub\u003e15\u003c/sub\u003e Prp\u003csub\u003e10\u003c/sub\u003e). \u0026nbsp;\u003c/p\u003e\n\u003cp\u003e\u003cem\u003eOmphacitite\u003c/em\u003e\u003c/p\u003e\n\u003cp\u003eIn PIEM79, omphacite represents about 75 vol. % of the rock and is slightly zoned, with the jadeite end-member decreasing core-to-rim from Jd\u003csub\u003e45\u0026nbsp;\u003c/sub\u003eto Jd\u003csub\u003e35\u003c/sub\u003e, at constant aegirine content (Aeg\u003csub\u003e20\u003c/sub\u003e) (Fig. 9.a). Two roughly round-shaped portions, consisting of Mg-chlorite with relict pyroxene, are interpreted as pseudomorphs after former poikiloblastic garnet. In PIEM89, omphacite is strongly zoned with jadeite increasing from Jd\u003csub\u003e15\u003c/sub\u003e in the core to Jd\u003csub\u003e40\u003c/sub\u003e in the rim (Fig. 9.a). Tiny oriented rutile inclusions in the omphacite core suggest its derivation from exsolution of an original magmatic pyroxene.\u0026nbsp;\u003c/p\u003e\n\u003cp\u003e\u003cem\u003eJadeitite\u003c/em\u003e\u003c/p\u003e\n\u003cp\u003ePIEM81 and PIEM82 consist of \u0026gt; 90 vol. % of fine-grained, almost pure jadeite (\u0026sup3;\u0026nbsp;Jd\u003csub\u003e95\u003c/sub\u003e), which locally contain at the core drop-like omphacitic exsolutions and acicular rutile (Fig. 8.c). Jadeite is surrounded by an omphacite rim with composition Jd\u003csub\u003e50-35\u0026nbsp;\u003c/sub\u003e(Wo+En+Fs)\u003csub\u003e30-45\u003c/sub\u003e and Aeg\u003csub\u003e20\u003c/sub\u003e (Fig. 8.d; 9.a), similar to the exsolutions in the jadeite core. In PIEM82, a darker sub-circular domain is observed (similar to PIEM79), consisting of epidote, albite, paragonite and relict Na-pyroxene (Fig. 8.d). In PIEM83, the pyroxene occurs as big, irregularly zoned and sub-idioblastic crystals, usually Jd-richer at the core (Jd\u003csub\u003e100-70\u003c/sub\u003e) than the rim Jd\u003csub\u003e50\u003c/sub\u003e (Wo+En+Fs)\u003csub\u003e30\u003c/sub\u003e Aeg\u003csub\u003e20\u003c/sub\u003e (B in Fig. 9.a). The core includes tiny inclusions of acicular rutile and drop-like exsolved omphacite (A in Fig. 9.a). Late domains of albite also appear, which frequently include euhedral prismatic Na-pyroxene with aegirin-augite composition (C in Fig. 8.a).\u0026nbsp;\u003c/p\u003e\n\u003cp\u003e\u003cem\u003eGeologic samples\u003c/em\u003e\u0026nbsp;\u003c/p\u003e\n\u003cp\u003e\u003cstrong\u003e4 thin sections\u003c/strong\u003e were analyzed, namely:\u003c/p\u003e\n\u003cul\u003e\n \u003cli\u003e\u003cstrong\u003e1\u003c/strong\u003e Na-pyroxenite (jadeitite)\u003c/li\u003e\n \u003cli\u003e\u003cstrong\u003e3\u003c/strong\u003e Na-pyroxene + garnet rocks (all eclogites).\u0026nbsp;\u003c/li\u003e\n\u003c/ul\u003e\n\u003cp\u003e\u003cem\u003eEclogite\u003c/em\u003e\u003c/p\u003e\n\u003cp\u003eThe \u003cstrong\u003e\u003cem\u003eeclogite\u003c/em\u003e\u003c/strong\u003e OF2780\u003cstrong\u003e\u0026nbsp;\u003c/strong\u003eis\u003cstrong\u003e\u0026nbsp;\u003c/strong\u003emedium- to fine-grained, with grano-nematoblastic structure and a weak foliation. Omphacite crystals are zoned, with an aegirine-augite richer core (Aeg\u003csub\u003e30-40\u003c/sub\u003e) and a more omphacitic rim (Jd\u003csub\u003e40\u003c/sub\u003e, Wo+En+Fs\u003csub\u003e35\u003c/sub\u003e and Aeg\u003csub\u003e25\u003c/sub\u003e). Idioblastic garnets with atoll-like habitus are also zoned, with Grs increasing from core [(Alm+Sps)\u003csub\u003e80\u003c/sub\u003e, Prp\u003csub\u003e15\u003c/sub\u003e, Grs\u003csub\u003e5\u003c/sub\u003e] to rim (up to\u0026nbsp;\u0026raquo;\u0026nbsp;20 wt %) (Fig. 9.b). The other two eclogites come from the Val Carbonieri [45]. OF2671 is fine-grained, with small garnets that seldom show an atoll-like aspect; they are contoured by a pyroxene matrix with a homogeneous omphacite composition (Jd\u003csub\u003e40\u003c/sub\u003e, Wo+En+Fs\u003csub\u003e40\u003c/sub\u003e and Aeg\u003csub\u003e20\u003c/sub\u003e). Garnets are zoned and rich in almandine (75 to 85 wt %), with grossular decreasing from core to rim (\u0026raquo;\u0026nbsp;20 to 0 wt %). OF2702 is formed by omphacite porphyroclasts, wrapped by a finer matrix of both omphacite and garnets. The pyroxene has quite a homogeneous chemistry (Jd\u003csub\u003e25-50\u003c/sub\u003e and Aeg\u003csub\u003e10-25\u003c/sub\u003e), with garnets very similar to the previous sample (Fig. 9.b). \u0026nbsp; \u0026nbsp;\u0026nbsp;\u003c/p\u003e\n\u003cp\u003e\u003cem\u003eJadeitite\u003c/em\u003e\u003c/p\u003e\n\u003cp\u003eOF2788 is a fine-grained granoblastic rock with almost pure jadeite (\u0026gt;95 wt.%) (group A in Fig. 9.b), containing accessory rutile and zircon. In the core, jadeite crystals have small, drop-like omphacite exsolutions with composition Jd\u003csub\u003e50\u003c/sub\u003e, (Wo+En+Fs)\u003csub\u003e25\u003c/sub\u003e, Aeg\u003csub\u003e25\u003c/sub\u003e (group B in Fig. 9.b). These crystals are surrounded by a rim (Fig. 8.f) in which the jadeite content decreases from Jd\u003csub\u003e55\u0026nbsp;\u003c/sub\u003eto Jd\u003csub\u003e75\u003c/sub\u003e, at a constant (Wo+En+Fs)/Aeg ratio (group C in Fig. 9.b). \u0026nbsp;\u003c/p\u003e\n\u003cp\u003e\u003cem\u003eGeothermometry\u003c/em\u003e\u0026nbsp;\u003c/p\u003e\n\u003cp\u003eIn petrology, an estimate of the temperature peak of an eclogite-facies rock can be achieved from the garnet-omphacite, Fe/Mg exchange geothermometer. This is based on the partitioning of Fe and Mg between coexisting garnet and omphacite, whose amounts vary as a function of temperature. By applying the Ellis and Green (1979) calibration [54] for a nominal pressure of 15 kb, the T estimates were found to vary between 350 and 600 \u0026deg;C (Table 2) \u0026ndash; with most samples in the 400-500 \u0026deg;C range, which is consistent with the literature data for the Monviso meta-ophiolite (e.g., [55]). However, unlike the coarse-grained eclogites \u0026ndash; already mapped and analyzed in the geologic literature [42], two distinct temperature groups were obtained for each fine-grained eclogite of archaeological interest. This anomaly was interpreted as a consequence of the complex metamorphic history of these scarce and peculiar rocks, which experienced a polyphase mylonitic deformation in the presence of active aqueous fluids that produced a significant metasomatism, evidenced by the complex chemical zoning of both garnet and Na-pyroxene. Due to this, geothermometry is unfit to be used for identifying their provenance.\u0026nbsp;\u003c/p\u003e\n\u003cp\u003e\u003cstrong\u003eTable 2.\u0026nbsp;\u003c/strong\u003eGeothermometry results on the Fe-Mg partitioning in coexisting omphacite/garnet couples. Temperatures were computed at the nominal pressure of 15 kb.\u003c/p\u003e\n\u003cdiv align=\"\"\u003e\n \u003ctable border=\"1\" cellspacing=\"0\" cellpadding=\"0\" width=\"433\"\u003e\n \u003ctbody\u003e\n \u003ctr\u003e\n \u003ctd valign=\"top\" style=\"width: 104px;\"\u003e\n \u003cp\u003e\u003cstrong\u003eAnalytical code\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd valign=\"top\" style=\"width: 123px;\"\u003e\n \u003cp\u003e\u003cstrong\u003eLithotype\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd valign=\"top\" style=\"width: 104px;\"\u003e\n \u003cp\u003e\u003cstrong\u003e\u003cem\u003eT\u003c/em\u003e\u003c/strong\u003e\u003cstrong\u003e-range\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd valign=\"top\" style=\"width: 102px;\"\u003e\n \u003cp\u003e\u003cstrong\u003eT-clusters\u003c/strong\u003e\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd valign=\"top\" style=\"width: 104px;\"\u003e\n \u003cp\u003ePIEM 77\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd valign=\"top\" style=\"width: 123px;\"\u003e\n \u003cp\u003eEclogite\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd valign=\"top\" style=\"width: 104px;\"\u003e\n \u003cp\u003e390 \u0026ndash; 540 \u0026deg;C\u0026nbsp;\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd valign=\"top\" style=\"width: 102px;\"\u003e\n \u003cp\u003e520\u0026nbsp;\u0026plusmn;\u0026nbsp;20 \u0026deg;C\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd valign=\"top\" style=\"width: 104px;\"\u003e\n \u003cp\u003ePIEM 80\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd valign=\"top\" style=\"width: 123px;\"\u003e\n \u003cp\u003eEclogite\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd valign=\"top\" style=\"width: 104px;\"\u003e\n \u003cp\u003e310 \u0026ndash; 470 \u0026deg;C\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd valign=\"top\" style=\"width: 102px;\"\u003e\n \u003cp\u003eNone\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd valign=\"top\" style=\"width: 104px;\"\u003e\n \u003cp\u003ePIEM 76\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd valign=\"top\" style=\"width: 123px;\"\u003e\n \u003cp\u003eEclogite\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd valign=\"top\" style=\"width: 104px;\"\u003e\n \u003cp\u003e355 \u0026ndash; 405 \u0026deg;C\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd valign=\"top\" style=\"width: 102px;\"\u003e\n \u003cp\u003e383\u0026nbsp;\u0026plusmn;\u0026nbsp;30 \u0026deg;C\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd valign=\"top\" style=\"width: 104px;\"\u003e\n \u003cp\u003ePIEM 75\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd valign=\"top\" style=\"width: 123px;\"\u003e\n \u003cp\u003egarnet-omphacitite\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd valign=\"top\" style=\"width: 104px;\"\u003e\n \u003cp\u003e330 \u0026ndash; 690 \u0026deg;C\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd valign=\"top\" style=\"width: 102px;\"\u003e\n \u003cp\u003eNone\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd valign=\"top\" style=\"width: 104px;\"\u003e\n \u003cp\u003eOF2780\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd valign=\"top\" style=\"width: 123px;\"\u003e\n \u003cp\u003eEclogite\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd valign=\"top\" style=\"width: 104px;\"\u003e\n \u003cp\u003e375 \u0026ndash; 625 \u0026deg;C\u003c/p\u003e\n \u003c/td\u003e\n \u003ctd valign=\"top\" style=\"width: 102px;\"\u003e\n \u003cp\u003eNone\u003c/p\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003c/tbody\u003e\n \u003c/table\u003e\n\u003c/div\u003e"},{"header":"Discussion","content":"\u003cp\u003ePolished \u003cem\u003egreenstone\u003c/em\u003e axes have always been considered by archaeologists as typical of Neolithic. The Neolithic site of the \u003cem\u003eRocca di Cavour\u003c/em\u003e, in spite of its position (in front of the meta-ophiolitic complex of the Monviso Massif \u0026ndash; the main area of origin, together with the Voltri Massif, of most archaeological \u003cem\u003egreenstone\u003c/em\u003e tools spread throughout all Europe), had never been the object of a detailed archaeometric study so far. Although in this case the origin of the raw materials, as far as \u003cem\u003egreenstones\u003c/em\u003e are concerned, is quite straightforward (i.e., from local eclogite-facies meta-ophiolites), the performed archaeometric survey still provides useful information about the mineralogy and petrology of the investigated lithologies, especially in light of the comparative study on geological samples from the primary outcrops of the Monviso Complex and related secondary deposits. Although it is well-known that these rocks belong to the calc-schists with \u003cem\u003egreenstones\u003c/em\u003e Piemonte Zone (e.g., [24]), the vastness of this area and their limited distribution in a wide reservoir such as the Western Alps cause this knowledge to still be unsatisfactory. Natural, fine-grained \u0026lsquo;\u003cem\u003ejade\u003c/em\u003e\u0026rsquo; samples similar to the archaeological finds were unknown to geologists until recently, since the primary outcrops are extremely scattered, small (few m\u003csup\u003e3\u003c/sup\u003e) and heterogeneous \u0026ndash; thus hardly traceable even by expert petrologists focused on the study of eclogite-facies meta-ophiolites. These rocks can also be found in secondary deposits, where they tend to concentrate due to their higher hardness and lower erodibility, if compared to other rocks. Here, these deposits are represented by the Quaternary alluvial surrounding the Monviso Massif and the Oligocene post-orogenic conglomerates.\u003c/p\u003e\n\u003cp\u003eThe 98 studied polished-stone implements of the \u003cem\u003eRocca di Cavour\u003c/em\u003e settlement are mostly made of eclogite (54 %) and garnet-omphacitite (13 %), with subordinate jadeitite (5 %) and omphacitite (8 %; Fig. 4). Predominance of eclogite is consistent with several coeval sites of Northwestern Italy (e.g., Alba, Castello di Annone, Gaione, Ponte Ghiara, Rivanazzano, Sammardenchia, San Lazzaro di Savena and Valgrana/Tetto Chiappello [10,45,56-66]). In \u003cstrong\u003eeclogite\u003c/strong\u003e and \u003cstrong\u003egarnet-omphacitite\u003c/strong\u003e, the modally prevalent pyroxene (i.e., mostly omphacite) is characterized by a wide compositional range. Moreover, it is frequently zoned with complex and variable patterns. Garnets are also highly heterogeneous, both structurally and compositionally. The widespread atoll-like garnets, which locally contain remnants of the original core, indicate that these minerals experienced at least two main types of growth, under different \u003cem\u003eP-T\u003c/em\u003e conditions: \u003cem\u003ei)\u003c/em\u003e at first, multiple nucleation and coalescence processes allowed the poikiloblastic growth of small garnets; \u003cem\u003eii)\u003c/em\u003e later, their cores became unstable and in the presence of an abundant influx of hydrous fluids, they were easily corroded through replacement and re-crystallization reactions [67-72]. In most cases, garnets show an almandine-rich (i.e., Alm\u0026nbsp;\u0026sup3;70) average composition, either homogeneous (e.g., in PIEM76, where Alm\u003csub\u003e87-93\u003c/sub\u003e-Prp\u003csub\u003e9-5\u003c/sub\u003e-Grs\u003csub\u003e9-2\u003c/sub\u003e) or with an appreciable zoning (e.g., in PIEM75, where Grs grows from 5-to-21 % from core to rim). Also, in most eclogites and garnet-omphacitites lozenge-shaped aggregates of zoisite + clinozoisite + white mica exist, interpreted as pseudomorphs after an original porphyroblastic lawsonite, which grew at high-pressure conditions but broke down during later exhumation. \u003cstrong\u003eJadeitite\u003c/strong\u003e and \u003cstrong\u003eomphacitite\u003c/strong\u003e are monomineralic rocks, since Na-pyroxene is modally prevalent (\u0026gt; 90 vol. %). In \u003cstrong\u003ejadeitites\u003c/strong\u003e, crystals of almost pure jadeite (Jd\u003csub\u003e\u0026sup3;\u003c/sub\u003e\u003csub\u003e90\u003c/sub\u003e) are often contoured by omphacitic rims and include, at their core, tiny drop-like exsolutions with akin omphacitic composition. Such an occurrence has already been described in the literature [73-75].\u0026nbsp;Accessory rutile (TiO\u003csub\u003e2\u003c/sub\u003e: see Supplementary Material, Table S4) indicates that these rocks belong to the internal Piemonte Zone, i.e., from the Monviso Massif (in the external Piemonte Zone, titanite [CaTi(SiO\u003csub\u003e4\u003c/sub\u003e)O] would have appeared instead).\u0026nbsp;\u003cstrong\u003eOmphacitites\u003c/strong\u003e have quite a homogeneous chemistry, being mostly made of weakly zoned omphacite.\u0026nbsp;\u003c/p\u003e\n\u003cp\u003eThe performed geologic survey allowed collecting and analyzing several \u003cem\u003egreenstone\u003c/em\u003e specimens akin to the rocks of the prehistoric tools. In both instances, an intimate association of various omphacites with a modest zoning and variable Aeg contents is consistent with the variability described in the literature [76,77], which supports the possible existence of a miscibility gap between Aeg-poorer and Aeg-richer omphacites. Another systematic prospection of the Monviso Massif, aimed at locating primary outcrops of jadeitite-jades, was carried out quite recently [23,78]. In that instance, however, the archaeometric recognitions were achieved by using a completely different protocol \u0026ndash; namely visual identification and spectro-radiometry [79,80]. These approaches, unfortunately, may not always allow a thorough and reliable characterization of these lithotypes\u003cem\u003e\u0026nbsp;\u003c/em\u003e(not only jadeitites, but all \u003cem\u003egreenstones\u003c/em\u003e \u003cem\u003es.s.\u003c/em\u003e), which possess both compositional and micro-structural complexities hardly extrapolable without recurring to in-depth mineral/petrographic approaches. The comparative study performed here by using rigorous methods unequivocally proves that most \u003cstrong\u003eeclogites\u003c/strong\u003e are very similar in archaeological and geologic samples, both marked by fine grain often with mylonitic structure. Other common issues are: \u003cem\u003ei)\u003c/em\u003e the typical atoll-like structure and zoning of garnets (e.g., in OF2780, with Alm up to 84 % and Grs varying from \u0026asymp; 0-20 % between core and rim, respectively; the two geologic samples from the Val Carbonieri show moderate zoning, but with an opposite trend, i.e., Grs decreasing from core to rim.); \u003cem\u003eii)\u003c/em\u003e the recurrence of pluri-millimetric zoisite + clinozoisite + white mica pseudomorphs on original lawsonite; \u003cem\u003eiii)\u003c/em\u003e the persistence of regressed areas in greenschist-facies and \u003cem\u003ev)\u003c/em\u003e a lack or scarcity of white mica (muscovite, paragonite and/or phengite). The last feature is an undisputable clue indicating provenance from the Monviso Massif [3,47,66] \u0026ndash; whereas the abundance of white mica is instead an issue typical of \u003cem\u003egreenstones\u003c/em\u003e from the Beigua district, in the Voltri Massif (e.g., in the tools from Brignano Frascata, Villaromagnano and Momperone and related geological samples [31,46]). In these fine grained eclogites, veins or irregular omphacite domains lacking garnets are also observed, with features at times similar to those appreciable in Neolithic tools qualified as \u0026lsquo;Na-pyroxenites\u0026rsquo;. It is therefore possible that some omphacitites, classified as such in Neolithic tools, might indeed result from considering restricted omphacitic domains in larger, garnet-bearing rocks. This is confirmed by that fact that, in some artefacts (e.g., PIEM75), vast different portions with and/or without garnets are detected. Similarly, in other archaeological tools classified differently based on said parameters (i.e, presence/absence of garnets), pyroxenes with similar chemistry and features are observed. For example, in PIEM90 (a \u003cstrong\u003egarnet-omphacitite\u003c/strong\u003e, due to presence of scarce garnets) a light-green, anhedral and non-pleochroic omphacite exists, whose optical properties are very similar to that of PIEM79 (classified instead as an omphacitite, after an apparent lack of garnets). All these aspects account for the petrologic/petrographic complexity of these rocks, which must be considered any time an in-depth study should be attempted. Such a complexity, which involves both the micro-structure and composition of pyroxenes and garnets, is synergic to the geological context in which these rocks are located and formed. In fact, they are confined in small boudins (few dm\u003csup\u003e3\u003c/sup\u003e to m\u003csup\u003e3\u003c/sup\u003e) within shear zones, which underwent a polyphasic evolution marked by circulation of fluids with variable composition in time, as certified by the peculiar zoning of such minerals. In garnets, for example, this zoning, rather than being related to T/P variations (i.e., the metamorphic degree), depends on a metasomatic process in which the fluid (aqueous) phase had variable composition in different sites and moments in time and space, with direct consequences on their chemistry. For what concern \u003cstrong\u003ejadeitites\u003c/strong\u003e, several interesting clues emerge by comparing archaeological and geologic samples. The four metaophiolites from the alluvial sediments of the Po River \u0026ndash; all fine grained with mylonitic fabric and accessory rutile \u0026ndash; are very similar to most of their Neolithic counterparts. This suggests a provenance from the internal Piemonte Zone, marked by an Alpine eclogite-facies overprint. Other similarities concern specific features observed at SEM in BSE images \u0026ndash; i.e., the clear-cut zoning of Na-pyroxenes and the coexistence of two distinct pyroxene phases, jadeite and omphacite, the latter confined in drop-like omphacite exsolutions hosted at the core of the jadeite crystals, in turn contoured by omphacitic rims (e.g., in OF2788 and PIEM81/82/83; see Fig. 8.d and f). Also, in the prospected area, nodules of omphacitites crop out within extended chloritic-carbonatic schists, with compositional signatures very similar to some archaeological tools. Any attempt to determine the thermal peak of the high-pressure metamorphic event by applying the Fe/Mg partitioning between coexisting Na-pyroxene and garnets in eclogites did not yield satisfactory results, due to the recurring presence of two Na-pyroxenes with different compositions, coupled to mostly zoned garnets. Despite this, most of the obtained values \u0026nbsp;are consistent with the literature data estimated for the Monviso eclogites [42,55].\u003c/p\u003e\n\u003cp\u003eAs stated above, the rocks of the Neolithic tools are all fine grained, with typically zoned pyroxenes and garnets. Thus, their mineral/petrographic features and chemistry should be compared \u003cem\u003eonly\u003c/em\u003e with geologic samples having similar features (particularly, the fine grain-size). Unfortunately, the analyses of pyroxenes and garnets available in the geologic literature so far often refer to coarse-grained meta-gabbros, exposed in large outcrops (e.g., [40,42,81]). In fact, two different kinds of eclogite exist: \u003cem\u003ei)\u003c/em\u003e coarse-grained lithologies, whose microstructure is indicative of a magmatic protolith; \u003cem\u003eii)\u003c/em\u003e fine-grained lithologies, located in scarce and tiny (few dm-to-m\u003csup\u003e3\u003c/sup\u003e) outcrops \u0026ndash; yet mostly unmapped \u0026ndash; scattered along shear zones and affected by metasomatic processes. Only the latter \u0026ndash; the rarest one \u0026ndash; is of archaeologic interest. Fine-grained eclogites deriving from metasomatic events can also be recognized by the extreme compositional variability of the sodic pyroxene, ranging from jadeite to omphacite. These features, which are typical of most archaeologic tools, are geologically observed only in the metaophiolites of the Monviso and Voltri massifs (e.g., in Brignano Frascata: see Figs. 9 and 10 in [46]). These metasomatic processes brought to variations in the bulk chemical composition of the rocks, a phenomenon occurring only along shear zones, where repeated influxes of aqueous fluids with different compositions enter the system. Such an occurrence also justifies the extreme scattering and scarceness of these \u0026lsquo;\u003cem\u003ejades\u003c/em\u003e\u0026rsquo; on a geologic level. Despite this, these lithologies were extremely suitable for the preparation of implements, due their technological features (e.g., density, hardness, toughness,\u0026nbsp;workability and appeal) \u0026ndash; and thus painstakingly sought after by our Neolithic ancestors (possibly, the first \u0026lsquo;petrologists\u0026rsquo;) even in impervious places, for the manufacture of artefacts then to be traded all over Europe.\u003c/p\u003e\n\u003cp\u003eTherefore, basing on their mineral-petrographic features and chemistry, several clues confirm that the \u003cem\u003eHP\u003c/em\u003e-metaophiolites used to produce the prehistoric tools from the \u003cem\u003eRocca di Cavour\u003c/em\u003e originate from analogous lithotypes of the Monviso metamorphic complex \u0026ndash; which is consistent, under logical deduction, with the proximity of this supply source. Our results also confirm the conclusions of a previous archaeologic survey [38], claiming that a preliminary shaping of the \u003cem\u003egreenstone\u003c/em\u003e raw materials was performed on site by using ophiolitic pebbles and cobbles from the Quaternary alluvial deposits of the Pellice stream or a palaeo-bed of the Po River (in which they concentrate, being more resistant to erosion). Several tools, in fact, still preserve relict surfaces traceable to their original pebble/cobble shapes.\u003c/p\u003e"},{"header":"Declarations","content":"\u003cp\u003e\u003cem\u003eData availability\u003c/em\u003e\u003c/p\u003e\n\u003cp\u003eData reported in the manuscript or in the Supplementary Information will be rendered available on request.\u003c/p\u003e\n\u003cp\u003e\u003cem\u003eAcknowledgements\u003c/em\u003e\u003c/p\u003e\n\u003cp\u003eThis article is dedicated to the memory of \u003cstrong\u003eDino Delcaro\u003c/strong\u003e, a friend and experimental archaeologist who sadly passed away in 2022, with whom we exchanged over the years samples and information about \u003cem\u003egreenstones\u003c/em\u003e from the Monviso Massif. Six of his samples are discussed here. The authors would also like to thank Marica Venturino, for her critical reading and useful suggestions. This research did not receive any funding.\u003c/p\u003e\n\u003cp\u003e\u003cem\u003eConflict of interest or competing interests\u003c/em\u003e\u003c/p\u003e\n\u003cp\u003eThe authors declare no competing financial or non-financial interests.\u003c/p\u003e\n\u003cp\u003e\u003cem\u003eAuthor contribution\u003c/em\u003e\u003c/p\u003e\n\u003cp\u003eR.G. and R.C. coordinated the research project, supervised collection of analytical data and prepared the manuscript. M.B. and U.P. performed geologic prospections and collected analytical data. L.B. prepared the geographical/geological maps and provided geological descriptions.\u003c/p\u003e"},{"header":"References","content":"\u003col\u003e\n\u003cli\u003eAtkinson, R.J.C. (1974). Neolithic science and technology. Philosophical Transactions of the Royal Society A, Matematical, Physical and Engineering sciences, https://doi.org/10.1098/rsta.1974.0014.\u003c/li\u003e\n\u003cli\u003eCompagnoni, R. (2003). HP metamorphic belt of the western Alps. \u003cem\u003eEpisodes\u003c/em\u003e, 26(3), 200-204.\u003c/li\u003e\n\u003cli\u003eGiustetto, R. Padovan, S., Barale, L., Compagnoni, R. (2020). The Neolithic greenstone industry of Chiomonte (Northwestern Italy): mineralogy, petrography and archaeometric implications. \u003cem\u003eEur. J. Mineral\u003c/em\u003e., 32, 147\u0026ndash;166.\u003c/li\u003e\n\u003cli\u003eD\u0026rsquo;amico C., Starnini E., Gasparotto G., and Ghedini M. (2004). Eclogites, jades and other HP-metaophiolites employed for prehistoric polished stone implements in Italy and Europe. Periodico di Mineralogia, 73, Special Issue (3), 17-42.\u003c/li\u003e\n\u003cli\u003eOu Yang, M.C.M. (2006). The development of Fei Cui\u0026rsquo;s study in China. Proceedings of the First International Gem and Jewelry Conference, Gemological Institute of Thailand, Bangkok, December 6-9, 2006, p. 44.\u003c/li\u003e\n\u003cli\u003eOu Yang, M.C.M., Yen, H.K., Ng, M.F.Y., and Chan, S.Y. 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Acta 9 (3), 363\u0026ndash;387.\u003c/li\u003e\n\u003cli\u003eSchertl, H.P., Maresch, W.V., Stanek, K.P., Hertwig, A., Krebs, M., Baese, R., Sergeev, S.S. (2012). New occurrences of jadeitite, jadeite quartzite and jadeite-lawsonite quartzite in the Dominican Republic, Hispaniola: petrological and geochronological overview. \u003cem\u003eEur. J. Mineral\u003c/em\u003e., 24, 199-216.\u003c/li\u003e\n\u003cli\u003eKienast, J. R. (1983) Le m\u0026eacute;tamorphisme de haute pression et basse temp\u0026eacute;rature (\u0026eacute;clogites et schistes bleus): donn\u0026eacute;es nouvelles sur la p\u0026eacute;trologie de la cro\u0026ucirc;te oc\u0026eacute;anique subduct\u0026eacute;e et des s\u0026eacute;diments associ\u0026eacute;s. These Dr. Sci., Universit\u0026eacute; P. et M. Curie, Paris, 384 pp.\u003c/li\u003e\n\u003cli\u003ePhilippot, P.,Kienast, J.R. (1989). Chemical-microstructural changes in eclogite-facies shear zones (Monviso, Western Alps, north Italy) as indicators of strain history and the mechanism and scale of mass transfer. Lithos, 23 (3), 179-200.\u003c/li\u003e\n\u003cli\u003eP\u0026eacute;trequin, P., Errera, M., Rossy, M. (avec la collaboration de C. D\u0026rsquo;Amico et M. Ghedini) (2012). Viso ou Beigua : approche p\u0026eacute;trographique du r\u0026eacute;f\u0026eacute;rentiel des \u0026ldquo;jades alpins\u0026rdquo;. In: Jade. Grandes haches alpines du N\u0026eacute;olithique europ\u0026eacute;en, P. P\u0026eacute;trequin, S. Cassen, M. Errera, L. Klassen, A. Sheridan, A.M. P\u0026eacute;trequin (Sous la direction de), Chapitre 6, Presses Universitaires de Franche-Comt\u0026eacute; Ed., Besan\u0026ccedil;on, pp. 292-41.\u003c/li\u003e\n\u003cli\u003eErrera, M., P\u0026eacute;trequin, P., P\u0026eacute;trequin, A.M. (2012). Spectroradiom\u0026eacute;trie, r\u0026eacute;f\u0026eacute;rentiel naturel et \u0026eacute;tude de la diffusion des haches alpines. in \u0026ldquo;Jade. Grandes haches alpines du N\u0026eacute;olithique europ\u0026eacute;en\u0026rdquo;, Chapitre 8, P. P\u0026eacute;trequin, S. Cassen, M. Errera, L. Klassen, A. Sheridan, A.-M. P\u0026eacute;trequin, eds., Presses Universitaires de Franche-Comt\u0026eacute; Ed, Besan\u0026ccedil;on, 440\u0026ndash;533.\u003c/li\u003e\n\u003cli\u003eP\u0026eacute;trequin, P., Errera, M. (2017). Spectroradiom\u0026eacute;trie, approches macroscopiques et origine des jades alpins: Viso ou Beigua? In \u0026ldquo;Jade. Objets-signes et interpr\u0026eacute;tations sociales des jades alpins dans l\u0026rsquo;Europe n\u0026eacute;olitique\u0026rdquo;, Tome 3, Chapitre 4, Klassen P. P\u0026eacute;trequin, E. Gauthier, A.-M. P\u0026eacute;trequin, eds., Presses Universitaires de Franche-Comt\u0026eacute; Ed, Besan\u0026ccedil;on, 75\u0026ndash;86.\u003c/li\u003e\n\u003cli\u003eBalestro, G., Festa, A., Borghi, A., Castelli, D., Gattiglio M., Tartarotti, P. (2018). Role of Late Jurassic intra-oceanic structural inheritance in the Alpine tectonic evolution of the Monviso meta-ophiolite Complex (Western Alps). \u003cem\u003eGeological Magazine\u003c/em\u003e, 155(2), 233-249, doi:10.1017/S0016756817000553.\u003c/li\u003e\n\u003c/ol\u003e"}],"fulltextSource":"","fullText":"","funders":[],"hasAdminPriorityOnWorkflow":false,"hasManuscriptDocX":true,"hasOptedInToPreprint":true,"hasPassedJournalQc":"","hasAnyPriority":false,"hideJournal":false,"highlight":"","institution":"","isAcceptedByJournal":false,"isAuthorSuppliedPdf":false,"isDeskRejected":"","isHiddenFromSearch":false,"isInQc":false,"isInWorkflow":false,"isPdf":false,"isPdfUpToDate":true,"isWithdrawnOrRetracted":false,"journal":{"display":true,"email":"[email protected]","identity":"npj-heritage-science","isNatureJournal":false,"hasQc":true,"allowDirectSubmit":false,"externalIdentity":"hsci","sideBox":"Learn more about [Heritage Science](http://heritagesciencejournal.springeropen.com)","snPcode":"40494","submissionUrl":"https://submission.nature.com/new-submission/40494/3","title":"npj Heritage Science","twitterHandle":"@SpringerOpen","acdcEnabled":true,"dfaEnabled":true,"editorialSystem":"em","reportingPortfolio":"BMC/SO AJ","inReviewEnabled":true,"inReviewRevisionsEnabled":true},"keywords":"Greenstone, Eclogite, Jadeitite, Omphacitite, Neolithic implement","lastPublishedDoi":"10.21203/rs.3.rs-9051667/v1","lastPublishedDoiUrl":"https://doi.org/10.21203/rs.3.rs-9051667/v1","license":{"name":"CC BY 4.0","url":"https://creativecommons.org/licenses/by/4.0/"},"manuscriptAbstract":"\u003cp\u003eArtefacts in presumed \u0026lsquo;\u003cem\u003ejade\u003c/em\u003e\u0026rsquo; were used all over Europe during Neolithic. Their archaeometric investigation, due to this geo-resource scarcity, allows extrapolating info about supply sources and/or trades. The \u003cem\u003egreenstone\u003c/em\u003e industry of the \u003cem\u003eRocca di Cavour\u003c/em\u003e settlement was characterized and compared to geologic \u0026lsquo;jades\u0026rsquo; from circumscribed \u0026ndash; yet mostly unmapped \u0026ndash; outcrops on the Monviso Massif and adjoining valleys. Most tools are made of eclogite, jadeitite and omphacitite \u0026ndash; a distribution found also in natural samples. The systematic detection of peculiar petrographic features confirms that all artefacts derive from the Monviso and highlights that these rocks form after metasomatic processes in shear-zones rich in aqueous fluids, typical of Western Alps \u0026ndash; justifying their actual location and scarceness. Despite this, they were specifically sought after due to their technological potential, producing tools whose distribution expanded far beyond their sources. Relict surfaces suggest these artefacts were shaped by pebbles/cobbles from the Pellice or Po Rivers alluvial deposits.\u003c/p\u003e","manuscriptTitle":"Neolithic artefacts in ‘Jade’ from Rocca di Cavour (Northwestern-Italy): archaeometric characterization, geologic contextualization and provenance","msid":"","msnumber":"","nonDraftVersions":[{"code":1,"date":"2026-03-13 12:33:28","doi":"10.21203/rs.3.rs-9051667/v1","editorialEvents":[{"type":"communityComments","content":0},{"type":"decision","content":"Revision requested","date":"2026-04-06T12:36:57+00:00","index":"","fulltext":""},{"type":"editorInvitedReview","content":"","date":"2026-04-02T15:14:38+00:00","index":"hide","fulltext":""},{"type":"editorInvitedReview","content":"","date":"2026-03-29T18:12:04+00:00","index":"hide","fulltext":""},{"type":"editorInvitedReview","content":"","date":"2026-03-26T16:05:14+00:00","index":"hide","fulltext":""},{"type":"reviewerAgreed","content":"160037990987320474446481529623673647060","date":"2026-03-12T09:01:45+00:00","index":"hide","fulltext":""},{"type":"reviewerAgreed","content":"131925689921050912489341446077543359571","date":"2026-03-11T14:23:16+00:00","index":"hide","fulltext":""},{"type":"reviewerAgreed","content":"118171392145413331588557055860538990982","date":"2026-03-11T13:22:14+00:00","index":"hide","fulltext":""},{"type":"reviewersInvited","content":"","date":"2026-03-11T12:53:19+00:00","index":"","fulltext":""},{"type":"editorAssigned","content":"","date":"2026-03-09T12:51:35+00:00","index":"","fulltext":""},{"type":"checksComplete","content":"","date":"2026-03-09T12:50:55+00:00","index":"","fulltext":""},{"type":"submitted","content":"npj Heritage Science","date":"2026-03-06T14:33:50+00:00","index":"","fulltext":""}],"status":"published","journal":{"display":true,"email":"[email protected]","identity":"npj-heritage-science","isNatureJournal":false,"hasQc":true,"allowDirectSubmit":false,"externalIdentity":"hsci","sideBox":"Learn more about [Heritage Science](http://heritagesciencejournal.springeropen.com)","snPcode":"40494","submissionUrl":"https://submission.nature.com/new-submission/40494/3","title":"npj Heritage Science","twitterHandle":"@SpringerOpen","acdcEnabled":true,"dfaEnabled":true,"editorialSystem":"em","reportingPortfolio":"BMC/SO AJ","inReviewEnabled":true,"inReviewRevisionsEnabled":true}}],"origin":"","ownerIdentity":"d2e9c2eb-97dc-43e6-86b7-0ea71fb9d6b6","owner":[],"postedDate":"March 13th, 2026","published":true,"recentEditorialEvents":[],"rejectedJournal":[],"revision":"","amendment":"","status":"in-revision","subjectAreas":[],"tags":[],"updatedAt":"2026-04-06T12:40:22+00:00","versionOfRecord":[],"versionCreatedAt":"2026-03-13 12:33:28","video":"","vorDoi":"","vorDoiUrl":"","workflowStages":[]},"version":"v1","identity":"rs-9051667","journalConfig":"researchsquare"},"__N_SSP":true},"page":"/article/[identity]/[[...version]]","query":{"redirect":"/article/rs-9051667","identity":"rs-9051667","version":["v1"]},"buildId":"XKTyCvWXoU3ODBz1xrDgd","isFallback":false,"isExperimentalCompile":false,"dynamicIds":[84888],"gssp":true,"scriptLoader":[]}