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Monte Amiata is a small volcano composed by trachytic to olivine latitic lava flows and domes emplaced in a very short time between 305 and 231 ka. The main petrographic features are represented by the occurrence of i) abundant rounded magmatic enclaves increasing in dimension and quantity passing from early to late erupted Monte Amiata volcanic rocks, ii) large sanidine megacrysts, mainly confined in the second stage of activity characterised by the emplacement of exogenous domes and massive lava flows, and iii) mafic olivine latitic lava flows, with intermediate compositions between the early silica-rich volcanic rocks and the most mafic rounded magmatic enclaves hosted by the Monte Amiata volcanic rocks. The occurrence of rounded magmatic enclaves testifies fresh magma injection and stirring within a differentiated magma reservoir. This triggered the pouring out of the viscous trachydacitic resident magma. A reverse differentiation pathway is observed with time of magma emplacement, which is accompanied by the decrease of silica contents and increase of MgO and compatible elements passing from early trachydacites to final olivine-latites. The same timely reverse differentiation pathway is observed among magmatic enclaves, with the most mafic terms hosted by final olivine-latitic lava flows. Fine-grained rounded magmatic enclaves, indeed, range in composition from potassic trachybasalt (absarokite) to olivine-latite. The overall geochemical and isotopic features agree with a mixing process between a highly differentiated (i.e., high silica), and partially crystallised, high-K calc-alkaline end- member and a mafic ultrapotassic magma possibly leucite-bearing. Absence of leucite in the Amiata rocks and enclaves is due to high-silica activity of derived magmas caused by the high-silica end-member of the mixing process.

The Colli Albani volcano belongs to the Roman Magmatic Province and is character- ized by strongly silica undersaturated leucite-bearing ultrapotassic rocks. Melilite-bearing leuciti- tic lavas, beside tephritic to tephritic phonolitic ignimbrites, were erupted during the pre-caldera (Vulcano Laziale) period. The post-caldera phase opened with magmas erupted from different feeding systems, with melilite-bearing leucitites in the early phases followed by tephritic and pho- nolitic tephritic lavas. The late-stage activity (i.e. the Via dei Laghi period) is characterized by hydromagmatic tuffs with small juvenile fragments that prevent a clear compositional definition of the magma triggering the eruptions. Despite their mineralogical and compositional similarities, the Vulcano Laziale period (pre-caldera) has significantly higher levels of incompatible trace elements and 87Sr/86Sr isotopes than found in magmatic rocks erupted after the caldera formation. Pre- and post-caldera parental magmas are considered to be significantly different from each other and generated within a metasomatized upper mantle under different degrees of partial melting. Crustal-derived carbonate-rich metasomatism is thought to have affected the mantle wedge of the Italian peninsula. Melting of pelitic sediments with different amounts of CaCO3 is considered the source of the metasomatic agents, which are able to re-fertilize the lithospheric upper mantle. Partial melting of this modally metasomatized lithospheric mantle under high XCO 2 produced the strongly silica undersaturated ultrapotassic magmas observed at the Colli Albani volcano. A second-order differentiation process occurs at shallow levels, with fractional crystallization and crustal assimilation of wall rock (AFC), locally changing the compositions of magmas and pro- ducing several differentiation pathways that have given rise to the geochemical and petrological complexity of the Colli Albani volcano. Assimilation of carbonate sediments and silicoclastic sedimentary lithologies also occurred coevally, suggesting the existence of several separate magmatic reservoirs at shallow levels, possibly at different depths and surrounded by different sedimentary formations.

High-MgO ultrapotassic rocks are found in four different areas of the Western Mediterranean basin associated in space and time with shoshonitic and calc-alkaline rocks. They represent different magmatic events at the active continental plate margin from Oligocene to Pleistocene. These rocks are found within the Western Alps (Northern Italy), in Corsica (France), in Murcia-Almeria (South-Eastern Spain), and in Southern Tuscany (Central Italy). Ultrapotassic terms are mostly lamprophyres, but olivine latitic lavas with a clear lamproitic affinity are also found. Lamproite-like rocks range from slightly silica under-saturated to silica over-saturated, and they are characterised by low Al2O3, CaO, and Na2O contents. They are plagioclase-free rocks, but K-feldspar is abundant beside other K-bearing phases. Shoshonitic and calc-alkaline rocks are invariably space associated to lamproites, and they either precede or follow them. High-Mg ultrapotassic rocks are characterised by strong enrichment of incompatible elements, which prevent further enrichment due to shallow level crustal contamination. K2O and incompatible element contents decrease passing from high-Mg ultrapotassic to high-Mg shoshonitic and calc-alkaline rocks suggesting that K and incompatible trace elements enrichments are a primary characteristic. Ultrapotassic to calc-alkaline rocks from Western Mediterranean regions, in spite of their different age of emplacement, are characterised by similar incompatible trace elements distribution. Depletion of High Field Strength elements with respect to Large Ion Lithophile elements is observed. Positive spikes at Th, U, and Pb, with negative spikes at Ba, Nb, Ta, Sr, P, and Ti, are common characteristics of ultrapotassic (lamproitic) to high-K calc-alkaline rocks. Ultrapotassic rocks are extremely enriched in radiogenic Sr and unradiogenic Nd with respect to the associated shoshonitic and calc-alkaline rocks. Different isotopic values are distinctive of the different magmatic provinces irrespective of magmatic affinities. 87Sr/86Sri ranges between 0.71645 and 0.71759 for Western Alps lamproites, between 0.71226 and 0.71230 for Corsica lamproite, between 0.71642 and 0.72259 for Murcia-Almeria lamproites, and between 0.71578 and 0.71672 for Tuscany lamproites. Radiogenic Sr decreases along with K2O through shoshonitic to calc-alkaline rocks. Conversely 143Nd/144Ndi values increase with decreasing K2O, with the highest value of 0.51243 found for the one samples from Murcia-Almeria. Contrasting trends are observed among initial values of lead isotopes, but all falling well within the field of upper crustal rocks. Different trends of 207Pb/204Pbi and 208Pb/204Pbi vs. 206Pb/204Pbi for samples from the different provinces are observed. Several evidences indicate that most of the magmas of the different provinces have been generated in a depleted upper mantle (i.e., lithospheric) modified by metasomatism, but an asthenospheric component is also recognised in Corsica. At least two different subduction-related metasomatic agents re-fertilised the depleted original upper mantle source. Carbonate-free siliciclastic sediments and carbonate-rich sediments have been recycled within the upper mantle through subduction and partial melting. Assuming that metasomatic component is concentrated in a vein network, in Tuscany and Corsica, time relationships indicate that low degree of partial melting of the pure vein produced lamproitic-like magmas, whereas an increase in the partial melting involve the surrounding upper mantle, then diluting the alkaline component and produced the entire spectra of magma observed. In South-Eastern Spain calc-alkaline magmatism preceded lamproitic ones, and might be generated by partial melting of mantle wedge metasomatised by fluids from oceanic slab prior to collision. Lamproitic magmas followed after melt-dominated metasomatic agents invaded the lithospheric upper mantle domain. Migration of the magmatism with time is the result of eastward migration of subduction with subsequent opening of Balearic, Ligure-Provençal, and Tyrrhenian basins.

The “Colli Albani” composite volcano is made up of strongly silica-undersaturated leucite-bearing rocks. Magmas were erupted during three main periods, but a complex plumbing system dominated by regional tectonics channelled magmas into different reservoirs. The most alkali-rich magmas, restricted to the caldera-forming period (pre-caldera), are extremely enriched in incompatible trace elements and display more radiogenic Sr (87Sr/86Sr = 0.71057–0.71067), with slightly less radiogenic Pb with respect to those of the post-caldera period. Post-caldera volcanic activity was concentrated in three different volcanic environments: external to the caldera, along the caldera edge and within the caldera. The post-caldera magmas produced melilite- to leucitite-bearing, plagioclase-free leucitites. In contrast to the pre-caldera lavas, they are characterised by lower incompatible trace element abundances and less radiogenic Sr ( 87 Sr / 8 6Sr = 0. 71006–0. 71039) . Magmas evolved through crystal fractionation plus minor crustal assimilation in a large magma chamber during the pre- caldera period. The multiple caldera collapses dissected and partially obliterated the early magma chamber. During the post-caldera stage, magmas were channelled through several pathways and multiple shallow-level magma reservoirs were established. A lithospheric mantle wedge previously depleted in the basaltic component and subsequently enriched by metasomatic slab-derived component is suggested as the mantle source of Colli Albani parental magmas. Two different parental magmas are recognised for the pre- and post-caldera stages. The differences may be related to the interplay between smaller degrees of melting for the pre-caldera magmas and more carbonate-rich recycled subducted lithologies in the post-caldera magmas.

En este trabajo se presentan y describen flujos de lava extremadamente largos. Estos flujos se originaron en el complejo volcánico fisural Payen, dentro de la provincia volcánica Payenia en el retroarco andino. Los flujos de lava fueron emitidos durante el Cuaternario tardío desde el sector superior de un volcán en escudo, el que constituyó el primer centro volcánico de este complejo. Uno de estos flujos presenta forma de lengua y tiene una longitud de 181 km, constituyendo el flujo de lava cuaternario conocido, más largo sobre la Tierra. Este flujo alcanzó el valle del río Salado en La Pampa y mantuvo una forma angosta y recta sin ningún control topográfico, hasta su porción más distal sobre una planicie aluvial. La roca que forma esta colada es una hawaita con un bajo contenido de fenocristales de olivino y plagioclasa. Los patrones de elementos traza son típicos de basaltos alcalino-sódicos de intraplaca, sin embargo el patrón de elementos traza incompatibles y las relaciones de isótopos de Sr y Nd, sugieren un marco transicional al orogénico. El flujo estudiado fluyó siguiendo un mecanismo térmicamente eficiente denominado inflation, como demuestran las asociaciones de sus rasgos morfológicos, estructurales y texturales. Las causas principales de este sistema de transporte extremadamente largo pueden ser una temperatura de 1.130º-1160ºC y viscosidad de 3-73 Pa*s (calculadas a partir de los datos petroquímicos), junto con una muy baja velocidad de enfriamiento y una tasa de efusión grande y sostenida en el tiempo. La gran longitud y la falta parcial de control topográfico del flujo pueden aportar nuevos conocimientos acerca de la física de los grandes flujos inflados, los que constituyen las más extensas provincias volcánicas de la Tierra y probablemente también la de otros planetas terrestres. Extremely long basaltic lava flows are here presented and described. The flows originated from the great, polygenetic, fissural Payen Volcanic Complex, in the Andean back-arc volcanic province of Payenia in Argentina. The lava flows outpoured during the Late Quaternary from the summit rift of a shield volcano representing the first volcanic centre of this complex. One of these flows presents an individual tongue-like shape with a length of 181 km and therefore is the longest known individual Quaternary lava flow on Earth. Leaving the flanks of the volcano this flow reached the Salado river valley at La Pampa and, in its distal portion, maintained its narrow and straight shape without any topographic control over a flat alluvial plain. It has a hawaiite composition with low phenocryst content of prevailing olivine and minor plagioclase. Rare Earth element patterns are typical of Na-alkaline basalts, but incompatible trace element patterns and Sr -Nd isotope ratios, suggest a geodynamic setting transitional to the orogenic one. The flow advanced following the thermally efficient "inflation" mechanism, as demonstrated by a peculiar association of well developed morphological, structural and textural features. The temperature of 1130-1160°C and the viscosity of 3-73 Pa*s, calculated by petrochemical data, may be considered, together with a very low cooling rate and a sustained and long lasting effusion rate, the main causes of the extremely long transport system of this flow. Both the extreme length of the flow and the partial lack of topographic control may provide new constraints on the physics of large inflated flows, which constitute the largest volcanic provinces on Earth and probably also on the terrestrial planets. Fil: Pasquare, Giorgio. Università degli Studi di Milano; Italia Fil: Bistacchi, Andrea. Università Degli Studi Di Milano-bicocca; Italia Fil: Francalanci, Lorella. Università degli Studi di Firenze; Italia Fil: Bertotto, Gustavo Walter. Consejo Nacional de Investigaciones Científicas y Técnicas. Instituto de Ciencias de la Tierra y Ambientales de La Pampa. Universidad Nacional de La Pampa. Facultad de Ciencias Exactas y Naturales. Instituto de Ciencias de la Tierra y Ambientales de La Pampa; Argentina Fil: Boari, Elena. Università degli Studi di Firenze; Italia Fil: Massironi, Matteo. Università di Padova; Italia Fil: Rossotti, Andrea. Universitá Degli Studi Dell´insubria; Italia

The Roccamonfina Volcano is characterised by a two stage volcanic activity, divided by volcano- tectonic collapses. Ultrapotassic leucite-bearing rocks are confined in the pre-caldera stage and display geochemical characteristics very similar to those of other volcanoes of the Roman Province. Shoshonitic rocks have been poured out from cinder cones and domes both within the caldera and on the external flanks of the pre-caldera Roccamonfina volcano. On the basis of new trace element and Sr-Nd-Pb isotope data, Roccamonfina shoshonitic rocks show differences with respect to shoshonites from Northern Roman Province, and recall closely those of the Neapolitan volcanoes. Eventually, in the very last phases of volcanic activity, sub-alkaline magmas are found both as enclaves in trachytic domes, and as final lavas vented by a fracture within the Monte Santa Croce dome. Ultrapotassic rocks that built up the pre-caldera composite volcano are plagioclase-bearing leucitites and, similarly to other Roman Provinces volcanoes, have by high levels of incompatible trace elements with an orogenic signature having troughs at Ba, Ta, Nb, Ta, and Ti, and peaks at Cs, K, Th, U, and Pb. Initial values of 87Sr/86Sr range from 0.709261 to 0.709987, of 143Nd/144Nd range from 0.512134 to 512195, of 206Pb/204Pb range from 18.788 to 18.851, of 207Pb/204Pb range from 15.685 to 15.701, and of 208Pb/204Pb range from 39.048 to 39.076. Shoshonites show a larger differentiation degree but, as a whole, lower levels of incompatible trace elements with similar pattern of incompatible trace element contents with respect to earlier ultrapotassic leucite-bearing rocks. On the other hand, shoshonitic rocks have Sr, Nd, and Pb isotopes consistently different than pre-caldera ultrapotassic leucite-bearing rocks. 87Sr/86Sr ranges from 0.706604 to 0.708332, 143Nd/144Nd ranges from 0.512179 to 0.512382, 206Pb/204Pb ranges from 18.838 to 19.153, 207Pb/204Pb ranges from 15.661 to 15.694, and 208Pb/204Pb ranges from 38.999 to 39.212. High-K calc-alkaline samples have intermediate isotopic values between ultrapotassic plagioclase leucitites and shoshonites, but the lowest levels of incompatible trace element contents. The genesis of this uncommon association is investigated in details. It is argued that ultrapotassic magmas have been generated in a modified lithospheric mantle after crustal- derived metasomatism. Interaction between metasomatic agent and lithospheric upper mantle produced a low-melting metasomatised veined network. Pure partial melting of vein mineralogy produced pre-caldera leucite-bearing ultrapotassic magmas. Leucite-free magmas have been generated further melting, at higher temperature, of the same meltasomatic mantle previously depleted by the ectraction of ultrapotassic rocks. We suggest that a key role in this second episode of melting is played by little but significant addition of astenospheric upper mantle material from foreland mantle, flowing through the corner of the Ionian present day subducted slab during its roll-back

In Italy and surroundings, leucite-free (i.e., lamproites), leucite-bearing (i.e., kamafugites, leucitites, plagioclase-leucitites), and haüyne-bearing (i.e., haüynites, haüyne-leucitites) ultrapotassic igneous rocks have been recorded from Oligocene to present in association with shoshonitic, and high-K calc-alkaline volcanic rocks. The oldest outcrops of ultrapotassic and related rocks are found within the western Alps in the form of lamprophyric to calc-alkaline dykes intruded during the Oligocene. Four different magmatic provinces, characterised by the association of ultrapotassic igneous rocks with shoshonitic to calc-alkaline series, are also found along the Tyrrhenian margin of the peninsula. These rocks have been produced from Miocene to Holocene with an eastward/southeastward migration with time. Leucite-free silica-rich ultrapotassic lamproitic rocks are restricted to the early stages of magmatism, whereas ultrapotassic leucite-bearing rocks to the middle and late stages. Mafic ultrapotassic igneous rocks are enriched in incompatible trace elements, with variable fractionation of Ta, Nb, and Ti with respect to Th and Large Ion Lithophile elements, and variable enrichment in radiogenic Sr and Pb and unradiogenic Nd. These characteristics are reconducted to sediment recycling within the upper mantle via subduction. Recycling of carbonate-rich pelites plays an important role in the genesis of leucite-bearing magmas. Large volume of metasomatic components is predicted to be accommodated within a vein network in the sub- continental lithospheric mantle. Partial melting of the vein generates ultrapotassic magmas, either lamproitic or kamafugitic. Increased interaction between the metasomatic veins and the surrounding mantle dilutes the alkaline component producing shoshonites and high-K calc-alkaline suites. The addition of a further subduction-related component shortly before magma generation is required to explain the isotopic composition of rocks from the Neapolitan district, together with the probable arrival of a within-plate component from the Adria mantle through slab- tear.

High-MgO ultrapotassic rocks are found in four different areas of the Western Mediterranean basin associated in space and time with shoshonitic and calc-alkaline rocks. They represent different magmatic events at the active continental plate margin from Oligocene to Pleistocene. These rocks are found within the Western Alps (Northern Italy), in Corsica (France), in Murcia-Almeria (South-Eastern Spain), and in Southern Tuscany (Central Italy). Ultrapotassic terms are mostly lamprophyres, but olivine latitic lavas with a clear lamproitic affinity are also found. Lamproite-like rocks range from slightly silica under-saturated to silica over-saturated, and they are characterised by low Al(2)O(3), CaO, and Na(2)O contents. They are plagioclase-free rocks, but K-feldspar is abundant beside other K-bearing phases. Shoshonitic and calc-alkaline rocks are invariably space associated to lamproites, and they either precede or follow them. High-Mg ultrapotassic rocks are characterised by strong enrichment of incompatible elements, which prevent further enrichment due to shallow level crustal contamination. K(2)O and incompatible element contents decrease passing from high-Mg ultrapotassic to high-Mg shoshonitic and calc-alkaline rocks suggesting that K(2)O and incompatible trace elements enrichments are a primary characteristic. Ultrapotassic to calc-alkaline rocks from Western Mediterranean regions, in spite of their different age of emplacement, are characterised by similar incompatible trace elements distribution. Depletion of High Field Strength elements with respect to Large Ion Lithophile elements is observed. Positive spikes at Th, U, and Pb, with negative spikes at Ba, Nb, Ta, Sr, P, and Ti, are common characteristics of ultrapotassic (lamproitic) to high-K calc-alkaline rocks. Ultrapotassic rocks are extremely enriched in radiogenic Sr and unradiogenic Nd with respect to the associated shoshonitic and calc-alkaline rocks. Different isotopic values are distinctive of the different magmatic provinces irrespective of magmatic affinities. (87)Sr/(36)Sr(i) ranges between 0.71645 and 0.71759 for Western Alps lamproites, between 0.71226 and 0.71230 for Corsica lamproite, between 0.71642 and 0.72259 for Murcia-Almeria lamproites, and between 0.71578 and 0.71672 for Tuscany lamproites. Radiogenic Sr decreases along with K(2)O through shoshonitic to calc-alkaline rocks. Conversely (143)Nd/(144)Nd(i) values increase with decreasing K(2)O with the highest value of 0.51243 found for the one samples from Murcia-Almeria. Contrasting trends are observed among initial values of lead isotopes, but all falling well within the field of upper crustal rocks. Different trends of (207)Pb/(204)Pb(i) and (208)Pb/(204)Pb(i) VS. (206)Pb/(204)Pb(i) for samples from the different provinces are observed. Several evidences indicate that most of the magmas of the different provinces have been generated in a depleted upper mantle (i.e., lithospheric) modified by metasomatism, but an asthenospheric component is also recognised in Corsica. At least two different subduction-related metasomatic agents re-fertilised the depleted original upper mantle source. Carbonate-free siliciclastic sediments and carbonate-rich sediments have been recycled within the upper mantle through subduction and partial melting. Assuming that metasomatic component is concentrated in a vein network, in Tucany and Corsica, time relationships indicate that low degree of partial melting of the pure vein produced lamproitic-like magmas, whereas an increase in the partial melting involve the surrounding upper mantle, then diluting the alkaline component and produced the entire spectra of magma observed. In South-Eastern Spain calc-alkaline magmatism preceded lamproitic ones, and might be generated by partial melting of mantle wedge metasomatised by fluids from oceanic slab prior to collision. Lamproitic magmas followed after melt-dominated metasomatic agents invaded the lithospheric upper mantle domain. Migration of the magmatism with time is the result of eastward migration of subduction with subsequent opening of Balearic, Ligure-Provencal, and Tyrrhenian basins. (C) 2008 Elsevier B.V. All rights reserved.