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</a></div></div></div></div><div class="right-panel-container"><div class="user-content-wrapper"><div class="uploads-container" id="social-redesign-work-container"><div class="upload-header"><h2 class="ds2-5-heading-sans-serif-xs">Uploads</h2></div><div class="documents-container backbone-social-profile-documents" style="width: 100%;"><div class="u-taCenter"></div><div class="profile--tab_content_container js-tab-pane tab-pane active" id="all"><div class="profile--tab_heading_container js-section-heading" data-section="Papers" id="Papers"><h3 class="profile--tab_heading_container">Papers by Claudia D'Oriano</h3></div><div class="js-work-strip profile--work_container" data-work-id="23855003"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/23855003/Magmatic_processes_revealed_by_textural_and_compositional_features_of_large_anorthoclase_crystals_from_the_Lajes_Angra_Ignimbrite_Terceira_Island_Azores_"><img alt="Research paper thumbnail of Magmatic processes revealed by textural and compositional features of large anorthoclase crystals from the Lajes-Angra Ignimbrite (Terceira Island, Azores)" class="work-thumbnail" src="https://attachments.academia-assets.com/44249626/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/23855003/Magmatic_processes_revealed_by_textural_and_compositional_features_of_large_anorthoclase_crystals_from_the_Lajes_Angra_Ignimbrite_Terceira_Island_Azores_">Magmatic processes revealed by textural and compositional features of large anorthoclase crystals from the Lajes-Angra Ignimbrite (Terceira Island, Azores)</a></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Lajes-Angra Ignimbrite (LAI) is the most recent (around 21 ka) caldera-forming event produced by ...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Lajes-Angra Ignimbrite (LAI) is the most recent (around 21 ka) caldera-forming event produced by Pico Alto volcano at Terceira Island (Azores). Lajes-Angra Ignimbrite Formation comprises two members closely spaced in time: Lajes and Angra. The Lajes member, the most widely distributed throughout the island, was sampled at two sites: 1) at Lajes (type location), in the northern part of the island, where the succession is characterized by a thin crystal-rich basal layer (TERS 17.1) overlaid by a fine-grained welded lapilli-tuff layer and an upper partially welded coarse clast-bearing layer (TERS 17.2); 2) at São Mateus, in the south coast, where the upper layer of the succession is also partially welded (TERS 62.1). Juvenile clasts are comenditic-trachyte in composition and coarsely porphyritic, ranging from highly vesicular pumice to dense vitrophyric clasts. Mineral assemblage mainly consists of anorthoclase (Ab64-70, An<7 mol%), and less abundant olivine (Fo28-45), clinopyroxene (En60-80Fs20-40), ilmenite and magnetite. Phenocrysts of anorthoclase range in size from < 2mm in the crystal-rich basal layer, up to 4-5 mm in the partially welded upper layer. We found that, except for the basal layer, in the other two samples, large crystals of anorthoclase include pockets of highly vesicular melts ( ). Large crystals with similar textures are quite common in trachytic magmas at Pantelleria and in other silicic magmas. In addition to vesicular glass, these crystals also include vesicles not rimmed by glass. The borders of glassy pockets can be both smooth and angular, and usually marked by a line of Fe-rich melt. This melt is enriched in elements that are not admitted into anorthoclase (Ca, Fe, Mg, Ti) and depleted in Si, Al, K and to a lesser extent in Na. The vesicular glass in the pockets is a comendite-trachyte with composition quite similar to that of the matrix glass. Despite the large phenocrysts appear compositionally homogeneous at SEM, the cathodoluminescence imaging spectroscopy reveals complex growing textures. Crystals are patchy-zoned, with resorbed cores and inclusions-free rims (100-300 µm) ( . Preliminary LAM-ICP-MS analyses of anorthoclases highlighted a large trace-element compositional variation, which is also evident at the scale of the single crystal. Our interest is to understand HOW and WHY the large glass pockets-bearing anorthoclases were formed and if they were related to dissolution or rapid growth, during pre-or syn-eruption degassing processes. Textural and geochemical data are used to obtain information on: i) the evolution of the shallow reservoir; ii) relation between magma and crystal mush; iii) syn-eruptive processes of crystallization-induced degassing. Results are discussed in terms of growth mechanisms of crystals and magma dynamics immediately before or during the eruptive event.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="489e23520e7e2de3a5c1c29f3f7bf974" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":44249626,"asset_id":23855003,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/44249626/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="23855003"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="23855003"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 23855003; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=23855003]").text(description); $(".js-view-count[data-work-id=23855003]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 23855003; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='23855003']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "489e23520e7e2de3a5c1c29f3f7bf974" } } $('.js-work-strip[data-work-id=23855003]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":23855003,"title":"Magmatic processes revealed by textural and compositional features of large anorthoclase crystals from the Lajes-Angra Ignimbrite (Terceira Island, Azores)","translated_title":"","metadata":{"grobid_abstract":"Lajes-Angra Ignimbrite (LAI) is the most recent (around 21 ka) caldera-forming event produced by Pico Alto volcano at Terceira Island (Azores). Lajes-Angra Ignimbrite Formation comprises two members closely spaced in time: Lajes and Angra. The Lajes member, the most widely distributed throughout the island, was sampled at two sites: 1) at Lajes (type location), in the northern part of the island, where the succession is characterized by a thin crystal-rich basal layer (TERS 17.1) overlaid by a fine-grained welded lapilli-tuff layer and an upper partially welded coarse clast-bearing layer (TERS 17.2); 2) at São Mateus, in the south coast, where the upper layer of the succession is also partially welded (TERS 62.1). Juvenile clasts are comenditic-trachyte in composition and coarsely porphyritic, ranging from highly vesicular pumice to dense vitrophyric clasts. Mineral assemblage mainly consists of anorthoclase (Ab64-70, An\u003c7 mol%), and less abundant olivine (Fo28-45), clinopyroxene (En60-80Fs20-40), ilmenite and magnetite. Phenocrysts of anorthoclase range in size from \u003c 2mm in the crystal-rich basal layer, up to 4-5 mm in the partially welded upper layer. We found that, except for the basal layer, in the other two samples, large crystals of anorthoclase include pockets of highly vesicular melts ( ). Large crystals with similar textures are quite common in trachytic magmas at Pantelleria and in other silicic magmas. In addition to vesicular glass, these crystals also include vesicles not rimmed by glass. The borders of glassy pockets can be both smooth and angular, and usually marked by a line of Fe-rich melt. This melt is enriched in elements that are not admitted into anorthoclase (Ca, Fe, Mg, Ti) and depleted in Si, Al, K and to a lesser extent in Na. The vesicular glass in the pockets is a comendite-trachyte with composition quite similar to that of the matrix glass. Despite the large phenocrysts appear compositionally homogeneous at SEM, the cathodoluminescence imaging spectroscopy reveals complex growing textures. Crystals are patchy-zoned, with resorbed cores and inclusions-free rims (100-300 µm) ( . Preliminary LAM-ICP-MS analyses of anorthoclases highlighted a large trace-element compositional variation, which is also evident at the scale of the single crystal. Our interest is to understand HOW and WHY the large glass pockets-bearing anorthoclases were formed and if they were related to dissolution or rapid growth, during pre-or syn-eruption degassing processes. Textural and geochemical data are used to obtain information on: i) the evolution of the shallow reservoir; ii) relation between magma and crystal mush; iii) syn-eruptive processes of crystallization-induced degassing. Results are discussed in terms of growth mechanisms of crystals and magma dynamics immediately before or during the eruptive event.","grobid_abstract_attachment_id":44249626},"translated_abstract":null,"internal_url":"https://www.academia.edu/23855003/Magmatic_processes_revealed_by_textural_and_compositional_features_of_large_anorthoclase_crystals_from_the_Lajes_Angra_Ignimbrite_Terceira_Island_Azores_","translated_internal_url":"","created_at":"2016-03-31T00:55:38.427-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":14420859,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":44249626,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/44249626/thumbnails/1.jpg","file_name":"Magmatic_processes_revealed_by_textural_20160331-25224-48c40n.pdf","download_url":"https://www.academia.edu/attachments/44249626/download_file","bulk_download_file_name":"Magmatic_processes_revealed_by_textural.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/44249626/Magmatic_processes_revealed_by_textural_20160331-25224-48c40n-libre.pdf?1459411720=\u0026response-content-disposition=attachment%3B+filename%3DMagmatic_processes_revealed_by_textural.pdf\u0026Expires=1743974704\u0026Signature=WkNPP8yRsBZsdtPwADGGrkjIdHQv9H~Fy27T7-1eL1soApZxAJD3nUrp7DGelwjnC9DnRrZstbiLyecASQ6eGMfBQ~Eu1IilpH~vQ1iaY9wxl5aSB4CKIPVPLh~s2iz8Ju6RE8ziXgplyC98P~BEAmpr2wGIBG9xxUNqdBFq4ROOHg8Mc62Za1VEa1Gk6IO337eW~fB4kMIPsgASoRkPOt5UPnMWqWvyOGou7OiYdXyLByV9i7YHaMQfjer2ktzrvWNjedTXKdysZ86dBmlupBsTUnaXlhpXnQJ9gxPQzHoSOaDtilwjPJWd0cFABHK1hrS2XV1zCNwXgbMZ9M64Pg__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Magmatic_processes_revealed_by_textural_and_compositional_features_of_large_anorthoclase_crystals_from_the_Lajes_Angra_Ignimbrite_Terceira_Island_Azores_","translated_slug":"","page_count":2,"language":"en","content_type":"Work","summary":"Lajes-Angra Ignimbrite (LAI) is the most recent (around 21 ka) caldera-forming event produced by Pico Alto volcano at Terceira Island (Azores). Lajes-Angra Ignimbrite Formation comprises two members closely spaced in time: Lajes and Angra. The Lajes member, the most widely distributed throughout the island, was sampled at two sites: 1) at Lajes (type location), in the northern part of the island, where the succession is characterized by a thin crystal-rich basal layer (TERS 17.1) overlaid by a fine-grained welded lapilli-tuff layer and an upper partially welded coarse clast-bearing layer (TERS 17.2); 2) at São Mateus, in the south coast, where the upper layer of the succession is also partially welded (TERS 62.1). Juvenile clasts are comenditic-trachyte in composition and coarsely porphyritic, ranging from highly vesicular pumice to dense vitrophyric clasts. Mineral assemblage mainly consists of anorthoclase (Ab64-70, An\u003c7 mol%), and less abundant olivine (Fo28-45), clinopyroxene (En60-80Fs20-40), ilmenite and magnetite. Phenocrysts of anorthoclase range in size from \u003c 2mm in the crystal-rich basal layer, up to 4-5 mm in the partially welded upper layer. We found that, except for the basal layer, in the other two samples, large crystals of anorthoclase include pockets of highly vesicular melts ( ). Large crystals with similar textures are quite common in trachytic magmas at Pantelleria and in other silicic magmas. In addition to vesicular glass, these crystals also include vesicles not rimmed by glass. The borders of glassy pockets can be both smooth and angular, and usually marked by a line of Fe-rich melt. This melt is enriched in elements that are not admitted into anorthoclase (Ca, Fe, Mg, Ti) and depleted in Si, Al, K and to a lesser extent in Na. The vesicular glass in the pockets is a comendite-trachyte with composition quite similar to that of the matrix glass. Despite the large phenocrysts appear compositionally homogeneous at SEM, the cathodoluminescence imaging spectroscopy reveals complex growing textures. Crystals are patchy-zoned, with resorbed cores and inclusions-free rims (100-300 µm) ( . Preliminary LAM-ICP-MS analyses of anorthoclases highlighted a large trace-element compositional variation, which is also evident at the scale of the single crystal. Our interest is to understand HOW and WHY the large glass pockets-bearing anorthoclases were formed and if they were related to dissolution or rapid growth, during pre-or syn-eruption degassing processes. Textural and geochemical data are used to obtain information on: i) the evolution of the shallow reservoir; ii) relation between magma and crystal mush; iii) syn-eruptive processes of crystallization-induced degassing. Results are discussed in terms of growth mechanisms of crystals and magma dynamics immediately before or during the eruptive event.","impression_tracking_id":null,"owner":{"id":14420859,"first_name":"Claudia","middle_initials":null,"last_name":"D'Oriano","page_name":"CDOriano","domain_name":"ingv","created_at":"2014-07-27T18:56:54.386-07:00","display_name":"Claudia D'Oriano","url":"https://ingv.academia.edu/CDOriano"},"attachments":[{"id":44249626,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/44249626/thumbnails/1.jpg","file_name":"Magmatic_processes_revealed_by_textural_20160331-25224-48c40n.pdf","download_url":"https://www.academia.edu/attachments/44249626/download_file","bulk_download_file_name":"Magmatic_processes_revealed_by_textural.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/44249626/Magmatic_processes_revealed_by_textural_20160331-25224-48c40n-libre.pdf?1459411720=\u0026response-content-disposition=attachment%3B+filename%3DMagmatic_processes_revealed_by_textural.pdf\u0026Expires=1743974704\u0026Signature=WkNPP8yRsBZsdtPwADGGrkjIdHQv9H~Fy27T7-1eL1soApZxAJD3nUrp7DGelwjnC9DnRrZstbiLyecASQ6eGMfBQ~Eu1IilpH~vQ1iaY9wxl5aSB4CKIPVPLh~s2iz8Ju6RE8ziXgplyC98P~BEAmpr2wGIBG9xxUNqdBFq4ROOHg8Mc62Za1VEa1Gk6IO337eW~fB4kMIPsgASoRkPOt5UPnMWqWvyOGou7OiYdXyLByV9i7YHaMQfjer2ktzrvWNjedTXKdysZ86dBmlupBsTUnaXlhpXnQJ9gxPQzHoSOaDtilwjPJWd0cFABHK1hrS2XV1zCNwXgbMZ9M64Pg__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":1370,"name":"Volcanology","url":"https://www.academia.edu/Documents/in/Volcanology"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-23855003-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="23855002"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/23855002/Dynamics_of_ash_eruptions_at_Vesuvius"><img alt="Research paper thumbnail of Dynamics of ash eruptions at Vesuvius" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title">Dynamics of ash eruptions at Vesuvius</div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">ABSTRACT In the recent years, continuous ash emission activity, related to mid-low intensity, lon...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">ABSTRACT In the recent years, continuous ash emission activity, related to mid-low intensity, long lasting eruptions, has been increasingly described to occur at different volcanoes worldwide. Focusing on this type of deposits, a retrospective analysis of the stratigraphic successions at Vesuvius revealed that such type of eruptions have occurred repeatedly in the last 4000 years of activity. This type of activity has been overlooked in the past and the mechanism of ash production in these eruptions is not yet clear. The detailed study of the deposits suggests that these eruptions are dominated by discrete phases of repeated emission of a highly fragmented mixture, alternated with violent strombolian episodes. In this study we present morphological, textural and compositional data on the products of two ash eruptions representative of the whole variability of this activity at Vesuvius (Italy), occurred in the periods between the “Avellino” and “Pompeii” Pumice eruptions (AP3, 2,710±60 years B.P.) and after the 512 A.D. eruption, (AS1a). Juvenile fragments from different ash layers throughout the studied stratigraphic sections were fully characterized in terms of external morphology, particle outline parameterization, groundmass texture (in terms of Crystal and Vesicle Size Distributions) and glass composition. Volcanic ash holds information about magma dynamics within the volcanic conduit, where fragmentation occurs and eruption style is decided. Results of our investigations have been interpreted in terms of fragmentation processes, transport and dispositional mechanisms, dynamics of magma ascent ant timing of the eruption. The methodology of ash analysis used for this study has also important implications for tephrochronological studies, adding a complete parameterization of physical and textural properties of the ash to the routinely used compositional data.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="23855002"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="23855002"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 23855002; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=23855002]").text(description); $(".js-view-count[data-work-id=23855002]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 23855002; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='23855002']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=23855002]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":23855002,"title":"Dynamics of ash eruptions at Vesuvius","translated_title":"","metadata":{"abstract":"ABSTRACT In the recent years, continuous ash emission activity, related to mid-low intensity, long lasting eruptions, has been increasingly described to occur at different volcanoes worldwide. Focusing on this type of deposits, a retrospective analysis of the stratigraphic successions at Vesuvius revealed that such type of eruptions have occurred repeatedly in the last 4000 years of activity. This type of activity has been overlooked in the past and the mechanism of ash production in these eruptions is not yet clear. The detailed study of the deposits suggests that these eruptions are dominated by discrete phases of repeated emission of a highly fragmented mixture, alternated with violent strombolian episodes. In this study we present morphological, textural and compositional data on the products of two ash eruptions representative of the whole variability of this activity at Vesuvius (Italy), occurred in the periods between the “Avellino” and “Pompeii” Pumice eruptions (AP3, 2,710±60 years B.P.) and after the 512 A.D. eruption, (AS1a). Juvenile fragments from different ash layers throughout the studied stratigraphic sections were fully characterized in terms of external morphology, particle outline parameterization, groundmass texture (in terms of Crystal and Vesicle Size Distributions) and glass composition. Volcanic ash holds information about magma dynamics within the volcanic conduit, where fragmentation occurs and eruption style is decided. Results of our investigations have been interpreted in terms of fragmentation processes, transport and dispositional mechanisms, dynamics of magma ascent ant timing of the eruption. The methodology of ash analysis used for this study has also important implications for tephrochronological studies, adding a complete parameterization of physical and textural properties of the ash to the routinely used compositional data."},"translated_abstract":"ABSTRACT In the recent years, continuous ash emission activity, related to mid-low intensity, long lasting eruptions, has been increasingly described to occur at different volcanoes worldwide. Focusing on this type of deposits, a retrospective analysis of the stratigraphic successions at Vesuvius revealed that such type of eruptions have occurred repeatedly in the last 4000 years of activity. This type of activity has been overlooked in the past and the mechanism of ash production in these eruptions is not yet clear. The detailed study of the deposits suggests that these eruptions are dominated by discrete phases of repeated emission of a highly fragmented mixture, alternated with violent strombolian episodes. In this study we present morphological, textural and compositional data on the products of two ash eruptions representative of the whole variability of this activity at Vesuvius (Italy), occurred in the periods between the “Avellino” and “Pompeii” Pumice eruptions (AP3, 2,710±60 years B.P.) and after the 512 A.D. eruption, (AS1a). Juvenile fragments from different ash layers throughout the studied stratigraphic sections were fully characterized in terms of external morphology, particle outline parameterization, groundmass texture (in terms of Crystal and Vesicle Size Distributions) and glass composition. Volcanic ash holds information about magma dynamics within the volcanic conduit, where fragmentation occurs and eruption style is decided. Results of our investigations have been interpreted in terms of fragmentation processes, transport and dispositional mechanisms, dynamics of magma ascent ant timing of the eruption. The methodology of ash analysis used for this study has also important implications for tephrochronological studies, adding a complete parameterization of physical and textural properties of the ash to the routinely used compositional data.","internal_url":"https://www.academia.edu/23855002/Dynamics_of_ash_eruptions_at_Vesuvius","translated_internal_url":"","created_at":"2016-03-31T00:55:38.231-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":14420859,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[],"slug":"Dynamics_of_ash_eruptions_at_Vesuvius","translated_slug":"","page_count":null,"language":"en","content_type":"Work","summary":"ABSTRACT In the recent years, continuous ash emission activity, related to mid-low intensity, long lasting eruptions, has been increasingly described to occur at different volcanoes worldwide. Focusing on this type of deposits, a retrospective analysis of the stratigraphic successions at Vesuvius revealed that such type of eruptions have occurred repeatedly in the last 4000 years of activity. This type of activity has been overlooked in the past and the mechanism of ash production in these eruptions is not yet clear. The detailed study of the deposits suggests that these eruptions are dominated by discrete phases of repeated emission of a highly fragmented mixture, alternated with violent strombolian episodes. In this study we present morphological, textural and compositional data on the products of two ash eruptions representative of the whole variability of this activity at Vesuvius (Italy), occurred in the periods between the “Avellino” and “Pompeii” Pumice eruptions (AP3, 2,710±60 years B.P.) and after the 512 A.D. eruption, (AS1a). Juvenile fragments from different ash layers throughout the studied stratigraphic sections were fully characterized in terms of external morphology, particle outline parameterization, groundmass texture (in terms of Crystal and Vesicle Size Distributions) and glass composition. Volcanic ash holds information about magma dynamics within the volcanic conduit, where fragmentation occurs and eruption style is decided. Results of our investigations have been interpreted in terms of fragmentation processes, transport and dispositional mechanisms, dynamics of magma ascent ant timing of the eruption. The methodology of ash analysis used for this study has also important implications for tephrochronological studies, adding a complete parameterization of physical and textural properties of the ash to the routinely used compositional data.","impression_tracking_id":null,"owner":{"id":14420859,"first_name":"Claudia","middle_initials":null,"last_name":"D'Oriano","page_name":"CDOriano","domain_name":"ingv","created_at":"2014-07-27T18:56:54.386-07:00","display_name":"Claudia D'Oriano","url":"https://ingv.academia.edu/CDOriano"},"attachments":[],"research_interests":[],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-23855002-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="23855001"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/23855001/And_Their_Impact_on_Human_Activity"><img alt="Research paper thumbnail of And Their Impact on Human Activity" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title">And Their Impact on Human Activity</div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="23855001"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="23855001"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 23855001; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=23855001]").text(description); $(".js-view-count[data-work-id=23855001]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 23855001; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='23855001']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-23855001-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="23855000"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/23855000/The_2nd_to_4th_century_explosive_activity_of_Vesuvius_new_data_on_the_timing_of_the_upward_migration_of_the_post_AD_79_magma_chamber"><img alt="Research paper thumbnail of The 2nd to 4th century explosive activity of Vesuvius: new data on the timing of the upward migration of the post-AD 79 magma chamber" class="work-thumbnail" src="https://attachments.academia-assets.com/44249622/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/23855000/The_2nd_to_4th_century_explosive_activity_of_Vesuvius_new_data_on_the_timing_of_the_upward_migration_of_the_post_AD_79_magma_chamber">The 2nd to 4th century explosive activity of Vesuvius: new data on the timing of the upward migration of the post-AD 79 magma chamber</a></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">We present volcanological data on the deposits of the Santa Maria Member (SMM), the eruption cycl...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">We present volcanological data on the deposits of the Santa Maria Member (SMM), the eruption cycle occurred at Vesuvius (Italy) in the period between the A.D. 79 plinian and the A.D. 472 subplinan eruptions. Historical accounts report only sporadic, poorly reliable descriptions of the volcanic activity in this period, during which a stratified sequence of ash and lapilli beds, up to 150 cm thick, with a total volume estimated around 0.15 km 3 , was widely dispersed on the outer slopes of the volcano. Stratigraphic studies and component analyses suggest that activity was characterized by mixed hydromagmatic and magmatic processes. The eruption style has been interpreted as repeated alternations of continuous and prolonged ash emission activity intercalated with short-lived, violent strombolian phases. Analyses of the bulk rock composition reveal that during the entire eruption cycle, magma maintained an homogeneous phonotephritic composition. In addition, the general trends of major and trace elements depicted by the products of the A.D. 79 and A.D. 472 eruptions converge to the SMM composition, suggesting a common mafic endmember for these eruptions. The volatile content measured in pyroxene-hosted melt inclusions indicates two main values of crystallization pressures, around 220 and 70 MPa, roughly corresponding to the previously estimated depth of the magma reservoirs of the A.D. 79 and A.D. 472 eruptions, respectively. The study of SMM eruption cycle may thus contribute to understand the processes governing the volcano reawakening immediately after a plinian event, and the timing and modalities which govern the migration of the magma reservoir.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="528c6b7c10a604fdb6197f6cc2ae6be4" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":44249622,"asset_id":23855000,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/44249622/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="23855000"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="23855000"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 23855000; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=23855000]").text(description); $(".js-view-count[data-work-id=23855000]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 23855000; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='23855000']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "528c6b7c10a604fdb6197f6cc2ae6be4" } } $('.js-work-strip[data-work-id=23855000]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":23855000,"title":"The 2nd to 4th century explosive activity of Vesuvius: new data on the timing of the upward migration of the post-AD 79 magma chamber","translated_title":"","metadata":{"ai_title_tag":"Vesuvius Eruption Cycle: Magma Migration Insights","grobid_abstract":"We present volcanological data on the deposits of the Santa Maria Member (SMM), the eruption cycle occurred at Vesuvius (Italy) in the period between the A.D. 79 plinian and the A.D. 472 subplinan eruptions. Historical accounts report only sporadic, poorly reliable descriptions of the volcanic activity in this period, during which a stratified sequence of ash and lapilli beds, up to 150 cm thick, with a total volume estimated around 0.15 km 3 , was widely dispersed on the outer slopes of the volcano. Stratigraphic studies and component analyses suggest that activity was characterized by mixed hydromagmatic and magmatic processes. The eruption style has been interpreted as repeated alternations of continuous and prolonged ash emission activity intercalated with short-lived, violent strombolian phases. Analyses of the bulk rock composition reveal that during the entire eruption cycle, magma maintained an homogeneous phonotephritic composition. In addition, the general trends of major and trace elements depicted by the products of the A.D. 79 and A.D. 472 eruptions converge to the SMM composition, suggesting a common mafic endmember for these eruptions. The volatile content measured in pyroxene-hosted melt inclusions indicates two main values of crystallization pressures, around 220 and 70 MPa, roughly corresponding to the previously estimated depth of the magma reservoirs of the A.D. 79 and A.D. 472 eruptions, respectively. The study of SMM eruption cycle may thus contribute to understand the processes governing the volcano reawakening immediately after a plinian event, and the timing and modalities which govern the migration of the magma reservoir.","grobid_abstract_attachment_id":44249622},"translated_abstract":null,"internal_url":"https://www.academia.edu/23855000/The_2nd_to_4th_century_explosive_activity_of_Vesuvius_new_data_on_the_timing_of_the_upward_migration_of_the_post_AD_79_magma_chamber","translated_internal_url":"","created_at":"2016-03-31T00:55:37.861-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":14420859,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":44249622,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/44249622/thumbnails/1.jpg","file_name":"The_2nd_to_4th_century_explosive_activit20160331-24641-11cmds5.pdf","download_url":"https://www.academia.edu/attachments/44249622/download_file","bulk_download_file_name":"The_2nd_to_4th_century_explosive_activit.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/44249622/The_2nd_to_4th_century_explosive_activit20160331-24641-11cmds5-libre.pdf?1459411722=\u0026response-content-disposition=attachment%3B+filename%3DThe_2nd_to_4th_century_explosive_activit.pdf\u0026Expires=1743974706\u0026Signature=E6ZRrFYF38TFP5Uz2~SWL3iP-9q0ahfUl3dqNShqSWiFQ1iLTJAmw6BsRnYediY7N4hCkzRL5uRQ4hRhHel-4sr14bMav7P4RS5Zscz4IzA-QR0nTAPqx4~I2gHZvf9SdEn-QVO63bQcCE4l396WtfsLLgYUpRVmIyf~gZ6zbczx0Ao0wRgx0Hq-Py4erLbUc0T4HNg~5NQFvNGmypaASxf1ysaqXcihLLextjYgMjdU5sT6YbIvpGKdDJWqTiN-pbXQwB7qjPQkAB0xSoT58WTpnwJx6TG4e8PRbiMydvaI1qhgCYIHOdRMCaW-Vo1MVd3WKqEP5vOppZNju1H5UQ__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"The_2nd_to_4th_century_explosive_activity_of_Vesuvius_new_data_on_the_timing_of_the_upward_migration_of_the_post_AD_79_magma_chamber","translated_slug":"","page_count":17,"language":"en","content_type":"Work","summary":"We present volcanological data on the deposits of the Santa Maria Member (SMM), the eruption cycle occurred at Vesuvius (Italy) in the period between the A.D. 79 plinian and the A.D. 472 subplinan eruptions. Historical accounts report only sporadic, poorly reliable descriptions of the volcanic activity in this period, during which a stratified sequence of ash and lapilli beds, up to 150 cm thick, with a total volume estimated around 0.15 km 3 , was widely dispersed on the outer slopes of the volcano. Stratigraphic studies and component analyses suggest that activity was characterized by mixed hydromagmatic and magmatic processes. The eruption style has been interpreted as repeated alternations of continuous and prolonged ash emission activity intercalated with short-lived, violent strombolian phases. Analyses of the bulk rock composition reveal that during the entire eruption cycle, magma maintained an homogeneous phonotephritic composition. In addition, the general trends of major and trace elements depicted by the products of the A.D. 79 and A.D. 472 eruptions converge to the SMM composition, suggesting a common mafic endmember for these eruptions. The volatile content measured in pyroxene-hosted melt inclusions indicates two main values of crystallization pressures, around 220 and 70 MPa, roughly corresponding to the previously estimated depth of the magma reservoirs of the A.D. 79 and A.D. 472 eruptions, respectively. The study of SMM eruption cycle may thus contribute to understand the processes governing the volcano reawakening immediately after a plinian event, and the timing and modalities which govern the migration of the magma reservoir.","impression_tracking_id":null,"owner":{"id":14420859,"first_name":"Claudia","middle_initials":null,"last_name":"D'Oriano","page_name":"CDOriano","domain_name":"ingv","created_at":"2014-07-27T18:56:54.386-07:00","display_name":"Claudia D'Oriano","url":"https://ingv.academia.edu/CDOriano"},"attachments":[{"id":44249622,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/44249622/thumbnails/1.jpg","file_name":"The_2nd_to_4th_century_explosive_activit20160331-24641-11cmds5.pdf","download_url":"https://www.academia.edu/attachments/44249622/download_file","bulk_download_file_name":"The_2nd_to_4th_century_explosive_activit.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/44249622/The_2nd_to_4th_century_explosive_activit20160331-24641-11cmds5-libre.pdf?1459411722=\u0026response-content-disposition=attachment%3B+filename%3DThe_2nd_to_4th_century_explosive_activit.pdf\u0026Expires=1743974706\u0026Signature=E6ZRrFYF38TFP5Uz2~SWL3iP-9q0ahfUl3dqNShqSWiFQ1iLTJAmw6BsRnYediY7N4hCkzRL5uRQ4hRhHel-4sr14bMav7P4RS5Zscz4IzA-QR0nTAPqx4~I2gHZvf9SdEn-QVO63bQcCE4l396WtfsLLgYUpRVmIyf~gZ6zbczx0Ao0wRgx0Hq-Py4erLbUc0T4HNg~5NQFvNGmypaASxf1ysaqXcihLLextjYgMjdU5sT6YbIvpGKdDJWqTiN-pbXQwB7qjPQkAB0xSoT58WTpnwJx6TG4e8PRbiMydvaI1qhgCYIHOdRMCaW-Vo1MVd3WKqEP5vOppZNju1H5UQ__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":409,"name":"Geophysics","url":"https://www.academia.edu/Documents/in/Geophysics"},{"id":1034,"name":"Stratigraphy","url":"https://www.academia.edu/Documents/in/Stratigraphy"},{"id":78128,"name":"Vesuvius","url":"https://www.academia.edu/Documents/in/Vesuvius"},{"id":200887,"name":"Explosive volcanic eruptions","url":"https://www.academia.edu/Documents/in/Explosive_volcanic_eruptions"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-23855000-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="23854999"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/23854999/The_onset_of_an_eruption_selective_assimilation_of_hydrothermal_minerals_during_the_opening_phase_of_the_2010_summit_eruption_of_Eyjafjallaj%C3%B6kull_volcano_Iceland"><img alt="Research paper thumbnail of The onset of an eruption: selective assimilation of hydrothermal minerals during the opening phase of the 2010 summit eruption of Eyjafjallajökull volcano, Iceland" class="work-thumbnail" src="https://attachments.academia-assets.com/44249621/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/23854999/The_onset_of_an_eruption_selective_assimilation_of_hydrothermal_minerals_during_the_opening_phase_of_the_2010_summit_eruption_of_Eyjafjallaj%C3%B6kull_volcano_Iceland">The onset of an eruption: selective assimilation of hydrothermal minerals during the opening phase of the 2010 summit eruption of Eyjafjallajökull volcano, Iceland</a></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">The 2010 summit eruption of Eyjafjallajökull volcano (Iceland) started on 14 April and continued ...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">The 2010 summit eruption of Eyjafjallajökull volcano (Iceland) started on 14 April and continued for 39 days. The whole duration of the activity can be divided into different phases, characterized by variable intensity and eruption dynamics. The opening stage of the eruption, in particular, lasted few hours, during which the magma intruded into the glacier, melting the ice to the surface. In this subglacial stage the activity was dominated by the emission of ash-poor, vapour-rich clouds, with the sedimentation of a very thin ash layer in the very proximal area. The intensity of the summit eruption gradually increased during the day, and culminated with the emergence of a 9-10 km high, dark ash-laden plume, which continued, with variable intensity, until 18 April. We focus here on the opening stage of the event (first 3-4 hours), which represents a unique opportunity to investigate the immediately pre-eruptive dynamics .</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="6c28c15cc7e42209a4de1cded46334e8" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":44249621,"asset_id":23854999,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/44249621/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="23854999"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="23854999"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 23854999; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=23854999]").text(description); $(".js-view-count[data-work-id=23854999]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 23854999; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='23854999']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "6c28c15cc7e42209a4de1cded46334e8" } } $('.js-work-strip[data-work-id=23854999]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":23854999,"title":"The onset of an eruption: selective assimilation of hydrothermal minerals during the opening phase of the 2010 summit eruption of Eyjafjallajökull volcano, Iceland","translated_title":"","metadata":{"grobid_abstract":"The 2010 summit eruption of Eyjafjallajökull volcano (Iceland) started on 14 April and continued for 39 days. The whole duration of the activity can be divided into different phases, characterized by variable intensity and eruption dynamics. The opening stage of the eruption, in particular, lasted few hours, during which the magma intruded into the glacier, melting the ice to the surface. In this subglacial stage the activity was dominated by the emission of ash-poor, vapour-rich clouds, with the sedimentation of a very thin ash layer in the very proximal area. The intensity of the summit eruption gradually increased during the day, and culminated with the emergence of a 9-10 km high, dark ash-laden plume, which continued, with variable intensity, until 18 April. We focus here on the opening stage of the event (first 3-4 hours), which represents a unique opportunity to investigate the immediately pre-eruptive dynamics .","grobid_abstract_attachment_id":44249621},"translated_abstract":null,"internal_url":"https://www.academia.edu/23854999/The_onset_of_an_eruption_selective_assimilation_of_hydrothermal_minerals_during_the_opening_phase_of_the_2010_summit_eruption_of_Eyjafjallaj%C3%B6kull_volcano_Iceland","translated_internal_url":"","created_at":"2016-03-31T00:55:37.660-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":14420859,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":44249621,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/44249621/thumbnails/1.jpg","file_name":"The_onset_of_an_eruption_selective_assim20160331-30246-mm74ls.pdf","download_url":"https://www.academia.edu/attachments/44249621/download_file","bulk_download_file_name":"The_onset_of_an_eruption_selective_assim.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/44249621/The_onset_of_an_eruption_selective_assim20160331-30246-mm74ls-libre.pdf?1459411720=\u0026response-content-disposition=attachment%3B+filename%3DThe_onset_of_an_eruption_selective_assim.pdf\u0026Expires=1743974706\u0026Signature=ULYlmps6JyxGmd~EU~J0GvSFqtogWfThQ49PclpJGtgNG74TwKzh~Xq72rsM4hMpl3KEzu-pQzLqNGru3swtlj6NR8XaBeHS7y3E41mq9ahk1bTs8lWPoae4mn6KLV7jmWYbqFzAI68qzIri52sYE2zTmXSsiGWVbWHLw~uLzXobtIXWhr8Gnj3sVO7NsJFhQeMc4JSD9weARadHUrv6IG3U8kEthQyJ30mYR28bruj7DFLFojIhaiqCTV93zIPhbg7nc5itYJVdvCFydnTDH7EUwBoV6eSDGbsgxEZLeHi4LHUbFcrkpcCKqKAjCgb4ZKRJCHp0vPz75WzhDPTUxw__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"The_onset_of_an_eruption_selective_assimilation_of_hydrothermal_minerals_during_the_opening_phase_of_the_2010_summit_eruption_of_Eyjafjallajökull_volcano_Iceland","translated_slug":"","page_count":2,"language":"en","content_type":"Work","summary":"The 2010 summit eruption of Eyjafjallajökull volcano (Iceland) started on 14 April and continued for 39 days. The whole duration of the activity can be divided into different phases, characterized by variable intensity and eruption dynamics. The opening stage of the eruption, in particular, lasted few hours, during which the magma intruded into the glacier, melting the ice to the surface. In this subglacial stage the activity was dominated by the emission of ash-poor, vapour-rich clouds, with the sedimentation of a very thin ash layer in the very proximal area. The intensity of the summit eruption gradually increased during the day, and culminated with the emergence of a 9-10 km high, dark ash-laden plume, which continued, with variable intensity, until 18 April. We focus here on the opening stage of the event (first 3-4 hours), which represents a unique opportunity to investigate the immediately pre-eruptive dynamics .","impression_tracking_id":null,"owner":{"id":14420859,"first_name":"Claudia","middle_initials":null,"last_name":"D'Oriano","page_name":"CDOriano","domain_name":"ingv","created_at":"2014-07-27T18:56:54.386-07:00","display_name":"Claudia D'Oriano","url":"https://ingv.academia.edu/CDOriano"},"attachments":[{"id":44249621,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/44249621/thumbnails/1.jpg","file_name":"The_onset_of_an_eruption_selective_assim20160331-30246-mm74ls.pdf","download_url":"https://www.academia.edu/attachments/44249621/download_file","bulk_download_file_name":"The_onset_of_an_eruption_selective_assim.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/44249621/The_onset_of_an_eruption_selective_assim20160331-30246-mm74ls-libre.pdf?1459411720=\u0026response-content-disposition=attachment%3B+filename%3DThe_onset_of_an_eruption_selective_assim.pdf\u0026Expires=1743974706\u0026Signature=ULYlmps6JyxGmd~EU~J0GvSFqtogWfThQ49PclpJGtgNG74TwKzh~Xq72rsM4hMpl3KEzu-pQzLqNGru3swtlj6NR8XaBeHS7y3E41mq9ahk1bTs8lWPoae4mn6KLV7jmWYbqFzAI68qzIri52sYE2zTmXSsiGWVbWHLw~uLzXobtIXWhr8Gnj3sVO7NsJFhQeMc4JSD9weARadHUrv6IG3U8kEthQyJ30mYR28bruj7DFLFojIhaiqCTV93zIPhbg7nc5itYJVdvCFydnTDH7EUwBoV6eSDGbsgxEZLeHi4LHUbFcrkpcCKqKAjCgb4ZKRJCHp0vPz75WzhDPTUxw__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-23854999-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="23854998"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/23854998/Past_and_present_mid_intensity_explosive_eruptions_of_Italian_volcanoes_and_their_impact_on_human_activity"><img alt="Research paper thumbnail of Past and present mid-intensity explosive eruptions of Italian volcanoes and their impact on human activity" class="work-thumbnail" src="https://attachments.academia-assets.com/44249624/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/23854998/Past_and_present_mid_intensity_explosive_eruptions_of_Italian_volcanoes_and_their_impact_on_human_activity">Past and present mid-intensity explosive eruptions of Italian volcanoes and their impact on human activity</a></div><div class="wp-workCard_item"><span>Journal of the Virtual Explorer</span><span>, 2010</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Active Italian volcanoes are characterized by a large variability of eruptive mechanisms, from qu...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Active Italian volcanoes are characterized by a large variability of eruptive mechanisms, from quiet lava effusions to catastrophic ignimbritic eruptions. The impact of volcanic activity, and in particular of explosive activity, is clearly related to the intensity and magnitude of the eruptions, varying from an incidental interference with everyday life up to devastating consequences on civilizations. While the largest events have usually monopolized the interest of volcanologists and historians, the modalities and impact of mid intensity eruptions have not been investigated in so much detail. In addition, the frequency of occurrence of mid intensity eruptions is by far higher than that of the largest events, so making their study of primary importance for the assessment of the impact of volcanic activity on environment and human life.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="00d337b09ce3da5acda8e6904c7536e1" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":44249624,"asset_id":23854998,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/44249624/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="23854998"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="23854998"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 23854998; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=23854998]").text(description); $(".js-view-count[data-work-id=23854998]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 23854998; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='23854998']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "00d337b09ce3da5acda8e6904c7536e1" } } $('.js-work-strip[data-work-id=23854998]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":23854998,"title":"Past and present mid-intensity explosive eruptions of Italian volcanoes and their impact on human activity","translated_title":"","metadata":{"ai_title_tag":"Mid-Intensity Explosive Eruptions in Italy","grobid_abstract":"Active Italian volcanoes are characterized by a large variability of eruptive mechanisms, from quiet lava effusions to catastrophic ignimbritic eruptions. The impact of volcanic activity, and in particular of explosive activity, is clearly related to the intensity and magnitude of the eruptions, varying from an incidental interference with everyday life up to devastating consequences on civilizations. While the largest events have usually monopolized the interest of volcanologists and historians, the modalities and impact of mid intensity eruptions have not been investigated in so much detail. In addition, the frequency of occurrence of mid intensity eruptions is by far higher than that of the largest events, so making their study of primary importance for the assessment of the impact of volcanic activity on environment and human life.","publication_date":{"day":null,"month":null,"year":2010,"errors":{}},"publication_name":"Journal of the Virtual Explorer","grobid_abstract_attachment_id":44249624},"translated_abstract":null,"internal_url":"https://www.academia.edu/23854998/Past_and_present_mid_intensity_explosive_eruptions_of_Italian_volcanoes_and_their_impact_on_human_activity","translated_internal_url":"","created_at":"2016-03-31T00:55:37.476-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":14420859,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":44249624,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/44249624/thumbnails/1.jpg","file_name":"Past_and_present_mid-intensity_explosive20160331-25224-jnn1st.pdf","download_url":"https://www.academia.edu/attachments/44249624/download_file","bulk_download_file_name":"Past_and_present_mid_intensity_explosive.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/44249624/Past_and_present_mid-intensity_explosive20160331-25224-jnn1st-libre.pdf?1459411724=\u0026response-content-disposition=attachment%3B+filename%3DPast_and_present_mid_intensity_explosive.pdf\u0026Expires=1743974706\u0026Signature=OTtAtd7HqdhowdlXmh6FL6fuJephMHk16QtXzUIY3NfHauQ0rDeoznm2b1grBPdYX5wD0IZqgvqG~2VirTiaIT6VbWa~52SBhS9p40PDEgNJydI6pzfSFZYSoOMxKu7jke6dKC9VClINlJXDr95-j55ElHPxBov~q1JA0oWPXPZFaZ782g-1q5W7viENYm-9j0HlS23ryu~6dZOd2jzLGjFNli-HB8X33njIzuEZINmmtVATygqlXgZcqQ8H7LyaLltlmX19TL2l~WBI80FLPiWFrA-hDPCJ7FM-sI8SBesD2fy9nacfFQt4Zy9ycceRDIFFB1TlNGd3iPpmJ~5s3w__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Past_and_present_mid_intensity_explosive_eruptions_of_Italian_volcanoes_and_their_impact_on_human_activity","translated_slug":"","page_count":32,"language":"en","content_type":"Work","summary":"Active Italian volcanoes are characterized by a large variability of eruptive mechanisms, from quiet lava effusions to catastrophic ignimbritic eruptions. The impact of volcanic activity, and in particular of explosive activity, is clearly related to the intensity and magnitude of the eruptions, varying from an incidental interference with everyday life up to devastating consequences on civilizations. While the largest events have usually monopolized the interest of volcanologists and historians, the modalities and impact of mid intensity eruptions have not been investigated in so much detail. 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Pumice sample PST-9 comes from a fallout deposit older than a spatter agglutinate sequence emplaced during the twentieth century. The eruption that produced it had a size exceeding that of intermediate paroxysms but was smaller than large-scale, spatter-forming, paroxysms from the sixteenth century and 1930 A.D. Lapilli are strongly vesicular and crystal-poor, similar to other ''golden'' pumices. Modal proportions include 89 vol% glass, 8 vol% clinopyroxene, 1-2 vol% olivine and 1-2 vol% plagioclase. Plagioclase is represented by reacted crystals coming from the shallow resident magma and incorporated in the pumice during eruption. A total of 74 and 44 crystals of olivine and clinopyroxene, respectively, were examined and 187 and 99 electron microprobe analyses obtained. Fo in olivine ranges between 70 and 92 mol% and Fs in clinopyroxene between 3 and 13 mol%. PST-9 hosts a higher proportion of Fo-rich olivine and Fs-poor clinopyroxene than the other ''golden'' pumices. Groundmass glasses are basaltic (Mg# ¼ 66-69), as are most rim glasses around olivine and clinopyroxene, and glass inclusions in clinopyroxene. They are more primitive than in the other ''golden'' pumices. A few rim glasses and glass inclusions are shoshonitic (Mg# ¼ 45-50). Most glass inclusions in olivine have CaO/Al 2 O 3 higher than the other glasses and the whole-rock. PST-9 has the highest bulk MgO, CaO, Mg# and CaO/Al 2 O 3 and the lowest FeO t of all ''golden'' pumices analysed to date. Analysis of Fe-Mg partitioning between olivine, clinopyroxene and melt allows three crystallization stages to be recognized. The first involves primitive mantle-derived melts (Mg# ¼ 74-80), the second basaltic melts represented by groundmass glasses and the third is associated with more evolved melts represented by the shoshonitic glasses. The population of crystals in ''golden'' pumices is heterogeneous not only because of crystal incorporation from the shallow resident magma, but also because of pre-eruptive recharge of the deep reservoir with primitive melts. Differences between PST-9 and the other ''golden'' pumices in terms of groundmass glass composition and distribution of olivine and clinopyroxene compositions reflect contrasted replenishment rates of the deep reservoir with primitive liquids. Gabbroic inclusions in a clinopyroxene crystal provide a direct illustration of melt wall-rock interaction and stress the variability of the deep reservoir in terms of temperature, crystallinity and phase assemblages. Deep crystallization of plagioclase should be considered as a possibility at Stromboli. PST-9 is exceptionally well representative of the early magmatic evolution of ''golden'' pumices.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="a8c81650036010407acd5d2bb0b99430" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":44249625,"asset_id":23854997,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/44249625/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="23854997"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="23854997"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 23854997; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=23854997]").text(description); $(".js-view-count[data-work-id=23854997]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 23854997; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='23854997']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "a8c81650036010407acd5d2bb0b99430" } } $('.js-work-strip[data-work-id=23854997]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":23854997,"title":"Petrography, mineralogy and geochemistry of a primitive pumice from Stromboli: implications for the deep feeding system","translated_title":"","metadata":{"grobid_abstract":"We describe the field relations, petrographic, mineralogical and geochemical characteristics of an exceptional ''golden'' pumice belonging to a tephra layer exposed on the summit area of Stromboli volcano, Italy. Pumice sample PST-9 comes from a fallout deposit older than a spatter agglutinate sequence emplaced during the twentieth century. The eruption that produced it had a size exceeding that of intermediate paroxysms but was smaller than large-scale, spatter-forming, paroxysms from the sixteenth century and 1930 A.D. Lapilli are strongly vesicular and crystal-poor, similar to other ''golden'' pumices. Modal proportions include 89 vol% glass, 8 vol% clinopyroxene, 1-2 vol% olivine and 1-2 vol% plagioclase. Plagioclase is represented by reacted crystals coming from the shallow resident magma and incorporated in the pumice during eruption. A total of 74 and 44 crystals of olivine and clinopyroxene, respectively, were examined and 187 and 99 electron microprobe analyses obtained. Fo in olivine ranges between 70 and 92 mol% and Fs in clinopyroxene between 3 and 13 mol%. PST-9 hosts a higher proportion of Fo-rich olivine and Fs-poor clinopyroxene than the other ''golden'' pumices. Groundmass glasses are basaltic (Mg# ¼ 66-69), as are most rim glasses around olivine and clinopyroxene, and glass inclusions in clinopyroxene. They are more primitive than in the other ''golden'' pumices. A few rim glasses and glass inclusions are shoshonitic (Mg# ¼ 45-50). Most glass inclusions in olivine have CaO/Al 2 O 3 higher than the other glasses and the whole-rock. PST-9 has the highest bulk MgO, CaO, Mg# and CaO/Al 2 O 3 and the lowest FeO t of all ''golden'' pumices analysed to date. Analysis of Fe-Mg partitioning between olivine, clinopyroxene and melt allows three crystallization stages to be recognized. The first involves primitive mantle-derived melts (Mg# ¼ 74-80), the second basaltic melts represented by groundmass glasses and the third is associated with more evolved melts represented by the shoshonitic glasses. The population of crystals in ''golden'' pumices is heterogeneous not only because of crystal incorporation from the shallow resident magma, but also because of pre-eruptive recharge of the deep reservoir with primitive melts. Differences between PST-9 and the other ''golden'' pumices in terms of groundmass glass composition and distribution of olivine and clinopyroxene compositions reflect contrasted replenishment rates of the deep reservoir with primitive liquids. Gabbroic inclusions in a clinopyroxene crystal provide a direct illustration of melt wall-rock interaction and stress the variability of the deep reservoir in terms of temperature, crystallinity and phase assemblages. Deep crystallization of plagioclase should be considered as a possibility at Stromboli. PST-9 is exceptionally well representative of the early magmatic evolution of ''golden'' pumices.","publication_date":{"day":null,"month":null,"year":2011,"errors":{}},"publication_name":"European Journal of Mineralogy","grobid_abstract_attachment_id":44249625},"translated_abstract":null,"internal_url":"https://www.academia.edu/23854997/Petrography_mineralogy_and_geochemistry_of_a_primitive_pumice_from_Stromboli_implications_for_the_deep_feeding_system","translated_internal_url":"","created_at":"2016-03-31T00:55:37.292-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":14420859,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":44249625,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/44249625/thumbnails/1.jpg","file_name":"Petrography_mineralogy_and_geochemistry_20160331-9958-22xsi7.pdf","download_url":"https://www.academia.edu/attachments/44249625/download_file","bulk_download_file_name":"Petrography_mineralogy_and_geochemistry.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/44249625/Petrography_mineralogy_and_geochemistry_20160331-9958-22xsi7-libre.pdf?1459411723=\u0026response-content-disposition=attachment%3B+filename%3DPetrography_mineralogy_and_geochemistry.pdf\u0026Expires=1743974706\u0026Signature=BwvHk472pRz7GP8XzxUvYxlxehRUo91cipfK7B~huXE0pG9D22MpX0i33FokdEaFGC-qII9QCPMa65b55GnjBnSjyDBYQuBibNQBdHApbSuNp7Eq7U1QDl-OXjY6ZQjkJ2uC7wZB1pPSxSKM1V6XjrRbO-kEVinQSQhmlOdG1hjiBl~oXPopcf1WEe11hZlTP4scK3nUcDN2n1RyKCmFqg~F1ACPObYfZfjK2ee8sdNqPfPqqvBJXgNZ9Acgx9GuBLfAvKrV5~PA9VNuua32NdowkwI~LYafi0iIUouSyJh7p8BI5I7trp8PGd0vV9w~Gl5LqYCsUF-Flao~lzVj0A__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Petrography_mineralogy_and_geochemistry_of_a_primitive_pumice_from_Stromboli_implications_for_the_deep_feeding_system","translated_slug":"","page_count":19,"language":"en","content_type":"Work","summary":"We describe the field relations, petrographic, mineralogical and geochemical characteristics of an exceptional ''golden'' pumice belonging to a tephra layer exposed on the summit area of Stromboli volcano, Italy. 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Groundmass glasses are basaltic (Mg# ¼ 66-69), as are most rim glasses around olivine and clinopyroxene, and glass inclusions in clinopyroxene. They are more primitive than in the other ''golden'' pumices. A few rim glasses and glass inclusions are shoshonitic (Mg# ¼ 45-50). Most glass inclusions in olivine have CaO/Al 2 O 3 higher than the other glasses and the whole-rock. PST-9 has the highest bulk MgO, CaO, Mg# and CaO/Al 2 O 3 and the lowest FeO t of all ''golden'' pumices analysed to date. Analysis of Fe-Mg partitioning between olivine, clinopyroxene and melt allows three crystallization stages to be recognized. The first involves primitive mantle-derived melts (Mg# ¼ 74-80), the second basaltic melts represented by groundmass glasses and the third is associated with more evolved melts represented by the shoshonitic glasses. The population of crystals in ''golden'' pumices is heterogeneous not only because of crystal incorporation from the shallow resident magma, but also because of pre-eruptive recharge of the deep reservoir with primitive melts. Differences between PST-9 and the other ''golden'' pumices in terms of groundmass glass composition and distribution of olivine and clinopyroxene compositions reflect contrasted replenishment rates of the deep reservoir with primitive liquids. Gabbroic inclusions in a clinopyroxene crystal provide a direct illustration of melt wall-rock interaction and stress the variability of the deep reservoir in terms of temperature, crystallinity and phase assemblages. Deep crystallization of plagioclase should be considered as a possibility at Stromboli. PST-9 is exceptionally well representative of the early magmatic evolution of ''golden'' pumices.","impression_tracking_id":null,"owner":{"id":14420859,"first_name":"Claudia","middle_initials":null,"last_name":"D'Oriano","page_name":"CDOriano","domain_name":"ingv","created_at":"2014-07-27T18:56:54.386-07:00","display_name":"Claudia D'Oriano","url":"https://ingv.academia.edu/CDOriano"},"attachments":[{"id":44249625,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/44249625/thumbnails/1.jpg","file_name":"Petrography_mineralogy_and_geochemistry_20160331-9958-22xsi7.pdf","download_url":"https://www.academia.edu/attachments/44249625/download_file","bulk_download_file_name":"Petrography_mineralogy_and_geochemistry.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/44249625/Petrography_mineralogy_and_geochemistry_20160331-9958-22xsi7-libre.pdf?1459411723=\u0026response-content-disposition=attachment%3B+filename%3DPetrography_mineralogy_and_geochemistry.pdf\u0026Expires=1743974706\u0026Signature=BwvHk472pRz7GP8XzxUvYxlxehRUo91cipfK7B~huXE0pG9D22MpX0i33FokdEaFGC-qII9QCPMa65b55GnjBnSjyDBYQuBibNQBdHApbSuNp7Eq7U1QDl-OXjY6ZQjkJ2uC7wZB1pPSxSKM1V6XjrRbO-kEVinQSQhmlOdG1hjiBl~oXPopcf1WEe11hZlTP4scK3nUcDN2n1RyKCmFqg~F1ACPObYfZfjK2ee8sdNqPfPqqvBJXgNZ9Acgx9GuBLfAvKrV5~PA9VNuua32NdowkwI~LYafi0iIUouSyJh7p8BI5I7trp8PGd0vV9w~Gl5LqYCsUF-Flao~lzVj0A__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry"},{"id":279027,"name":"European","url":"https://www.academia.edu/Documents/in/European"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-23854997-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="23854996"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/23854996/Changes_in_eruptive_style_during_the_A_D_1538_Monte_Nuovo_eruption_Phlegrean_Fields_Italy_the_role_of_syn_eruptive_crystallization"><img alt="Research paper thumbnail of Changes in eruptive style during the A.D. 1538 Monte Nuovo eruption (Phlegrean Fields, Italy): the role of syn-eruptive crystallization" class="work-thumbnail" src="https://attachments.academia-assets.com/44249623/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/23854996/Changes_in_eruptive_style_during_the_A_D_1538_Monte_Nuovo_eruption_Phlegrean_Fields_Italy_the_role_of_syn_eruptive_crystallization">Changes in eruptive style during the A.D. 1538 Monte Nuovo eruption (Phlegrean Fields, Italy): the role of syn-eruptive crystallization</a></div><div class="wp-workCard_item"><span>Bulletin of Volcanology</span><span>, 2005</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="01c71c36e36fbe60ef85e4c81fb6ddce" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":44249623,"asset_id":23854996,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/44249623/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="23854996"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="23854996"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 23854996; 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This research examines the characteristics of the eruptive products, highlighting differences in texture and composition related to crystallization processes occurring during the eruption. Results indicate that syn-eruptive degassing and crystallization played crucial roles in transitioning from one eruptive style to another, underscoring the influence of magma properties on volcanic dynamics.","ai_title_tag":"Eruptive Style Changes in 1538 Monte Nuovo","publication_date":{"day":null,"month":null,"year":2005,"errors":{}},"publication_name":"Bulletin of Volcanology"},"translated_abstract":null,"internal_url":"https://www.academia.edu/23854996/Changes_in_eruptive_style_during_the_A_D_1538_Monte_Nuovo_eruption_Phlegrean_Fields_Italy_the_role_of_syn_eruptive_crystallization","translated_internal_url":"","created_at":"2016-03-31T00:55:37.095-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":14420859,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":44249623,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/44249623/thumbnails/1.jpg","file_name":"Changes_in_eruptive_style_during_the_A.D20160331-730-1nlvvhu.pdf","download_url":"https://www.academia.edu/attachments/44249623/download_file","bulk_download_file_name":"Changes_in_eruptive_style_during_the_A_D.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/44249623/Changes_in_eruptive_style_during_the_A.D20160331-730-1nlvvhu-libre.pdf?1459411721=\u0026response-content-disposition=attachment%3B+filename%3DChanges_in_eruptive_style_during_the_A_D.pdf\u0026Expires=1743974706\u0026Signature=aBwlamsY4AcH4AJtHyUBIbMVhohYSr1vhfyu92NUl2OBi~MEW09x4JiJibJxh7YHrGS~hZ3~IkftQ8O8cz4Du2PJfMtqQ9QWWftj1x8XnB2g5-HG6q7ReiJyCcEo7yJ3G4DlyHuITTFDlwtk3BrRoucQ-ge2KOAR8emDzEzUNqsXBEF2uUAVvHDTP2CP5YESCG8BGwoGtPoXIvQqgE6-V-E36q7Fh6K54ieRi9UexcsvI4KNBhRMhVnkVZb6lb1C-nrPuUS7zCD51rmSDhgtwp0h2pSGncB3hdMjZYbAWMu4tKmDL1Dg1Q8R6h374SIHoeKwbgd4OFvpaOFxJOgymg__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Changes_in_eruptive_style_during_the_A_D_1538_Monte_Nuovo_eruption_Phlegrean_Fields_Italy_the_role_of_syn_eruptive_crystallization","translated_slug":"","page_count":21,"language":"en","content_type":"Work","summary":null,"impression_tracking_id":null,"owner":{"id":14420859,"first_name":"Claudia","middle_initials":null,"last_name":"D'Oriano","page_name":"CDOriano","domain_name":"ingv","created_at":"2014-07-27T18:56:54.386-07:00","display_name":"Claudia D'Oriano","url":"https://ingv.academia.edu/CDOriano"},"attachments":[{"id":44249623,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/44249623/thumbnails/1.jpg","file_name":"Changes_in_eruptive_style_during_the_A.D20160331-730-1nlvvhu.pdf","download_url":"https://www.academia.edu/attachments/44249623/download_file","bulk_download_file_name":"Changes_in_eruptive_style_during_the_A_D.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/44249623/Changes_in_eruptive_style_during_the_A.D20160331-730-1nlvvhu-libre.pdf?1459411721=\u0026response-content-disposition=attachment%3B+filename%3DChanges_in_eruptive_style_during_the_A_D.pdf\u0026Expires=1743974706\u0026Signature=aBwlamsY4AcH4AJtHyUBIbMVhohYSr1vhfyu92NUl2OBi~MEW09x4JiJibJxh7YHrGS~hZ3~IkftQ8O8cz4Du2PJfMtqQ9QWWftj1x8XnB2g5-HG6q7ReiJyCcEo7yJ3G4DlyHuITTFDlwtk3BrRoucQ-ge2KOAR8emDzEzUNqsXBEF2uUAVvHDTP2CP5YESCG8BGwoGtPoXIvQqgE6-V-E36q7Fh6K54ieRi9UexcsvI4KNBhRMhVnkVZb6lb1C-nrPuUS7zCD51rmSDhgtwp0h2pSGncB3hdMjZYbAWMu4tKmDL1Dg1Q8R6h374SIHoeKwbgd4OFvpaOFxJOgymg__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":322085,"name":"Pyroclastic Flow","url":"https://www.academia.edu/Documents/in/Pyroclastic_Flow"},{"id":709300,"name":"Trace element","url":"https://www.academia.edu/Documents/in/Trace_element"},{"id":1228946,"name":"Physical Properties","url":"https://www.academia.edu/Documents/in/Physical_Properties"},{"id":1474826,"name":"Crystal Size Distribution","url":"https://www.academia.edu/Documents/in/Crystal_Size_Distribution"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-23854996-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="23854995"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/23854995/Eruptive_scenario_of_ash_dominated_events_at_Vesuvius_the_AP3_eruption_2_710_60_years_BP_"><img alt="Research paper thumbnail of Eruptive scenario of ash-dominated events at Vesuvius: the AP3 eruption (2,710±60 years BP)" class="work-thumbnail" src="https://attachments.academia-assets.com/44249620/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/23854995/Eruptive_scenario_of_ash_dominated_events_at_Vesuvius_the_AP3_eruption_2_710_60_years_BP_">Eruptive scenario of ash-dominated events at Vesuvius: the AP3 eruption (2,710±60 years BP)</a></div><div class="wp-workCard_item"><div class="carousel-container carousel-container--sm" id="profile-work-23854995-figures"><div class="prev-slide-container js-prev-button-container"><button aria-label="Previous" class="carousel-navigation-button js-profile-work-23854995-figures-prev"><span class="material-symbols-outlined" style="font-size: 24px" translate="no">arrow_back_ios</span></button></div><div class="slides-container js-slides-container"><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/21944412/figure-1-eruptive-scenario-of-ash-dominated-events-at"><img alt="" class="figure-slide-image" src="https://figures.academia-assets.com/44249620/figure_001.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/21944413/figure-2-eruptive-scenario-of-ash-dominated-events-at"><img alt="" class="figure-slide-image" src="https://figures.academia-assets.com/44249620/figure_002.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/21944414/figure-3-fic-images-of-ap-ash-fragments-selected-in-the-size"><img alt="Fic. 2. Images of AP3 ash fragments selected in the size range of 1-0.5 mm a) glassy, poorly vesicular; b) coalescent vesicles in a mod- erately vesicular crystal-rich fragments (red arrows follow the coalescence paths); c) pumice-like portion of magma including carry- ing a dense, microlite-rich enclave. " class="figure-slide-image" src="https://figures.academia-assets.com/44249620/figure_003.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/21944415/figure-4-fic-frequency-histogram-of-the-measured-shape"><img alt="Fic. 3. Frequency histogram of the measured shape parameters on ash samples collected along the stratigraphic succession. On the vertical axis data correspond to the % of the total number of clasts analysed for each sample. " class="figure-slide-image" src="https://figures.academia-assets.com/44249620/figure_004.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/21944417/figure-5-fic-different-types-of-outlines-discriminated-on"><img alt="Fic. 4. Different types of outlines discriminated on the base of the cluster tree analyses for the samples from the S1 (proximal) section. Hs = high spherical; sk = sub rounded; Ls = low spher- ical; va = very angular. Number indicate the % abundance of each type respect to the total of investigated clasts for each sample. " class="figure-slide-image" src="https://figures.academia-assets.com/44249620/figure_005.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/21944419/figure-4-fic-different-types-of-outlines-discriminated-on"><img alt="Fic. 5. Different types of outlines discriminated on the base of the cluster tree analyses for the samples from the S2 (distal) sec- tion. Numbers as in Figure 4. " class="figure-slide-image" src="https://figures.academia-assets.com/44249620/figure_006.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/21944421/figure-7-eruptive-scenario-of-ash-dominated-events-at"><img alt="" class="figure-slide-image" src="https://figures.academia-assets.com/44249620/figure_007.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/21944424/figure-8-fic-abundance-of-the-total-of-the-four-different"><img alt="Fic. 7. Abundance (% of the total) of the four different types of fragments in the analysed samples. " class="figure-slide-image" src="https://figures.academia-assets.com/44249620/figure_008.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/21944426/figure-9-eruptive-scenario-of-ash-dominated-events-at"><img alt="" class="figure-slide-image" src="https://figures.academia-assets.com/44249620/figure_009.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/21944427/figure-10-fic-curves-of-crystal-size-distribution-for"><img alt="Fic. 9. Curves of Crystal Size Distribution for plagioclase mi- crolites in the analysed samples. " class="figure-slide-image" src="https://figures.academia-assets.com/44249620/figure_010.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/21944428/table-1-mean-values-and-standard-deviation-in-bracket-of-the"><img alt="TABLE 1. Mean values and standard deviation (in bracket) of the measured shape parameters for each investigated layer. " class="figure-slide-image" src="https://figures.academia-assets.com/44249620/table_001.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/21944429/table-2-results-of-the-principal-component-analyses"><img alt="TaBLE 2. Results of the principal component analyses. " class="figure-slide-image" src="https://figures.academia-assets.com/44249620/table_002.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/21944430/table-4-averaged-glass-composition-number-of-analysis"><img alt="TaBLeE 3. Averaged glass composition. n = number of analysis; o = standard deviation. Five clasts were selected from each investigated sample, in order to obtain quantitative information on ground- mass texture. We consider only the mve fragments with similar vesicularity index (40-54 vol.%), which represent the most abundant type in all the investigated samples, except for the VSM54. Plagioclase is the unique miner- alogical phase considered for this textural study. Table 4 summarizes the main 2 D and 3D textural data. Leucite, the other abundant microlite phase, was not considered Analyses of the glass composition were performed on ash fragments selected from the mvc, mvc and pve types, while pcr fragments were difficult to analyse for the very low amount of glass between crystals. Clast- " class="figure-slide-image" src="https://figures.academia-assets.com/44249620/table_003.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/21944431/table-4-plagioclase-parameters-derived-from-the-crystals"><img alt="TaBLe 4. Plagioclase parameters derived from the crystals size distributions analyses. ® = fraction of microlites (vol.%), G = Average growth rate (mm/sec); tT = time for crystals growth (sec); 3G t = crystals average dominant size (Cashman 1992); Na = number of microlites per unit area (mm-2); n° = nuclei number density (mm-4). " class="figure-slide-image" src="https://figures.academia-assets.com/44249620/table_004.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/21944432/table-5-proposed-eruption-scenario-for-ash-dominated"><img alt="TaBLE 5. Proposed eruption scenario for ash-dominated eruptions at Vesuvius. Eruptive scenario of ash-dominated events at Vesuvius: the AP3 eruption (2,710 + 60 years BP) " class="figure-slide-image" src="https://figures.academia-assets.com/44249620/table_005.jpg" /></a></figure></div><div class="next-slide-container js-next-button-container"><button aria-label="Next" class="carousel-navigation-button js-profile-work-23854995-figures-next"><span class="material-symbols-outlined" style="font-size: 24px" translate="no">arrow_forward_ios</span></button></div></div></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="e3b45f08a2be41d35408f5ddfb503007" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":44249620,"asset_id":23854995,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/44249620/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="23854995"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="23854995"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 23854995; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=23854995]").text(description); $(".js-view-count[data-work-id=23854995]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 23854995; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='23854995']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "e3b45f08a2be41d35408f5ddfb503007" } } $('.js-work-strip[data-work-id=23854995]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":23854995,"title":"Eruptive scenario of ash-dominated events at Vesuvius: the AP3 eruption (2,710±60 years BP)","translated_title":"","metadata":{"ai_abstract":"Eruptive scenarios dominated by ash emission at Vesuvius have significant implications for understanding volcanic risks. The AP3 eruption, dated 2,710±60 years BP, illustrates mechanisms of ash production influenced by magma-water interactions. 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-23854994-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="12941618"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/12941618/Ash_production_within_a_pyroclastic_flow_grain_size_variations_due_to_mechanical_grinding"><img alt="Research paper thumbnail of Ash production within a pyroclastic flow: grain-size variations due to mechanical grinding" class="work-thumbnail" src="https://attachments.academia-assets.com/45834391/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/12941618/Ash_production_within_a_pyroclastic_flow_grain_size_variations_due_to_mechanical_grinding">Ash production within a pyroclastic flow: grain-size variations due to mechanical grinding</a></div><div class="wp-workCard_item wp-workCard--coauthors"><span>by </span><span><a class="" data-click-track="profile-work-strip-authors" href="https://unica-it.academia.edu/FMundula">F. Mundula</a> and <a class="" data-click-track="profile-work-strip-authors" href="https://ingv.academia.edu/CDOriano">Claudia D'Oriano</a></span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Pyroclastic flow deposits are generally characterized by a large amount of ash. Direct observatio...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Pyroclastic flow deposits are generally characterized by a large amount of ash. Direct observations and stratigraphic studies suggest that a portion of the ash fraction of pyroclastic flow deposits is generated during the transport, by abrasion and collision of largest particles. Conversely, part of the fine grained particles is generally elutriated during transport of the eruptive cloud. Due to their widespread dispersal and low sedimentation rate, ash particles represent a potential risk for living beings and environment. The knowledge of the initial grainsize distribution of an eruptive mixture is of fundamental importance for estimating physical parameters, such as intensity, magnitude and style of an eruption, and represents a basic input parameter for models of column dynamics and transport. In order to study the effect of particle collision and abrasion on the evolution of the particle-size distribution of a pyroclastic mixture,and to relate the production of ash to the evolution of particles shape, we performed grinding experiments using the Los Angeles test. This apparatus allows simulating the process of particle-particle interaction/collision and consequent abrasion and rupture. Starting material consists of three samples from Vesuvius eruptions, representing three end-members in term of textural features of the juvenile material (scoriae vs pumices) and of components that constitute the flow (whole sample vs selected scoriae): VS17 was collected at a proximal site from a flow unit of the subplinian Pollena eruption (472 DC) and represents an example of coarse-grained, lithic rich, matrix supported deposit mainly constituted by scoriaceous juvenile material; C24bis is constituted by juvenile, dm-sized, moderately vesicular scoria-like bombs, selected from a proximal pyroclastic flow deposit of the Pollena eruption (472 DC); while sample VSM80-81 is constituted by cm-sized, highly vesicular pumices from the fallout deposit of the plinian Mercato eruption (8000 yr BP). Three cycles of mechanical grinding were performed on each sample, with a duration of 3, 10 and 30 min, respectively. After each cycle, grain size analyses of experimental products were performed and an aliquot (few grams) of the resulting material from size-classes between -4 and 2 phi collected for morphological studies. In this way, the variation of the shape of the clasts and times of abrasion (roughly corresponding to the runout of the flow) can be correlated. Data are discussed in terms of enrichment in fine grained material with respect to untreated samples, revealing a strong effect of grinding duration and, surprisingly, only a minor control of material properties. Large amounts of ash are produced in the range 3 to 10 phi, with a net increase inside the smaller sizes of up to 2000%. Shape analysis were performed on a subset of 30-50 clasts from each size interval between -4 and 2 phi collected at the end of each experimental run. As good shape descriptors we consider the excess perimeter (?P) and defect area (?A), which well account for the fractured/angular (large ?P and small ?A) and lobate/rounded (large ?A and small ?P) shapes. As we could expect, clast roundness well correlates increasing experimental time with the most of the shape variation occurring immediately after short times of grinding. Grain size and shape data are useful to recognize and quantify co-ignimbrite ash early separated from pyroclastic flows and dispersed over larger areas by different transport mechanisms.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="2543f39024d25b4efd070ef2670cb653" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":45834391,"asset_id":12941618,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/45834391/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="12941618"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="12941618"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 12941618; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=12941618]").text(description); $(".js-view-count[data-work-id=12941618]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 12941618; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='12941618']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "2543f39024d25b4efd070ef2670cb653" } } $('.js-work-strip[data-work-id=12941618]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":12941618,"title":"Ash production within a pyroclastic flow: grain-size variations due to mechanical grinding","translated_title":"","metadata":{"ai_title_tag":"Ash Production from Pyroclastic Flow Grinding","grobid_abstract":"Pyroclastic flow deposits are generally characterized by a large amount of ash. Direct observations and stratigraphic studies suggest that a portion of the ash fraction of pyroclastic flow deposits is generated during the transport, by abrasion and collision of largest particles. Conversely, part of the fine grained particles is generally elutriated during transport of the eruptive cloud. Due to their widespread dispersal and low sedimentation rate, ash particles represent a potential risk for living beings and environment. The knowledge of the initial grainsize distribution of an eruptive mixture is of fundamental importance for estimating physical parameters, such as intensity, magnitude and style of an eruption, and represents a basic input parameter for models of column dynamics and transport. In order to study the effect of particle collision and abrasion on the evolution of the particle-size distribution of a pyroclastic mixture,and to relate the production of ash to the evolution of particles shape, we performed grinding experiments using the Los Angeles test. This apparatus allows simulating the process of particle-particle interaction/collision and consequent abrasion and rupture. Starting material consists of three samples from Vesuvius eruptions, representing three end-members in term of textural features of the juvenile material (scoriae vs pumices) and of components that constitute the flow (whole sample vs selected scoriae): VS17 was collected at a proximal site from a flow unit of the subplinian Pollena eruption (472 DC) and represents an example of coarse-grained, lithic rich, matrix supported deposit mainly constituted by scoriaceous juvenile material; C24bis is constituted by juvenile, dm-sized, moderately vesicular scoria-like bombs, selected from a proximal pyroclastic flow deposit of the Pollena eruption (472 DC); while sample VSM80-81 is constituted by cm-sized, highly vesicular pumices from the fallout deposit of the plinian Mercato eruption (8000 yr BP). Three cycles of mechanical grinding were performed on each sample, with a duration of 3, 10 and 30 min, respectively. After each cycle, grain size analyses of experimental products were performed and an aliquot (few grams) of the resulting material from size-classes between -4 and 2 phi collected for morphological studies. In this way, the variation of the shape of the clasts and times of abrasion (roughly corresponding to the runout of the flow) can be correlated. Data are discussed in terms of enrichment in fine grained material with respect to untreated samples, revealing a strong effect of grinding duration and, surprisingly, only a minor control of material properties. Large amounts of ash are produced in the range 3 to 10 phi, with a net increase inside the smaller sizes of up to 2000%. Shape analysis were performed on a subset of 30-50 clasts from each size interval between -4 and 2 phi collected at the end of each experimental run. As good shape descriptors we consider the excess perimeter (?P) and defect area (?A), which well account for the fractured/angular (large ?P and small ?A) and lobate/rounded (large ?A and small ?P) shapes. As we could expect, clast roundness well correlates increasing experimental time with the most of the shape variation occurring immediately after short times of grinding. Grain size and shape data are useful to recognize and quantify co-ignimbrite ash early separated from pyroclastic flows and dispersed over larger areas by different transport mechanisms.","grobid_abstract_attachment_id":45834391},"translated_abstract":null,"internal_url":"https://www.academia.edu/12941618/Ash_production_within_a_pyroclastic_flow_grain_size_variations_due_to_mechanical_grinding","translated_internal_url":"","created_at":"2015-06-12T02:01:51.266-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":32123250,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":18141909,"work_id":12941618,"tagging_user_id":32123250,"tagged_user_id":14420859,"co_author_invite_id":null,"email":"d***o@pi.ingv.it","affiliation":"Istituto Nazionale di Geofisica e Vulcanologia","display_order":0,"name":"Claudia D'Oriano","title":"Ash production within a pyroclastic flow: grain-size variations due to mechanical grinding"},{"id":18141911,"work_id":12941618,"tagging_user_id":32123250,"tagged_user_id":36210384,"co_author_invite_id":null,"email":"a***i@ingv.it","display_order":4194304,"name":"A. Bertagnini","title":"Ash production within a pyroclastic flow: grain-size variations due to mechanical grinding"},{"id":18141917,"work_id":12941618,"tagging_user_id":32123250,"tagged_user_id":null,"co_author_invite_id":298986,"email":"r***i@unica.it","display_order":6291456,"name":"Raffaello Cioni","title":"Ash production within a pyroclastic flow: grain-size variations due to mechanical grinding"}],"downloadable_attachments":[{"id":45834391,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/45834391/thumbnails/1.jpg","file_name":"Ash_production_within_a_pyroclastic_flow20160521-20507-djnfzp.pdf","download_url":"https://www.academia.edu/attachments/45834391/download_file","bulk_download_file_name":"Ash_production_within_a_pyroclastic_flow.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/45834391/Ash_production_within_a_pyroclastic_flow20160521-20507-djnfzp-libre.pdf?1463846996=\u0026response-content-disposition=attachment%3B+filename%3DAsh_production_within_a_pyroclastic_flow.pdf\u0026Expires=1743974707\u0026Signature=gI93xh2y6YBqK9ajW-AHtKVzYbCu-WbhQaYj-cx7BKjGWQs8a95TnSTgE7c~9dgR6eu7Aaysvcg82i~bBfUwbO7Koid1nwZ0iv5DEWpDJ~~TVcuh88E4Nanjsu2iuY38pEZuXPqGGGOfglv4HA4KM8da4P1SnllM9v~yCsenyRrcIc2SB7zseTQVsGqxQs3Z6VFrD93YxJieUGvHeL~R0pHwog8FYz4dzU038Hr7iDLyBzlodMhxIRAo6lIkErnr~xjH28pSxJCZKU7WfMoGEOaEtvETjs6s7gDgMwwkNheZBQvzS4Lsbrwt49ej~I~UcACJyGDpaqAkZo7dJz2jfw__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Ash_production_within_a_pyroclastic_flow_grain_size_variations_due_to_mechanical_grinding","translated_slug":"","page_count":1,"language":"en","content_type":"Work","summary":"Pyroclastic flow deposits are generally characterized by a large amount of ash. Direct observations and stratigraphic studies suggest that a portion of the ash fraction of pyroclastic flow deposits is generated during the transport, by abrasion and collision of largest particles. Conversely, part of the fine grained particles is generally elutriated during transport of the eruptive cloud. Due to their widespread dispersal and low sedimentation rate, ash particles represent a potential risk for living beings and environment. The knowledge of the initial grainsize distribution of an eruptive mixture is of fundamental importance for estimating physical parameters, such as intensity, magnitude and style of an eruption, and represents a basic input parameter for models of column dynamics and transport. In order to study the effect of particle collision and abrasion on the evolution of the particle-size distribution of a pyroclastic mixture,and to relate the production of ash to the evolution of particles shape, we performed grinding experiments using the Los Angeles test. This apparatus allows simulating the process of particle-particle interaction/collision and consequent abrasion and rupture. Starting material consists of three samples from Vesuvius eruptions, representing three end-members in term of textural features of the juvenile material (scoriae vs pumices) and of components that constitute the flow (whole sample vs selected scoriae): VS17 was collected at a proximal site from a flow unit of the subplinian Pollena eruption (472 DC) and represents an example of coarse-grained, lithic rich, matrix supported deposit mainly constituted by scoriaceous juvenile material; C24bis is constituted by juvenile, dm-sized, moderately vesicular scoria-like bombs, selected from a proximal pyroclastic flow deposit of the Pollena eruption (472 DC); while sample VSM80-81 is constituted by cm-sized, highly vesicular pumices from the fallout deposit of the plinian Mercato eruption (8000 yr BP). Three cycles of mechanical grinding were performed on each sample, with a duration of 3, 10 and 30 min, respectively. After each cycle, grain size analyses of experimental products were performed and an aliquot (few grams) of the resulting material from size-classes between -4 and 2 phi collected for morphological studies. In this way, the variation of the shape of the clasts and times of abrasion (roughly corresponding to the runout of the flow) can be correlated. Data are discussed in terms of enrichment in fine grained material with respect to untreated samples, revealing a strong effect of grinding duration and, surprisingly, only a minor control of material properties. Large amounts of ash are produced in the range 3 to 10 phi, with a net increase inside the smaller sizes of up to 2000%. Shape analysis were performed on a subset of 30-50 clasts from each size interval between -4 and 2 phi collected at the end of each experimental run. As good shape descriptors we consider the excess perimeter (?P) and defect area (?A), which well account for the fractured/angular (large ?P and small ?A) and lobate/rounded (large ?A and small ?P) shapes. As we could expect, clast roundness well correlates increasing experimental time with the most of the shape variation occurring immediately after short times of grinding. Grain size and shape data are useful to recognize and quantify co-ignimbrite ash early separated from pyroclastic flows and dispersed over larger areas by different transport mechanisms.","impression_tracking_id":null,"owner":{"id":32123250,"first_name":"F.","middle_initials":null,"last_name":"Mundula","page_name":"FMundula","domain_name":"unica-it","created_at":"2015-06-12T02:01:26.207-07:00","display_name":"F. 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Bertagnini</a> and <a class="" data-click-track="profile-work-strip-authors" href="https://ingv.academia.edu/CDOriano">Claudia D'Oriano</a></span></div><div class="wp-workCard_item"><span>Geophysical Research Letters</span><span>, 2012</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">ABSTRACT 1] Textures, petrography and geochemical compositions of products emitted during the ons...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">ABSTRACT 1] Textures, petrography and geochemical compositions of products emitted during the onset of the 2011–2012 sub-marine eruption (15 October, 2011) off the coast of El Hierro have been investigated to get information on interaction mechanism between the first rising magma and the crust during the onset of the eruption as well as to get information on magma storage and plumbing systems beneath El Hierro volcano. Studied products consist of 5–50 cm bombs with an outer black to greenish, vesicular crust with bulk basanite composition containing pumiceous xenoliths (xenopumices). Our results show that xenopumices are much more hetero-geneous that previously observed, since consist of a macro-scale mingling of a gray trachyte and white rhyolite. We interpreted xenopumices as resulting from the interaction (heating) between the basanitic magma feeding the eruption, a stagnant trachytic magma pocket/s and an associated hydro-thermally altered halo with rhyolitic composition. Our find-ings confirm the importance of the study of the early products of an eruption since they can contain crucial information on the plumbing system geometry and the mechanism of magma ascent. Citation: Meletlidis, S.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="d80a7659ca92e883811678826a8510ae" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":42400553,"asset_id":16777156,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/42400553/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="16777156"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="16777156"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 16777156; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=16777156]").text(description); $(".js-view-count[data-work-id=16777156]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 16777156; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='16777156']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "d80a7659ca92e883811678826a8510ae" } } $('.js-work-strip[data-work-id=16777156]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":16777156,"title":"Xenopumices from the 2011-2012 submarine eruption of El Hierro (Canary Islands, Spain): Constraints on the plumbing system and magma ascent","translated_title":"","metadata":{"abstract":"ABSTRACT 1] Textures, petrography and geochemical compositions of products emitted during the onset of the 2011–2012 sub-marine eruption (15 October, 2011) off the coast of El Hierro have been investigated to get information on interaction mechanism between the first rising magma and the crust during the onset of the eruption as well as to get information on magma storage and plumbing systems beneath El Hierro volcano. Studied products consist of 5–50 cm bombs with an outer black to greenish, vesicular crust with bulk basanite composition containing pumiceous xenoliths (xenopumices). Our results show that xenopumices are much more hetero-geneous that previously observed, since consist of a macro-scale mingling of a gray trachyte and white rhyolite. We interpreted xenopumices as resulting from the interaction (heating) between the basanitic magma feeding the eruption, a stagnant trachytic magma pocket/s and an associated hydro-thermally altered halo with rhyolitic composition. Our find-ings confirm the importance of the study of the early products of an eruption since they can contain crucial information on the plumbing system geometry and the mechanism of magma ascent. Citation: Meletlidis, S.","ai_title_tag":"Magma Ascent and Plumbing System from El Hierro's Eruption","publication_date":{"day":null,"month":null,"year":2012,"errors":{}},"publication_name":"Geophysical Research Letters"},"translated_abstract":"ABSTRACT 1] Textures, petrography and geochemical compositions of products emitted during the onset of the 2011–2012 sub-marine eruption (15 October, 2011) off the coast of El Hierro have been investigated to get information on interaction mechanism between the first rising magma and the crust during the onset of the eruption as well as to get information on magma storage and plumbing systems beneath El Hierro volcano. Studied products consist of 5–50 cm bombs with an outer black to greenish, vesicular crust with bulk basanite composition containing pumiceous xenoliths (xenopumices). Our results show that xenopumices are much more hetero-geneous that previously observed, since consist of a macro-scale mingling of a gray trachyte and white rhyolite. We interpreted xenopumices as resulting from the interaction (heating) between the basanitic magma feeding the eruption, a stagnant trachytic magma pocket/s and an associated hydro-thermally altered halo with rhyolitic composition. Our find-ings confirm the importance of the study of the early products of an eruption since they can contain crucial information on the plumbing system geometry and the mechanism of magma ascent. 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Studied products consist of 5–50 cm bombs with an outer black to greenish, vesicular crust with bulk basanite composition containing pumiceous xenoliths (xenopumices). Our results show that xenopumices are much more hetero-geneous that previously observed, since consist of a macro-scale mingling of a gray trachyte and white rhyolite. We interpreted xenopumices as resulting from the interaction (heating) between the basanitic magma feeding the eruption, a stagnant trachytic magma pocket/s and an associated hydro-thermally altered halo with rhyolitic composition. Our find-ings confirm the importance of the study of the early products of an eruption since they can contain crucial information on the plumbing system geometry and the mechanism of magma ascent. 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The deposits of this<br />eruption consist of an alternation of massive and thinly laminated ash layers and minor well sorted lapilli beds,<br />reflecting the pulsatory injection into the atmosphere of<br />variably concentrated ash-plumes alternating with Violent<br />Strombolian stages. Despite its nearly constant chemical<br />composition, the juvenile material shows variable external<br />clast morphologies and groundmass textures, reflecting the<br />fragmentation of a magma body with lateral and/or vertical<br />gradients in both vesicularity and crystal content. Glass<br />compositions and mineralogical assemblages indicate that the<br />eruption was fed by rather homogeneous phonotephritic<br />magma batches rising from a reservoir located at ~ 4 km<br />(100 MPa) depth, with fluctuations between magma delivery<br />and magma discharge. Using crystal size distribution (CSD)<br />analyses of plagioclase and leucite microlites, we estimate that<br />the transit time of the magma in the conduit was on the order<br />of ~ 2 days, corresponding to an ascent rate of around 2×<br />10−2 ms−1. Accordingly, assuming a typical conduit diameter<br />for this type of eruption, the minimum duration of the AS1a<br />event is between about 1.5 and 6 years. Magma fragmentation<br />occurred in an inertially driven regime that, in a magma<br />with low viscosity and surface tension, can act also under<br />conditions of slow ascent.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="0956e6172715b5918d61383af8016995" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":35229015,"asset_id":8899852,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/35229015/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="8899852"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="8899852"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 8899852; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=8899852]").text(description); $(".js-view-count[data-work-id=8899852]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 8899852; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='8899852']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "0956e6172715b5918d61383af8016995" } } $('.js-work-strip[data-work-id=8899852]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":8899852,"title":"Dynamics of ash-dominated eruptions at Vesuvius: the post-512 AD AS1a event","translated_title":"","metadata":{"abstract":"Recent stratigraphic studies at Vesuvius have\nrevealed that, during the past 4,000 years, long lasting,\nmoderate to low-intensity eruptions, associated with continuous\nor pulsating ash emission, have repeatedly occurred.\nThe present work focuses on the AS1a eruption, the\nfirst of a series of ash-dominated explosive episodes which\ncharacterized the period between the two Subplinian\neruptions of 472 AD and 1631 AD. The deposits of this\neruption consist of an alternation of massive and thinly laminated ash layers and minor well sorted lapilli beds,\nreflecting the pulsatory injection into the atmosphere of\nvariably concentrated ash-plumes alternating with Violent\nStrombolian stages. Despite its nearly constant chemical\ncomposition, the juvenile material shows variable external\nclast morphologies and groundmass textures, reflecting the\nfragmentation of a magma body with lateral and/or vertical\ngradients in both vesicularity and crystal content. Glass\ncompositions and mineralogical assemblages indicate that the\neruption was fed by rather homogeneous phonotephritic\nmagma batches rising from a reservoir located at ~ 4 km\n(100 MPa) depth, with fluctuations between magma delivery\nand magma discharge. Using crystal size distribution (CSD)\nanalyses of plagioclase and leucite microlites, we estimate that\nthe transit time of the magma in the conduit was on the order\nof ~ 2 days, corresponding to an ascent rate of around 2×\n10−2 ms−1. Accordingly, assuming a typical conduit diameter\nfor this type of eruption, the minimum duration of the AS1a\nevent is between about 1.5 and 6 years. Magma fragmentation\noccurred in an inertially driven regime that, in a magma\nwith low viscosity and surface tension, can act also under\nconditions of slow ascent."},"translated_abstract":"Recent stratigraphic studies at Vesuvius have\nrevealed that, during the past 4,000 years, long lasting,\nmoderate to low-intensity eruptions, associated with continuous\nor pulsating ash emission, have repeatedly occurred.\nThe present work focuses on the AS1a eruption, the\nfirst of a series of ash-dominated explosive episodes which\ncharacterized the period between the two Subplinian\neruptions of 472 AD and 1631 AD. The deposits of this\neruption consist of an alternation of massive and thinly laminated ash layers and minor well sorted lapilli beds,\nreflecting the pulsatory injection into the atmosphere of\nvariably concentrated ash-plumes alternating with Violent\nStrombolian stages. Despite its nearly constant chemical\ncomposition, the juvenile material shows variable external\nclast morphologies and groundmass textures, reflecting the\nfragmentation of a magma body with lateral and/or vertical\ngradients in both vesicularity and crystal content. Glass\ncompositions and mineralogical assemblages indicate that the\neruption was fed by rather homogeneous phonotephritic\nmagma batches rising from a reservoir located at ~ 4 km\n(100 MPa) depth, with fluctuations between magma delivery\nand magma discharge. Using crystal size distribution (CSD)\nanalyses of plagioclase and leucite microlites, we estimate that\nthe transit time of the magma in the conduit was on the order\nof ~ 2 days, corresponding to an ascent rate of around 2×\n10−2 ms−1. Accordingly, assuming a typical conduit diameter\nfor this type of eruption, the minimum duration of the AS1a\nevent is between about 1.5 and 6 years. Magma fragmentation\noccurred in an inertially driven regime that, in a magma\nwith low viscosity and surface tension, can act also under\nconditions of slow ascent.","internal_url":"https://www.academia.edu/8899852/Dynamics_of_ash_dominated_eruptions_at_Vesuvius_the_post_512_AD_AS1a_event","translated_internal_url":"","created_at":"2014-10-21T20:23:43.920-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":14420859,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":7992065,"work_id":8899852,"tagging_user_id":14420859,"tagged_user_id":36210384,"co_author_invite_id":null,"email":"a***i@ingv.it","display_order":0,"name":"A. Bertagnini","title":"Dynamics of ash-dominated eruptions at Vesuvius: the post-512 AD AS1a event"},{"id":18172523,"work_id":8899852,"tagging_user_id":14420859,"tagged_user_id":37146682,"co_author_invite_id":null,"email":"p***e@plymouth.ac.uk","display_order":4194304,"name":"P. Cole","title":"Dynamics of ash-dominated eruptions at Vesuvius: the post-512 AD AS1a event"},{"id":18172524,"work_id":8899852,"tagging_user_id":14420859,"tagged_user_id":null,"co_author_invite_id":654632,"email":"a***o@ct.ingv.it","display_order":6291456,"name":"Daniele Andronico","title":"Dynamics of ash-dominated eruptions at Vesuvius: the post-512 AD AS1a event"},{"id":18172537,"work_id":8899852,"tagging_user_id":14420859,"tagged_user_id":32521915,"co_author_invite_id":null,"email":"r***i@unifi.it","display_order":7340032,"name":"R. Cioni","title":"Dynamics of ash-dominated eruptions at Vesuvius: the post-512 AD AS1a event"}],"downloadable_attachments":[{"id":35229015,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/35229015/thumbnails/1.jpg","file_name":"DOriano_et_al_2011.pdf","download_url":"https://www.academia.edu/attachments/35229015/download_file","bulk_download_file_name":"Dynamics_of_ash_dominated_eruptions_at_V.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/35229015/DOriano_et_al_2011-libre.pdf?1413948161=\u0026response-content-disposition=attachment%3B+filename%3DDynamics_of_ash_dominated_eruptions_at_V.pdf\u0026Expires=1743974710\u0026Signature=ch3Nz2~7LeJYSrk2L1BrFwuxDUCso7N3qGymKaSNuiYiTuZ5sJt0jrY1uj5MOPyEU~7yfDS~WkhhicBwLxRGJwczvg6JlS~7bXJ6rJdC6oBIFfo6ij084NcaHtqmLW1MUgBV~Toy3i6bETorm4OR4bjNadL1RzEFjY-1f3hsDHEig8gAwkM-0rm6i2y-vzWbngvNB5hMsMTE7CtzC9VKuk-7WuKpuTgpb1P~NDuQsPVXywCjIVBoQlX6b-nkQNGiJe10cUsyTaKsEVtsbt5rUwjX~Qfnr5SQn9VMPZW7YXXEfpc12iCYd5AO3-Dwwz5Uvk3TS2nvpSSPnkVMblQVrw__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Dynamics_of_ash_dominated_eruptions_at_Vesuvius_the_post_512_AD_AS1a_event","translated_slug":"","page_count":19,"language":"en","content_type":"Work","summary":"Recent stratigraphic studies at Vesuvius have\nrevealed that, during the past 4,000 years, long lasting,\nmoderate to low-intensity eruptions, associated with continuous\nor pulsating ash emission, have repeatedly occurred.\nThe present work focuses on the AS1a eruption, the\nfirst of a series of ash-dominated explosive episodes which\ncharacterized the period between the two Subplinian\neruptions of 472 AD and 1631 AD. The deposits of this\neruption consist of an alternation of massive and thinly laminated ash layers and minor well sorted lapilli beds,\nreflecting the pulsatory injection into the atmosphere of\nvariably concentrated ash-plumes alternating with Violent\nStrombolian stages. Despite its nearly constant chemical\ncomposition, the juvenile material shows variable external\nclast morphologies and groundmass textures, reflecting the\nfragmentation of a magma body with lateral and/or vertical\ngradients in both vesicularity and crystal content. Glass\ncompositions and mineralogical assemblages indicate that the\neruption was fed by rather homogeneous phonotephritic\nmagma batches rising from a reservoir located at ~ 4 km\n(100 MPa) depth, with fluctuations between magma delivery\nand magma discharge. Using crystal size distribution (CSD)\nanalyses of plagioclase and leucite microlites, we estimate that\nthe transit time of the magma in the conduit was on the order\nof ~ 2 days, corresponding to an ascent rate of around 2×\n10−2 ms−1. Accordingly, assuming a typical conduit diameter\nfor this type of eruption, the minimum duration of the AS1a\nevent is between about 1.5 and 6 years. Magma fragmentation\noccurred in an inertially driven regime that, in a magma\nwith low viscosity and surface tension, can act also under\nconditions of slow ascent.","impression_tracking_id":null,"owner":{"id":14420859,"first_name":"Claudia","middle_initials":null,"last_name":"D'Oriano","page_name":"CDOriano","domain_name":"ingv","created_at":"2014-07-27T18:56:54.386-07:00","display_name":"Claudia D'Oriano","url":"https://ingv.academia.edu/CDOriano"},"attachments":[{"id":35229015,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/35229015/thumbnails/1.jpg","file_name":"DOriano_et_al_2011.pdf","download_url":"https://www.academia.edu/attachments/35229015/download_file","bulk_download_file_name":"Dynamics_of_ash_dominated_eruptions_at_V.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/35229015/DOriano_et_al_2011-libre.pdf?1413948161=\u0026response-content-disposition=attachment%3B+filename%3DDynamics_of_ash_dominated_eruptions_at_V.pdf\u0026Expires=1743974710\u0026Signature=ch3Nz2~7LeJYSrk2L1BrFwuxDUCso7N3qGymKaSNuiYiTuZ5sJt0jrY1uj5MOPyEU~7yfDS~WkhhicBwLxRGJwczvg6JlS~7bXJ6rJdC6oBIFfo6ij084NcaHtqmLW1MUgBV~Toy3i6bETorm4OR4bjNadL1RzEFjY-1f3hsDHEig8gAwkM-0rm6i2y-vzWbngvNB5hMsMTE7CtzC9VKuk-7WuKpuTgpb1P~NDuQsPVXywCjIVBoQlX6b-nkQNGiJe10cUsyTaKsEVtsbt5rUwjX~Qfnr5SQn9VMPZW7YXXEfpc12iCYd5AO3-Dwwz5Uvk3TS2nvpSSPnkVMblQVrw__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":1370,"name":"Volcanology","url":"https://www.academia.edu/Documents/in/Volcanology"},{"id":78128,"name":"Vesuvius","url":"https://www.academia.edu/Documents/in/Vesuvius"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-8899852-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="8899826"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/8899826/Effects_of_experimental_reheating_of_natural_basaltic_ash_at_different_temperatures_and_redox_conditions"><img alt="Research paper thumbnail of Effects of experimental reheating of natural basaltic ash at different temperatures and redox conditions" class="work-thumbnail" src="https://attachments.academia-assets.com/35228999/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/8899826/Effects_of_experimental_reheating_of_natural_basaltic_ash_at_different_temperatures_and_redox_conditions">Effects of experimental reheating of natural basaltic ash at different temperatures and redox conditions</a></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">A set of experiments have been performed on volcanic materials from Etna, Stromboli and Vesuvius ...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">A set of experiments have been performed on<br />volcanic materials from Etna, Stromboli and Vesuvius in<br />order to evaluate how the exposure to thermal and redox<br />conditions close to that of active craters affects the texture<br />and composition of juvenile pyroclasts. Selected samples<br />were placed within a quartz tube, in presence of air or<br />under vacuum, and kept at T between 700 and 1,130 C, for<br />variable time (40 min to 12 h). Results show that reheating<br />reactivates the melt, which, through processes of chemical<br />and thermal diffusion, reaches new equilibrium conditions.<br />In all the experiments performed at T = 700–750 C, a<br />large number of crystal nuclei and spherulites grows in the<br />groundmass, suggesting conditions of high undercooling.<br />This process creates textural heterogeneities at the scale of<br />few microns but only limited changes of groundmass<br />composition, which remains clustered around that of the<br />natural glasses. Reheating at T = 1,000–1,050 C promotes<br />massive groundmass crystallization, with a different<br />mineral assemblage as a function of the redox conditions. Morphological modifications of clasts, from softening to<br />sintering as temperature increases, occur under these conditions,<br />accompanied by progressive smoothing of external<br />surfaces, and a reduction in size and abundance of vesicles,<br />until the complete obliteration of the pre-existing vesicularity.<br />The transition from sintering to welding, characteristic<br />of high temperature, is influenced by redox conditions.<br />Experiments at T = 1,100–1,130 C and under vacuum<br />produce groundmass textures and glass compositions similar<br />to that of the respective starting material. Collapse and<br />welding of the clasts cause significant densification of the<br />whole charge. At the same temperature, but in presence of<br />air, experimental products at least result sintered and show<br />holocrystalline groundmass. In all experiments, sublimates<br />grow on the external surfaces of the clasts or form a lining<br />on the bubble walls. Their shape and composition is a<br />function of temperature and fO2 and the abundance of<br />sublimates shows a peak at 1,000 C. The identification of<br />the features recorded by pyroclasts during complex heating–<br />cooling cycles allows reconstructing the complete<br />clasts history before their final emplacement, during<br />weakly explosive volcanic activity. This has a strong<br />implication on the characterization of primary juvenile<br />material and on the interpretation of eruption dynamics.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="0435ccc572ec492967928f1ebcb4a237" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":35228999,"asset_id":8899826,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/35228999/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="8899826"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="8899826"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 8899826; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=8899826]").text(description); $(".js-view-count[data-work-id=8899826]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 8899826; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='8899826']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "0435ccc572ec492967928f1ebcb4a237" } } $('.js-work-strip[data-work-id=8899826]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":8899826,"title":"Effects of experimental reheating of natural basaltic ash at different temperatures and redox conditions","translated_title":"","metadata":{"abstract":"A set of experiments have been performed on\nvolcanic materials from Etna, Stromboli and Vesuvius in\norder to evaluate how the exposure to thermal and redox\nconditions close to that of active craters affects the texture\nand composition of juvenile pyroclasts. Selected samples\nwere placed within a quartz tube, in presence of air or\nunder vacuum, and kept at T between 700 and 1,130 \u0003C, for\nvariable time (40 min to 12 h). Results show that reheating\nreactivates the melt, which, through processes of chemical\nand thermal diffusion, reaches new equilibrium conditions.\nIn all the experiments performed at T = 700–750 \u0003C, a\nlarge number of crystal nuclei and spherulites grows in the\ngroundmass, suggesting conditions of high undercooling.\nThis process creates textural heterogeneities at the scale of\nfew microns but only limited changes of groundmass\ncomposition, which remains clustered around that of the\nnatural glasses. Reheating at T = 1,000–1,050 \u0003C promotes\nmassive groundmass crystallization, with a different\nmineral assemblage as a function of the redox conditions. Morphological modifications of clasts, from softening to\nsintering as temperature increases, occur under these conditions,\naccompanied by progressive smoothing of external\nsurfaces, and a reduction in size and abundance of vesicles,\nuntil the complete obliteration of the pre-existing vesicularity.\nThe transition from sintering to welding, characteristic\nof high temperature, is influenced by redox conditions.\nExperiments at T = 1,100–1,130 \u0003C and under vacuum\nproduce groundmass textures and glass compositions similar\nto that of the respective starting material. Collapse and\nwelding of the clasts cause significant densification of the\nwhole charge. At the same temperature, but in presence of\nair, experimental products at least result sintered and show\nholocrystalline groundmass. In all experiments, sublimates\ngrow on the external surfaces of the clasts or form a lining\non the bubble walls. Their shape and composition is a\nfunction of temperature and fO2 and the abundance of\nsublimates shows a peak at 1,000 \u0003C. The identification of\nthe features recorded by pyroclasts during complex heating–\ncooling cycles allows reconstructing the complete\nclasts history before their final emplacement, during\nweakly explosive volcanic activity. This has a strong\nimplication on the characterization of primary juvenile\nmaterial and on the interpretation of eruption dynamics.","ai_title_tag":"Reheating Effects on Basaltic Ash Textures"},"translated_abstract":"A set of experiments have been performed on\nvolcanic materials from Etna, Stromboli and Vesuvius in\norder to evaluate how the exposure to thermal and redox\nconditions close to that of active craters affects the texture\nand composition of juvenile pyroclasts. Selected samples\nwere placed within a quartz tube, in presence of air or\nunder vacuum, and kept at T between 700 and 1,130 \u0003C, for\nvariable time (40 min to 12 h). Results show that reheating\nreactivates the melt, which, through processes of chemical\nand thermal diffusion, reaches new equilibrium conditions.\nIn all the experiments performed at T = 700–750 \u0003C, a\nlarge number of crystal nuclei and spherulites grows in the\ngroundmass, suggesting conditions of high undercooling.\nThis process creates textural heterogeneities at the scale of\nfew microns but only limited changes of groundmass\ncomposition, which remains clustered around that of the\nnatural glasses. Reheating at T = 1,000–1,050 \u0003C promotes\nmassive groundmass crystallization, with a different\nmineral assemblage as a function of the redox conditions. Morphological modifications of clasts, from softening to\nsintering as temperature increases, occur under these conditions,\naccompanied by progressive smoothing of external\nsurfaces, and a reduction in size and abundance of vesicles,\nuntil the complete obliteration of the pre-existing vesicularity.\nThe transition from sintering to welding, characteristic\nof high temperature, is influenced by redox conditions.\nExperiments at T = 1,100–1,130 \u0003C and under vacuum\nproduce groundmass textures and glass compositions similar\nto that of the respective starting material. Collapse and\nwelding of the clasts cause significant densification of the\nwhole charge. At the same temperature, but in presence of\nair, experimental products at least result sintered and show\nholocrystalline groundmass. In all experiments, sublimates\ngrow on the external surfaces of the clasts or form a lining\non the bubble walls. Their shape and composition is a\nfunction of temperature and fO2 and the abundance of\nsublimates shows a peak at 1,000 \u0003C. The identification of\nthe features recorded by pyroclasts during complex heating–\ncooling cycles allows reconstructing the complete\nclasts history before their final emplacement, during\nweakly explosive volcanic activity. This has a strong\nimplication on the characterization of primary juvenile\nmaterial and on the interpretation of eruption dynamics.","internal_url":"https://www.academia.edu/8899826/Effects_of_experimental_reheating_of_natural_basaltic_ash_at_different_temperatures_and_redox_conditions","translated_internal_url":"","created_at":"2014-10-21T20:21:36.111-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":14420859,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":35228999,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/35228999/thumbnails/1.jpg","file_name":"DOriano_et_al_CMP2012.pdf","download_url":"https://www.academia.edu/attachments/35228999/download_file","bulk_download_file_name":"Effects_of_experimental_reheating_of_nat.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/35228999/DOriano_et_al_CMP2012-libre.pdf?1413948071=\u0026response-content-disposition=attachment%3B+filename%3DEffects_of_experimental_reheating_of_nat.pdf\u0026Expires=1743974710\u0026Signature=VoHgJlq-uWPQirTjUiWLf5zkXJANZ94l8eRIdHV4L9SR6D2n4ql0uxSDF5h-leQ-l-HjMPa7BZnwKRRuOvv~V5ZjKissF4h0XIwS0Z0HUkh-xzK1XuMSoJSMPVz5luUSMBpet-KHYiBswMPiDjva-QA10U8x6QpEA4wQQoqKnkncsfhfsCPldnMIUu0VDiMrsluVdEuQ-VM5AfxnEsTFQjHG0kp1Jj-xNH3yqTawctZDFlGiw4nkLpRTfl7U8MaBEYbwwlhChqyl9cQhZjifPdYdD7o3NJeL8wirtEkXqUpkWSdbhmJGzE8FW8KITBdgh8~JT25EoFaECGF8ADJXBQ__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Effects_of_experimental_reheating_of_natural_basaltic_ash_at_different_temperatures_and_redox_conditions","translated_slug":"","page_count":21,"language":"en","content_type":"Work","summary":"A set of experiments have been performed on\nvolcanic materials from Etna, Stromboli and Vesuvius in\norder to evaluate how the exposure to thermal and redox\nconditions close to that of active craters affects the texture\nand composition of juvenile pyroclasts. Selected samples\nwere placed within a quartz tube, in presence of air or\nunder vacuum, and kept at T between 700 and 1,130 \u0003C, for\nvariable time (40 min to 12 h). Results show that reheating\nreactivates the melt, which, through processes of chemical\nand thermal diffusion, reaches new equilibrium conditions.\nIn all the experiments performed at T = 700–750 \u0003C, a\nlarge number of crystal nuclei and spherulites grows in the\ngroundmass, suggesting conditions of high undercooling.\nThis process creates textural heterogeneities at the scale of\nfew microns but only limited changes of groundmass\ncomposition, which remains clustered around that of the\nnatural glasses. Reheating at T = 1,000–1,050 \u0003C promotes\nmassive groundmass crystallization, with a different\nmineral assemblage as a function of the redox conditions. Morphological modifications of clasts, from softening to\nsintering as temperature increases, occur under these conditions,\naccompanied by progressive smoothing of external\nsurfaces, and a reduction in size and abundance of vesicles,\nuntil the complete obliteration of the pre-existing vesicularity.\nThe transition from sintering to welding, characteristic\nof high temperature, is influenced by redox conditions.\nExperiments at T = 1,100–1,130 \u0003C and under vacuum\nproduce groundmass textures and glass compositions similar\nto that of the respective starting material. Collapse and\nwelding of the clasts cause significant densification of the\nwhole charge. At the same temperature, but in presence of\nair, experimental products at least result sintered and show\nholocrystalline groundmass. In all experiments, sublimates\ngrow on the external surfaces of the clasts or form a lining\non the bubble walls. Their shape and composition is a\nfunction of temperature and fO2 and the abundance of\nsublimates shows a peak at 1,000 \u0003C. The identification of\nthe features recorded by pyroclasts during complex heating–\ncooling cycles allows reconstructing the complete\nclasts history before their final emplacement, during\nweakly explosive volcanic activity. This has a strong\nimplication on the characterization of primary juvenile\nmaterial and on the interpretation of eruption dynamics.","impression_tracking_id":null,"owner":{"id":14420859,"first_name":"Claudia","middle_initials":null,"last_name":"D'Oriano","page_name":"CDOriano","domain_name":"ingv","created_at":"2014-07-27T18:56:54.386-07:00","display_name":"Claudia D'Oriano","url":"https://ingv.academia.edu/CDOriano"},"attachments":[{"id":35228999,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/35228999/thumbnails/1.jpg","file_name":"DOriano_et_al_CMP2012.pdf","download_url":"https://www.academia.edu/attachments/35228999/download_file","bulk_download_file_name":"Effects_of_experimental_reheating_of_nat.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/35228999/DOriano_et_al_CMP2012-libre.pdf?1413948071=\u0026response-content-disposition=attachment%3B+filename%3DEffects_of_experimental_reheating_of_nat.pdf\u0026Expires=1743974710\u0026Signature=VoHgJlq-uWPQirTjUiWLf5zkXJANZ94l8eRIdHV4L9SR6D2n4ql0uxSDF5h-leQ-l-HjMPa7BZnwKRRuOvv~V5ZjKissF4h0XIwS0Z0HUkh-xzK1XuMSoJSMPVz5luUSMBpet-KHYiBswMPiDjva-QA10U8x6QpEA4wQQoqKnkncsfhfsCPldnMIUu0VDiMrsluVdEuQ-VM5AfxnEsTFQjHG0kp1Jj-xNH3yqTawctZDFlGiw4nkLpRTfl7U8MaBEYbwwlhChqyl9cQhZjifPdYdD7o3NJeL8wirtEkXqUpkWSdbhmJGzE8FW8KITBdgh8~JT25EoFaECGF8ADJXBQ__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":51810,"name":"Experimental petrology and volcanology","url":"https://www.academia.edu/Documents/in/Experimental_petrology_and_volcanology"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-8899826-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="8899802"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/8899802/Identifying_recycled_ash_in_basaltic_eruptions"><img alt="Research paper thumbnail of Identifying recycled ash in basaltic eruptions" class="work-thumbnail" src="https://attachments.academia-assets.com/35228958/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/8899802/Identifying_recycled_ash_in_basaltic_eruptions">Identifying recycled ash in basaltic eruptions</a></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Deposits of mid-intensity basaltic explosive eruptions are characterized by the coexistence of di...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Deposits of mid-intensity basaltic explosive eruptions are characterized by the coexistence of different types<br />of juvenile clasts, which show a large variability of external properties and texture, reflecting alternatively the<br />effects of primary processes related to magma storage or ascent, or of syn-eruptive modifications occurred<br />during or immediately after their ejection. If fragments fall back within the crater area before being<br />re-ejected during the ensuing activity, they are subject to thermally- and chemically-induced alterations.<br />These ‘recycled’ clasts can be considered as cognate lithic for the eruption/explosion they derive. Their exact<br />identification has consequences for a correct interpretation of eruption dynamics, with important<br />implications for hazard assessment. On ash erupted during selected basaltic eruptions (at Stromboli, Etna,<br />Vesuvius, Gaua-Vanuatu), we have identified a set of characteristics that can be associated with the<br />occurrence of intra-crater recycling processes, based also on the comparison with results of reheating<br />experiments performed on primary juvenile material, at variable temperature and under different redox<br />conditions.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="b71721d64f6e7df7aa71cb510e7ba252" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":35228958,"asset_id":8899802,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/35228958/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="8899802"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="8899802"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 8899802; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=8899802]").text(description); $(".js-view-count[data-work-id=8899802]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 8899802; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='8899802']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "b71721d64f6e7df7aa71cb510e7ba252" } } $('.js-work-strip[data-work-id=8899802]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":8899802,"title":"Identifying recycled ash in basaltic eruptions","translated_title":"","metadata":{"abstract":"Deposits of mid-intensity basaltic explosive eruptions are characterized by the coexistence of different types\nof juvenile clasts, which show a large variability of external properties and texture, reflecting alternatively the\neffects of primary processes related to magma storage or ascent, or of syn-eruptive modifications occurred\nduring or immediately after their ejection. If fragments fall back within the crater area before being\nre-ejected during the ensuing activity, they are subject to thermally- and chemically-induced alterations.\nThese ‘recycled’ clasts can be considered as cognate lithic for the eruption/explosion they derive. Their exact\nidentification has consequences for a correct interpretation of eruption dynamics, with important\nimplications for hazard assessment. On ash erupted during selected basaltic eruptions (at Stromboli, Etna,\nVesuvius, Gaua-Vanuatu), we have identified a set of characteristics that can be associated with the\noccurrence of intra-crater recycling processes, based also on the comparison with results of reheating\nexperiments performed on primary juvenile material, at variable temperature and under different redox\nconditions.","ai_title_tag":"Identifying Recycled Ash in Basaltic Explosions"},"translated_abstract":"Deposits of mid-intensity basaltic explosive eruptions are characterized by the coexistence of different types\nof juvenile clasts, which show a large variability of external properties and texture, reflecting alternatively the\neffects of primary processes related to magma storage or ascent, or of syn-eruptive modifications occurred\nduring or immediately after their ejection. If fragments fall back within the crater area before being\nre-ejected during the ensuing activity, they are subject to thermally- and chemically-induced alterations.\nThese ‘recycled’ clasts can be considered as cognate lithic for the eruption/explosion they derive. Their exact\nidentification has consequences for a correct interpretation of eruption dynamics, with important\nimplications for hazard assessment. On ash erupted during selected basaltic eruptions (at Stromboli, Etna,\nVesuvius, Gaua-Vanuatu), we have identified a set of characteristics that can be associated with the\noccurrence of intra-crater recycling processes, based also on the comparison with results of reheating\nexperiments performed on primary juvenile material, at variable temperature and under different redox\nconditions.","internal_url":"https://www.academia.edu/8899802/Identifying_recycled_ash_in_basaltic_eruptions","translated_internal_url":"","created_at":"2014-10-21T20:19:49.210-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":14420859,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":18172533,"work_id":8899802,"tagging_user_id":14420859,"tagged_user_id":1501609,"co_author_invite_id":null,"email":"p***o@pi.ingv.it","affiliation":"Istituto Nazionale di Geofisica e Vulcanologia","display_order":0,"name":"Massimo Pompilio","title":"Identifying recycled ash in basaltic eruptions"},{"id":18172541,"work_id":8899802,"tagging_user_id":14420859,"tagged_user_id":36210384,"co_author_invite_id":null,"email":"a***i@ingv.it","display_order":4194304,"name":"A. Bertagnini","title":"Identifying recycled ash in basaltic eruptions"},{"id":18172545,"work_id":8899802,"tagging_user_id":14420859,"tagged_user_id":null,"co_author_invite_id":298986,"email":"r***i@unica.it","display_order":6291456,"name":"Raffaello Cioni","title":"Identifying recycled ash in basaltic eruptions"}],"downloadable_attachments":[{"id":35228958,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/35228958/thumbnails/1.jpg","file_name":"DOriano_et_al_SciRep_2014.pdf","download_url":"https://www.academia.edu/attachments/35228958/download_file","bulk_download_file_name":"Identifying_recycled_ash_in_basaltic_eru.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/35228958/DOriano_et_al_SciRep_2014-libre.pdf?1413947939=\u0026response-content-disposition=attachment%3B+filename%3DIdentifying_recycled_ash_in_basaltic_eru.pdf\u0026Expires=1743974710\u0026Signature=E0N3Zr1srxluAyD76EnYy4U9R0j96RQsTTjVFqzEHinWYIrAwI2apc5J01~UG0JP5mTfCm-fHwFEtslXS8Rjy8nkGo1rzmGjJEAse0wmjrgmjyvRjq3oDOxm4J7DhA4wN8QrjIbu0d1ByGGv46zXX1UmRUILi0KIv2Gf8ia7jA-vNv3sm1vjZpsJ~WpDsk62~8ie2pTdW~yp96iJc98z9RKx54uYw893uEViQDy6d2MUv59V8~v0uOihDIXAEFwZwArtZKVSi3U9n~pTR~ZWqD2acUPYcDIgysj-8HrcSqYhPq~LmZiPwymyrxTUd0PN5P-C0SQUyl-KwKguRDm5dA__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Identifying_recycled_ash_in_basaltic_eruptions","translated_slug":"","page_count":8,"language":"en","content_type":"Work","summary":"Deposits of mid-intensity basaltic explosive eruptions are characterized by the coexistence of different types\nof juvenile clasts, which show a large variability of external properties and texture, reflecting alternatively the\neffects of primary processes related to magma storage or ascent, or of syn-eruptive modifications occurred\nduring or immediately after their ejection. If fragments fall back within the crater area before being\nre-ejected during the ensuing activity, they are subject to thermally- and chemically-induced alterations.\nThese ‘recycled’ clasts can be considered as cognate lithic for the eruption/explosion they derive. Their exact\nidentification has consequences for a correct interpretation of eruption dynamics, with important\nimplications for hazard assessment. On ash erupted during selected basaltic eruptions (at Stromboli, Etna,\nVesuvius, Gaua-Vanuatu), we have identified a set of characteristics that can be associated with the\noccurrence of intra-crater recycling processes, based also on the comparison with results of reheating\nexperiments performed on primary juvenile material, at variable temperature and under different redox\nconditions.","impression_tracking_id":null,"owner":{"id":14420859,"first_name":"Claudia","middle_initials":null,"last_name":"D'Oriano","page_name":"CDOriano","domain_name":"ingv","created_at":"2014-07-27T18:56:54.386-07:00","display_name":"Claudia D'Oriano","url":"https://ingv.academia.edu/CDOriano"},"attachments":[{"id":35228958,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/35228958/thumbnails/1.jpg","file_name":"DOriano_et_al_SciRep_2014.pdf","download_url":"https://www.academia.edu/attachments/35228958/download_file","bulk_download_file_name":"Identifying_recycled_ash_in_basaltic_eru.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/35228958/DOriano_et_al_SciRep_2014-libre.pdf?1413947939=\u0026response-content-disposition=attachment%3B+filename%3DIdentifying_recycled_ash_in_basaltic_eru.pdf\u0026Expires=1743974710\u0026Signature=E0N3Zr1srxluAyD76EnYy4U9R0j96RQsTTjVFqzEHinWYIrAwI2apc5J01~UG0JP5mTfCm-fHwFEtslXS8Rjy8nkGo1rzmGjJEAse0wmjrgmjyvRjq3oDOxm4J7DhA4wN8QrjIbu0d1ByGGv46zXX1UmRUILi0KIv2Gf8ia7jA-vNv3sm1vjZpsJ~WpDsk62~8ie2pTdW~yp96iJc98z9RKx54uYw893uEViQDy6d2MUv59V8~v0uOihDIXAEFwZwArtZKVSi3U9n~pTR~ZWqD2acUPYcDIgysj-8HrcSqYhPq~LmZiPwymyrxTUd0PN5P-C0SQUyl-KwKguRDm5dA__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":1370,"name":"Volcanology","url":"https://www.academia.edu/Documents/in/Volcanology"},{"id":45291,"name":"Volcano monitoring","url":"https://www.academia.edu/Documents/in/Volcano_monitoring"},{"id":206238,"name":"Volcanic ash","url":"https://www.academia.edu/Documents/in/Volcanic_ash"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-8899802-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="7794657"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/7794657/Oxygen_isotope_geochemistry_of_mafic_magmas_at_Mt_Vesuvius"><img alt="Research paper thumbnail of Oxygen isotope geochemistry of mafic magmas at Mt. Vesuvius" class="work-thumbnail" src="https://attachments.academia-assets.com/48339158/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/7794657/Oxygen_isotope_geochemistry_of_mafic_magmas_at_Mt_Vesuvius">Oxygen isotope geochemistry of mafic magmas at Mt. Vesuvius</a></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Pumice and scoria from different eruptive layers of Mt. Vesuvius volcanic products contain mafic ...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Pumice and scoria from different eruptive layers of Mt. Vesuvius volcanic products contain mafic minerals consisting of High-Fo olivine and Diopsidic Pyroxene. These phases were crystallized in unerupted trachibasaltic to tephritic magmas, and were brought to surface by large phonolitic/tephri-phonolitic (e.g. Avellino and Pompei) and/or of tephritic and phono-tephritic (Pollena) eruptions. A large set of these mm-sized crystals was accurately separated from selected juvenile material and measured for their chemical compositions (EPMA, Laser Ablation ICP-MS) and 18O/16O ratios (conventional laser fluorination) to constrain the nature and evolution of the primary magmas at Mt. Vesuvius. Uncontaminated mantle δ18O values are hardly recovered in Italian Quaternary magmas, mostly due to the widespread occurrence of crustal contamination of the primary melts during their ascent to the surface (e.g. Alban Hills, Ernici Mts., and Aeolian Islands). At Mt. Vesuvius, measured olivine and clinopyroxene share quite homogeneous chemical compositions (Olivine Fo 85-90 ; Diopside En 45-48, respectively), and represent phases crystallized in near primary mafic magmas. Trace element composition constrains the near primary nature of the phases. Published data on volatile content of melt inclusions hosted in these crystals reveal the coexistence of dissolved water and carbon dioxide, and a minimum trapping pressure around 200-300 MPa, suggesting that crystal growth occurred in a reservoir at about 8-10 km depth. Recently, experimental data have suggested massive carbonate assimilation (up to about 20%) to derive potassic alkali magmas from trachybasaltic melts. Accordingly, the δ18O variability and the trace element content of the studied minerals suggest possible contamination of primary melts by an O-isotope enriched, REE-poor contaminant like the limestone of Vesuvius basement. Low, nearly primitive δ18O values are observed for olivine from Pompeii eruption, although still above the range of typical mantle minerals. The δ18Oolivine and δ18Ocpxof the minerals from all the studied eruptions define variable degrees of carbonate interaction and magma crystallization for the different eruptions, and possibly within the same eruption, and show evidence of oxygen isotope equilibrium at high temperature. However, energy-constrained AFC model suggest that carbonate assimilation was limited. On the basis of our data, we suggest that interaction between magma and a fluxing, decarbonation-derived CO2 fluid may be partly accounted for the measured O-isotope compositions.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="8f00255810159f42493cbcf82fd3fb3d" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":48339158,"asset_id":7794657,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/48339158/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="7794657"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="7794657"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 7794657; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=7794657]").text(description); $(".js-view-count[data-work-id=7794657]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 7794657; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='7794657']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "8f00255810159f42493cbcf82fd3fb3d" } } $('.js-work-strip[data-work-id=7794657]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":7794657,"title":"Oxygen isotope geochemistry of mafic magmas at Mt. 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Uncontaminated mantle δ18O values are hardly recovered in Italian Quaternary magmas, mostly due to the widespread occurrence of crustal contamination of the primary melts during their ascent to the surface (e.g. Alban Hills, Ernici Mts., and Aeolian Islands). At Mt. Vesuvius, measured olivine and clinopyroxene share quite homogeneous chemical compositions (Olivine Fo 85-90 ; Diopside En 45-48, respectively), and represent phases crystallized in near primary mafic magmas. Trace element composition constrains the near primary nature of the phases. Published data on volatile content of melt inclusions hosted in these crystals reveal the coexistence of dissolved water and carbon dioxide, and a minimum trapping pressure around 200-300 MPa, suggesting that crystal growth occurred in a reservoir at about 8-10 km depth. Recently, experimental data have suggested massive carbonate assimilation (up to about 20%) to derive potassic alkali magmas from trachybasaltic melts. Accordingly, the δ18O variability and the trace element content of the studied minerals suggest possible contamination of primary melts by an O-isotope enriched, REE-poor contaminant like the limestone of Vesuvius basement. Low, nearly primitive δ18O values are observed for olivine from Pompeii eruption, although still above the range of typical mantle minerals. The δ18Oolivine and δ18Ocpxof the minerals from all the studied eruptions define variable degrees of carbonate interaction and magma crystallization for the different eruptions, and possibly within the same eruption, and show evidence of oxygen isotope equilibrium at high temperature. However, energy-constrained AFC model suggest that carbonate assimilation was limited. On the basis of our data, we suggest that interaction between magma and a fluxing, decarbonation-derived CO2 fluid may be partly accounted for the measured O-isotope compositions.","publication_date":{"day":null,"month":null,"year":2010,"errors":{}}},"translated_abstract":"Pumice and scoria from different eruptive layers of Mt. Vesuvius volcanic products contain mafic minerals consisting of High-Fo olivine and Diopsidic Pyroxene. These phases were crystallized in unerupted trachibasaltic to tephritic magmas, and were brought to surface by large phonolitic/tephri-phonolitic (e.g. Avellino and Pompei) and/or of tephritic and phono-tephritic (Pollena) eruptions. A large set of these mm-sized crystals was accurately separated from selected juvenile material and measured for their chemical compositions (EPMA, Laser Ablation ICP-MS) and 18O/16O ratios (conventional laser fluorination) to constrain the nature and evolution of the primary magmas at Mt. Vesuvius. Uncontaminated mantle δ18O values are hardly recovered in Italian Quaternary magmas, mostly due to the widespread occurrence of crustal contamination of the primary melts during their ascent to the surface (e.g. Alban Hills, Ernici Mts., and Aeolian Islands). At Mt. Vesuvius, measured olivine and clinopyroxene share quite homogeneous chemical compositions (Olivine Fo 85-90 ; Diopside En 45-48, respectively), and represent phases crystallized in near primary mafic magmas. Trace element composition constrains the near primary nature of the phases. Published data on volatile content of melt inclusions hosted in these crystals reveal the coexistence of dissolved water and carbon dioxide, and a minimum trapping pressure around 200-300 MPa, suggesting that crystal growth occurred in a reservoir at about 8-10 km depth. Recently, experimental data have suggested massive carbonate assimilation (up to about 20%) to derive potassic alkali magmas from trachybasaltic melts. Accordingly, the δ18O variability and the trace element content of the studied minerals suggest possible contamination of primary melts by an O-isotope enriched, REE-poor contaminant like the limestone of Vesuvius basement. Low, nearly primitive δ18O values are observed for olivine from Pompeii eruption, although still above the range of typical mantle minerals. The δ18Oolivine and δ18Ocpxof the minerals from all the studied eruptions define variable degrees of carbonate interaction and magma crystallization for the different eruptions, and possibly within the same eruption, and show evidence of oxygen isotope equilibrium at high temperature. However, energy-constrained AFC model suggest that carbonate assimilation was limited. On the basis of our data, we suggest that interaction between magma and a fluxing, decarbonation-derived CO2 fluid may be partly accounted for the measured O-isotope compositions.","internal_url":"https://www.academia.edu/7794657/Oxygen_isotope_geochemistry_of_mafic_magmas_at_Mt_Vesuvius","translated_internal_url":"","created_at":"2014-07-27T18:57:42.704-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":14420859,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":18172544,"work_id":7794657,"tagging_user_id":14420859,"tagged_user_id":null,"co_author_invite_id":298986,"email":"r***i@unica.it","display_order":0,"name":"Raffaello Cioni","title":"Oxygen isotope geochemistry of mafic magmas at Mt. 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Vesuvius volcanic products contain mafic minerals consisting of High-Fo olivine and Diopsidic Pyroxene. These phases were crystallized in unerupted trachibasaltic to tephritic magmas, and were brought to surface by large phonolitic/tephri-phonolitic (e.g. Avellino and Pompei) and/or of tephritic and phono-tephritic (Pollena) eruptions. A large set of these mm-sized crystals was accurately separated from selected juvenile material and measured for their chemical compositions (EPMA, Laser Ablation ICP-MS) and 18O/16O ratios (conventional laser fluorination) to constrain the nature and evolution of the primary magmas at Mt. Vesuvius. Uncontaminated mantle δ18O values are hardly recovered in Italian Quaternary magmas, mostly due to the widespread occurrence of crustal contamination of the primary melts during their ascent to the surface (e.g. Alban Hills, Ernici Mts., and Aeolian Islands). At Mt. Vesuvius, measured olivine and clinopyroxene share quite homogeneous chemical compositions (Olivine Fo 85-90 ; Diopside En 45-48, respectively), and represent phases crystallized in near primary mafic magmas. Trace element composition constrains the near primary nature of the phases. Published data on volatile content of melt inclusions hosted in these crystals reveal the coexistence of dissolved water and carbon dioxide, and a minimum trapping pressure around 200-300 MPa, suggesting that crystal growth occurred in a reservoir at about 8-10 km depth. Recently, experimental data have suggested massive carbonate assimilation (up to about 20%) to derive potassic alkali magmas from trachybasaltic melts. Accordingly, the δ18O variability and the trace element content of the studied minerals suggest possible contamination of primary melts by an O-isotope enriched, REE-poor contaminant like the limestone of Vesuvius basement. Low, nearly primitive δ18O values are observed for olivine from Pompeii eruption, although still above the range of typical mantle minerals. The δ18Oolivine and δ18Ocpxof the minerals from all the studied eruptions define variable degrees of carbonate interaction and magma crystallization for the different eruptions, and possibly within the same eruption, and show evidence of oxygen isotope equilibrium at high temperature. However, energy-constrained AFC model suggest that carbonate assimilation was limited. On the basis of our data, we suggest that interaction between magma and a fluxing, decarbonation-derived CO2 fluid may be partly accounted for the measured O-isotope compositions.","impression_tracking_id":null,"owner":{"id":14420859,"first_name":"Claudia","middle_initials":null,"last_name":"D'Oriano","page_name":"CDOriano","domain_name":"ingv","created_at":"2014-07-27T18:56:54.386-07:00","display_name":"Claudia D'Oriano","url":"https://ingv.academia.edu/CDOriano"},"attachments":[{"id":48339158,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/48339158/thumbnails/1.jpg","file_name":"Oxygen_isotope_geochemistry_of_mafic_mag20160826-2946-al5ixx.pdf","download_url":"https://www.academia.edu/attachments/48339158/download_file","bulk_download_file_name":"Oxygen_isotope_geochemistry_of_mafic_mag.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/48339158/Oxygen_isotope_geochemistry_of_mafic_mag20160826-2946-al5ixx-libre.pdf?1472233363=\u0026response-content-disposition=attachment%3B+filename%3DOxygen_isotope_geochemistry_of_mafic_mag.pdf\u0026Expires=1743974711\u0026Signature=ASUTIw7f0DBbBXMrLufDmHyrfkmCmLOCuWdWYcEFlwaAa0ofDhUhJAuQ~O~tDflNfhnd~owHmPsPIAFBFqYSNmvy4HqbPOQineNpdTl30saSpDR6hUMxx-tx22INmO6I5IcBTegGGsg6MFVHAaUNta9qjIhjPNXunHxALLMHvBARIqbz~sdRwzA8nhyRiFI7cYCOWdvbx9xIJljjmId2XysKKZn5FD2GobSGnXcCz2ePpMBjGtnlC3sppu~e3r1-VK0pg91wzfFO9n3u72nvL2F-tx2ezww-pxmwXyZOiTAEuFPtCfyR4jBZawcQbXONJaBvOw3gk~hCC2gc7FPnaA__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":30929,"name":"Eruption Mechanisms","url":"https://www.academia.edu/Documents/in/Eruption_Mechanisms"},{"id":78128,"name":"Vesuvius","url":"https://www.academia.edu/Documents/in/Vesuvius"},{"id":230706,"name":"Volcanic degassing","url":"https://www.academia.edu/Documents/in/Volcanic_degassing"}],"urls":[{"id":3249161,"url":"http://adsabs.harvard.edu/abs/2010EGUGA..1211515D"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-7794657-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="7794655"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/7794655/Carbonate_derived_CO2_purging_magma_at_depth_Influence_on_the_eruptive_activity_of_Somma_Vesuvius_Italy"><img alt="Research paper thumbnail of Carbonate-derived CO2 purging magma at depth: Influence on the eruptive activity of Somma-Vesuvius, Italy" class="work-thumbnail" src="https://attachments.academia-assets.com/48339149/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/7794655/Carbonate_derived_CO2_purging_magma_at_depth_Influence_on_the_eruptive_activity_of_Somma_Vesuvius_Italy">Carbonate-derived CO2 purging magma at depth: Influence on the eruptive activity of Somma-Vesuvius, Italy</a></div><div class="wp-workCard_item"><span>Earth and Planetary Science Letters</span><span>, 2011</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Mafic phenocrysts from selected products of the last 4 ka volcanic activity at Mt. Vesuvius were ...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Mafic phenocrysts from selected products of the last 4 ka volcanic activity at Mt. Vesuvius were investigated for their chemical and O-isotope composition, as a proxy for primary magmas feeding the system. 18O/ 16O ratios of studied Mg-rich olivines suggest that near-primary shoshonitic to tephritic melts experienced a flux of sedimentary carbonate-derived CO 2, representing the early process of magma contamination in the roots of the volcanic structure. Bulk carbonate assimilation (physical digestion) mainly occurred in the shallow crust, strongly influencing magma chamber evolution. On a petrological and geochemical basis the effects of bulk sedimentary carbonate digestion on the chemical composition of the near-primary melts are resolved from those of carbonate-released CO 2 fluxed into magma. An important outcome of this process lies in the effect of external CO 2 in changing the overall volatile solubility of the magma, enhancing the ability of Vesuvius mafic magmas to rapidly rise and explosively erupt at the surface.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="0ba8df901faeaf925b0a3c91f538412e" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":48339149,"asset_id":7794655,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/48339149/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="7794655"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="7794655"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 7794655; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=7794655]").text(description); $(".js-view-count[data-work-id=7794655]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 7794655; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='7794655']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "0ba8df901faeaf925b0a3c91f538412e" } } $('.js-work-strip[data-work-id=7794655]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":7794655,"title":"Carbonate-derived CO2 purging magma at depth: Influence on the eruptive activity of Somma-Vesuvius, Italy","translated_title":"","metadata":{"abstract":"Mafic phenocrysts from selected products of the last 4 ka volcanic activity at Mt. Vesuvius were investigated for their chemical and O-isotope composition, as a proxy for primary magmas feeding the system. 18O/ 16O ratios of studied Mg-rich olivines suggest that near-primary shoshonitic to tephritic melts experienced a flux of sedimentary carbonate-derived CO 2, representing the early process of magma contamination in the roots of the volcanic structure. Bulk carbonate assimilation (physical digestion) mainly occurred in the shallow crust, strongly influencing magma chamber evolution. On a petrological and geochemical basis the effects of bulk sedimentary carbonate digestion on the chemical composition of the near-primary melts are resolved from those of carbonate-released CO 2 fluxed into magma. An important outcome of this process lies in the effect of external CO 2 in changing the overall volatile solubility of the magma, enhancing the ability of Vesuvius mafic magmas to rapidly rise and explosively erupt at the surface.","ai_title_tag":"Influence of Carbonate-derived CO2 on Vesuvius Eruptions","publication_date":{"day":null,"month":null,"year":2011,"errors":{}},"publication_name":"Earth and Planetary Science Letters"},"translated_abstract":"Mafic phenocrysts from selected products of the last 4 ka volcanic activity at Mt. Vesuvius were investigated for their chemical and O-isotope composition, as a proxy for primary magmas feeding the system. 18O/ 16O ratios of studied Mg-rich olivines suggest that near-primary shoshonitic to tephritic melts experienced a flux of sedimentary carbonate-derived CO 2, representing the early process of magma contamination in the roots of the volcanic structure. Bulk carbonate assimilation (physical digestion) mainly occurred in the shallow crust, strongly influencing magma chamber evolution. On a petrological and geochemical basis the effects of bulk sedimentary carbonate digestion on the chemical composition of the near-primary melts are resolved from those of carbonate-released CO 2 fluxed into magma. An important outcome of this process lies in the effect of external CO 2 in changing the overall volatile solubility of the magma, enhancing the ability of Vesuvius mafic magmas to rapidly rise and explosively erupt at the surface.","internal_url":"https://www.academia.edu/7794655/Carbonate_derived_CO2_purging_magma_at_depth_Influence_on_the_eruptive_activity_of_Somma_Vesuvius_Italy","translated_internal_url":"","created_at":"2014-07-27T18:57:27.461-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":14420859,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":18172527,"work_id":7794655,"tagging_user_id":14420859,"tagged_user_id":null,"co_author_invite_id":2805600,"email":"c***i@igg.cnr.it","display_order":0,"name":"Chiara Boschi","title":"Carbonate-derived CO2 purging magma at depth: Influence on the eruptive activity of Somma-Vesuvius, Italy"},{"id":18172530,"work_id":7794655,"tagging_user_id":14420859,"tagged_user_id":null,"co_author_invite_id":1114070,"email":"d***i@igg.cnr.it","display_order":4194304,"name":"Luigi Dallai","title":"Carbonate-derived CO2 purging magma at depth: Influence on the eruptive activity of Somma-Vesuvius, Italy"},{"id":18172536,"work_id":7794655,"tagging_user_id":14420859,"tagged_user_id":32521915,"co_author_invite_id":null,"email":"r***i@unifi.it","display_order":6291456,"name":"R. 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Vesuvius were investigated for their chemical and O-isotope composition, as a proxy for primary magmas feeding the system. 18O/ 16O ratios of studied Mg-rich olivines suggest that near-primary shoshonitic to tephritic melts experienced a flux of sedimentary carbonate-derived CO 2, representing the early process of magma contamination in the roots of the volcanic structure. Bulk carbonate assimilation (physical digestion) mainly occurred in the shallow crust, strongly influencing magma chamber evolution. On a petrological and geochemical basis the effects of bulk sedimentary carbonate digestion on the chemical composition of the near-primary melts are resolved from those of carbonate-released CO 2 fluxed into magma. An important outcome of this process lies in the effect of external CO 2 in changing the overall volatile solubility of the magma, enhancing the ability of Vesuvius mafic magmas to rapidly rise and explosively erupt at the surface.","impression_tracking_id":null,"owner":{"id":14420859,"first_name":"Claudia","middle_initials":null,"last_name":"D'Oriano","page_name":"CDOriano","domain_name":"ingv","created_at":"2014-07-27T18:56:54.386-07:00","display_name":"Claudia D'Oriano","url":"https://ingv.academia.edu/CDOriano"},"attachments":[{"id":48339149,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/48339149/thumbnails/1.jpg","file_name":"Carbonate-derived_CO_2_purging_magma_at_20160826-6034-bsxcdt.pdf","download_url":"https://www.academia.edu/attachments/48339149/download_file","bulk_download_file_name":"Carbonate_derived_CO2_purging_magma_at_d.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/48339149/Carbonate-derived_CO_2_purging_magma_at_20160826-6034-bsxcdt-libre.pdf?1472233364=\u0026response-content-disposition=attachment%3B+filename%3DCarbonate_derived_CO2_purging_magma_at_d.pdf\u0026Expires=1743974711\u0026Signature=OPMky2WeW7q31r3QMeHOCqs-uwWKUuHXZfLGsRgjafnrZfL0OK391-9cHb9Xqs6GC0sxs4J5~gIYOyMsY~LkaA6Kv2uJRPpYVTH9eZ4q5-~BpZznSiPiOmsffwFOzEpeHo41N6WGcwZFP71ibhqEXB2Ggj3mTku8SAeJGD6gML6cFIEgiqoQIty9HWvJ8pX0UHdI8CCMnptaZfc9~0GCW4mC9NZ1ysIZif85GPaJMkN-T9hkEAnYdCWXdxDbhFSurI9QXYnrIikowvHt6cmh--~FmhuVF8tMGEMWo2iqDShDG5zg87M3NXPQD~ppnhqxPoATo7Bx3CtASYNmsvqf9Q__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":7959,"name":"Stable Isotope Geochemistry","url":"https://www.academia.edu/Documents/in/Stable_Isotope_Geochemistry"},{"id":230706,"name":"Volcanic degassing","url":"https://www.academia.edu/Documents/in/Volcanic_degassing"}],"urls":[{"id":3249159,"url":"http://adsabs.harvard.edu/abs/2011E\u0026PSL.310...84D"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-7794655-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="7794654"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/7794654/Simulating_intracrater_ash_recycling_during_mid_intensity_explosive_activity_high_temperature_laboratory_experiments_on_natural_basaltic_ash"><img alt="Research paper thumbnail of Simulating intracrater ash recycling during mid-intensity explosive activity: high temperature laboratory experiments on natural basaltic ash" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title">Simulating intracrater ash recycling during mid-intensity explosive activity: high temperature laboratory experiments on natural basaltic ash</div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Direct observations of mid-intensity eruptions, in which a huge amount of ash is generated, indic...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Direct observations of mid-intensity eruptions, in which a huge amount of ash is generated, indicate that ash recycling is quite common. The recognition of juvenile vs. recycled fragments is not straightforward, and no unequivocal, widely accepted criteria exist to support this. The presence of recycled glassy fragments can hide primary magmatic information, introducing bias in the interpretations of the ongoing magmatic and volcanic activity. High temperature experiments were performed at atmospheric pressure on natural samples to investigate the effects of reheating on morphology, texture and composition of volcanic ash. Experiments simulate the transformation of juvenile glassy fragments that, falling into the crater or in the upper part of the conduit, are recycled by following explosions. Textural and compositional modifications obtained in laboratory are compared with similar features observed in natural samples in order to identify some main general criteria to be used for the discrimination of recycled material. Experiments were carried out on tephra produced during Strombolian activity, fire fountains and continuous ash emission at Etna, Stromboli and Vesuvius. Coarse glassy clasts were crushed in a nylon mortar in order to create an artificial ash, and then sieved to select the size interval of 1-0.71 mm. Ash shards were put in a sealed or open quartz tube, in order to prevent or to reproduce effects of air oxidation. The tube was suspended in a HT furnace at INGV-Pisa and kept at different temperatures (up to to 1110°C) for increasing time (0.5-12 hours). Preliminary experiments were also performed under gas flux conditions. Optical and electron microscope observations indicate that high temperature and exposure to the air induce large modifications on clast surface, ranging from change in color, to incipient plastic deformation till complete sintering. Significant change in color of clasts is strictly related to the presence of air, irrespective of temperature while sintering is favored by the high temperature and low fO2. Re-heating promotes nucleation and growth of crystals in the groundmass and associated change of glass composition, sometimes accompanied by growth and coalescence of vesicles in the size of 10-50 µm and cracking of the external surface.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="7794654"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="7794654"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 7794654; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=7794654]").text(description); $(".js-view-count[data-work-id=7794654]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 7794654; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='7794654']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=7794654]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":7794654,"title":"Simulating intracrater ash recycling during mid-intensity explosive activity: high temperature laboratory experiments on natural basaltic ash","translated_title":"","metadata":{"abstract":"Direct observations of mid-intensity eruptions, in which a huge amount of ash is generated, indicate that ash recycling is quite common. The recognition of juvenile vs. recycled fragments is not straightforward, and no unequivocal, widely accepted criteria exist to support this. The presence of recycled glassy fragments can hide primary magmatic information, introducing bias in the interpretations of the ongoing magmatic and volcanic activity. High temperature experiments were performed at atmospheric pressure on natural samples to investigate the effects of reheating on morphology, texture and composition of volcanic ash. Experiments simulate the transformation of juvenile glassy fragments that, falling into the crater or in the upper part of the conduit, are recycled by following explosions. Textural and compositional modifications obtained in laboratory are compared with similar features observed in natural samples in order to identify some main general criteria to be used for the discrimination of recycled material. Experiments were carried out on tephra produced during Strombolian activity, fire fountains and continuous ash emission at Etna, Stromboli and Vesuvius. Coarse glassy clasts were crushed in a nylon mortar in order to create an artificial ash, and then sieved to select the size interval of 1-0.71 mm. Ash shards were put in a sealed or open quartz tube, in order to prevent or to reproduce effects of air oxidation. The tube was suspended in a HT furnace at INGV-Pisa and kept at different temperatures (up to to 1110°C) for increasing time (0.5-12 hours). Preliminary experiments were also performed under gas flux conditions. Optical and electron microscope observations indicate that high temperature and exposure to the air induce large modifications on clast surface, ranging from change in color, to incipient plastic deformation till complete sintering. Significant change in color of clasts is strictly related to the presence of air, irrespective of temperature while sintering is favored by the high temperature and low fO2. Re-heating promotes nucleation and growth of crystals in the groundmass and associated change of glass composition, sometimes accompanied by growth and coalescence of vesicles in the size of 10-50 µm and cracking of the external surface.","publication_date":{"day":null,"month":null,"year":2010,"errors":{}}},"translated_abstract":"Direct observations of mid-intensity eruptions, in which a huge amount of ash is generated, indicate that ash recycling is quite common. The recognition of juvenile vs. recycled fragments is not straightforward, and no unequivocal, widely accepted criteria exist to support this. The presence of recycled glassy fragments can hide primary magmatic information, introducing bias in the interpretations of the ongoing magmatic and volcanic activity. High temperature experiments were performed at atmospheric pressure on natural samples to investigate the effects of reheating on morphology, texture and composition of volcanic ash. Experiments simulate the transformation of juvenile glassy fragments that, falling into the crater or in the upper part of the conduit, are recycled by following explosions. Textural and compositional modifications obtained in laboratory are compared with similar features observed in natural samples in order to identify some main general criteria to be used for the discrimination of recycled material. Experiments were carried out on tephra produced during Strombolian activity, fire fountains and continuous ash emission at Etna, Stromboli and Vesuvius. Coarse glassy clasts were crushed in a nylon mortar in order to create an artificial ash, and then sieved to select the size interval of 1-0.71 mm. Ash shards were put in a sealed or open quartz tube, in order to prevent or to reproduce effects of air oxidation. The tube was suspended in a HT furnace at INGV-Pisa and kept at different temperatures (up to to 1110°C) for increasing time (0.5-12 hours). Preliminary experiments were also performed under gas flux conditions. Optical and electron microscope observations indicate that high temperature and exposure to the air induce large modifications on clast surface, ranging from change in color, to incipient plastic deformation till complete sintering. Significant change in color of clasts is strictly related to the presence of air, irrespective of temperature while sintering is favored by the high temperature and low fO2. Re-heating promotes nucleation and growth of crystals in the groundmass and associated change of glass composition, sometimes accompanied by growth and coalescence of vesicles in the size of 10-50 µm and cracking of the external surface.","internal_url":"https://www.academia.edu/7794654/Simulating_intracrater_ash_recycling_during_mid_intensity_explosive_activity_high_temperature_laboratory_experiments_on_natural_basaltic_ash","translated_internal_url":"","created_at":"2014-07-27T18:57:27.341-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":14420859,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":18172532,"work_id":7794654,"tagging_user_id":14420859,"tagged_user_id":1501609,"co_author_invite_id":null,"email":"p***o@pi.ingv.it","affiliation":"Istituto Nazionale di Geofisica e Vulcanologia","display_order":0,"name":"Massimo Pompilio","title":"Simulating intracrater ash recycling during mid-intensity explosive activity: high temperature laboratory experiments on natural basaltic ash"},{"id":18172540,"work_id":7794654,"tagging_user_id":14420859,"tagged_user_id":36210384,"co_author_invite_id":null,"email":"a***i@ingv.it","display_order":4194304,"name":"A. Bertagnini","title":"Simulating intracrater ash recycling during mid-intensity explosive activity: high temperature laboratory experiments on natural basaltic ash"},{"id":18172543,"work_id":7794654,"tagging_user_id":14420859,"tagged_user_id":null,"co_author_invite_id":298986,"email":"r***i@unica.it","display_order":6291456,"name":"Raffaello Cioni","title":"Simulating intracrater ash recycling during mid-intensity explosive activity: high temperature laboratory experiments on natural basaltic ash"}],"downloadable_attachments":[],"slug":"Simulating_intracrater_ash_recycling_during_mid_intensity_explosive_activity_high_temperature_laboratory_experiments_on_natural_basaltic_ash","translated_slug":"","page_count":null,"language":"en","content_type":"Work","summary":"Direct observations of mid-intensity eruptions, in which a huge amount of ash is generated, indicate that ash recycling is quite common. The recognition of juvenile vs. recycled fragments is not straightforward, and no unequivocal, widely accepted criteria exist to support this. The presence of recycled glassy fragments can hide primary magmatic information, introducing bias in the interpretations of the ongoing magmatic and volcanic activity. High temperature experiments were performed at atmospheric pressure on natural samples to investigate the effects of reheating on morphology, texture and composition of volcanic ash. Experiments simulate the transformation of juvenile glassy fragments that, falling into the crater or in the upper part of the conduit, are recycled by following explosions. Textural and compositional modifications obtained in laboratory are compared with similar features observed in natural samples in order to identify some main general criteria to be used for the discrimination of recycled material. Experiments were carried out on tephra produced during Strombolian activity, fire fountains and continuous ash emission at Etna, Stromboli and Vesuvius. Coarse glassy clasts were crushed in a nylon mortar in order to create an artificial ash, and then sieved to select the size interval of 1-0.71 mm. Ash shards were put in a sealed or open quartz tube, in order to prevent or to reproduce effects of air oxidation. The tube was suspended in a HT furnace at INGV-Pisa and kept at different temperatures (up to to 1110°C) for increasing time (0.5-12 hours). Preliminary experiments were also performed under gas flux conditions. Optical and electron microscope observations indicate that high temperature and exposure to the air induce large modifications on clast surface, ranging from change in color, to incipient plastic deformation till complete sintering. Significant change in color of clasts is strictly related to the presence of air, irrespective of temperature while sintering is favored by the high temperature and low fO2. Re-heating promotes nucleation and growth of crystals in the groundmass and associated change of glass composition, sometimes accompanied by growth and coalescence of vesicles in the size of 10-50 µm and cracking of the external surface.","impression_tracking_id":null,"owner":{"id":14420859,"first_name":"Claudia","middle_initials":null,"last_name":"D'Oriano","page_name":"CDOriano","domain_name":"ingv","created_at":"2014-07-27T18:56:54.386-07:00","display_name":"Claudia D'Oriano","url":"https://ingv.academia.edu/CDOriano"},"attachments":[],"research_interests":[{"id":1370,"name":"Volcanology","url":"https://www.academia.edu/Documents/in/Volcanology"},{"id":10251,"name":"Experimental Petrology","url":"https://www.academia.edu/Documents/in/Experimental_Petrology"}],"urls":[{"id":3249158,"url":"http://adsabs.harvard.edu/abs/2010EGUGA..12.4403D"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-7794654-figures'); } }); </script> </div><div class="profile--tab_content_container js-tab-pane tab-pane" data-section-id="1656079" id="papers"><div class="js-work-strip profile--work_container" data-work-id="23855003"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/23855003/Magmatic_processes_revealed_by_textural_and_compositional_features_of_large_anorthoclase_crystals_from_the_Lajes_Angra_Ignimbrite_Terceira_Island_Azores_"><img alt="Research paper thumbnail of Magmatic processes revealed by textural and compositional features of large anorthoclase crystals from the Lajes-Angra Ignimbrite (Terceira Island, Azores)" class="work-thumbnail" src="https://attachments.academia-assets.com/44249626/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/23855003/Magmatic_processes_revealed_by_textural_and_compositional_features_of_large_anorthoclase_crystals_from_the_Lajes_Angra_Ignimbrite_Terceira_Island_Azores_">Magmatic processes revealed by textural and compositional features of large anorthoclase crystals from the Lajes-Angra Ignimbrite (Terceira Island, Azores)</a></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Lajes-Angra Ignimbrite (LAI) is the most recent (around 21 ka) caldera-forming event produced by ...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Lajes-Angra Ignimbrite (LAI) is the most recent (around 21 ka) caldera-forming event produced by Pico Alto volcano at Terceira Island (Azores). Lajes-Angra Ignimbrite Formation comprises two members closely spaced in time: Lajes and Angra. The Lajes member, the most widely distributed throughout the island, was sampled at two sites: 1) at Lajes (type location), in the northern part of the island, where the succession is characterized by a thin crystal-rich basal layer (TERS 17.1) overlaid by a fine-grained welded lapilli-tuff layer and an upper partially welded coarse clast-bearing layer (TERS 17.2); 2) at São Mateus, in the south coast, where the upper layer of the succession is also partially welded (TERS 62.1). Juvenile clasts are comenditic-trachyte in composition and coarsely porphyritic, ranging from highly vesicular pumice to dense vitrophyric clasts. Mineral assemblage mainly consists of anorthoclase (Ab64-70, An<7 mol%), and less abundant olivine (Fo28-45), clinopyroxene (En60-80Fs20-40), ilmenite and magnetite. Phenocrysts of anorthoclase range in size from < 2mm in the crystal-rich basal layer, up to 4-5 mm in the partially welded upper layer. We found that, except for the basal layer, in the other two samples, large crystals of anorthoclase include pockets of highly vesicular melts ( ). Large crystals with similar textures are quite common in trachytic magmas at Pantelleria and in other silicic magmas. In addition to vesicular glass, these crystals also include vesicles not rimmed by glass. The borders of glassy pockets can be both smooth and angular, and usually marked by a line of Fe-rich melt. This melt is enriched in elements that are not admitted into anorthoclase (Ca, Fe, Mg, Ti) and depleted in Si, Al, K and to a lesser extent in Na. The vesicular glass in the pockets is a comendite-trachyte with composition quite similar to that of the matrix glass. Despite the large phenocrysts appear compositionally homogeneous at SEM, the cathodoluminescence imaging spectroscopy reveals complex growing textures. Crystals are patchy-zoned, with resorbed cores and inclusions-free rims (100-300 µm) ( . Preliminary LAM-ICP-MS analyses of anorthoclases highlighted a large trace-element compositional variation, which is also evident at the scale of the single crystal. Our interest is to understand HOW and WHY the large glass pockets-bearing anorthoclases were formed and if they were related to dissolution or rapid growth, during pre-or syn-eruption degassing processes. Textural and geochemical data are used to obtain information on: i) the evolution of the shallow reservoir; ii) relation between magma and crystal mush; iii) syn-eruptive processes of crystallization-induced degassing. Results are discussed in terms of growth mechanisms of crystals and magma dynamics immediately before or during the eruptive event.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="489e23520e7e2de3a5c1c29f3f7bf974" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":44249626,"asset_id":23855003,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/44249626/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="23855003"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="23855003"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 23855003; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=23855003]").text(description); $(".js-view-count[data-work-id=23855003]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 23855003; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='23855003']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "489e23520e7e2de3a5c1c29f3f7bf974" } } $('.js-work-strip[data-work-id=23855003]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":23855003,"title":"Magmatic processes revealed by textural and compositional features of large anorthoclase crystals from the Lajes-Angra Ignimbrite (Terceira Island, Azores)","translated_title":"","metadata":{"grobid_abstract":"Lajes-Angra Ignimbrite (LAI) is the most recent (around 21 ka) caldera-forming event produced by Pico Alto volcano at Terceira Island (Azores). Lajes-Angra Ignimbrite Formation comprises two members closely spaced in time: Lajes and Angra. The Lajes member, the most widely distributed throughout the island, was sampled at two sites: 1) at Lajes (type location), in the northern part of the island, where the succession is characterized by a thin crystal-rich basal layer (TERS 17.1) overlaid by a fine-grained welded lapilli-tuff layer and an upper partially welded coarse clast-bearing layer (TERS 17.2); 2) at São Mateus, in the south coast, where the upper layer of the succession is also partially welded (TERS 62.1). Juvenile clasts are comenditic-trachyte in composition and coarsely porphyritic, ranging from highly vesicular pumice to dense vitrophyric clasts. Mineral assemblage mainly consists of anorthoclase (Ab64-70, An\u003c7 mol%), and less abundant olivine (Fo28-45), clinopyroxene (En60-80Fs20-40), ilmenite and magnetite. Phenocrysts of anorthoclase range in size from \u003c 2mm in the crystal-rich basal layer, up to 4-5 mm in the partially welded upper layer. We found that, except for the basal layer, in the other two samples, large crystals of anorthoclase include pockets of highly vesicular melts ( ). Large crystals with similar textures are quite common in trachytic magmas at Pantelleria and in other silicic magmas. In addition to vesicular glass, these crystals also include vesicles not rimmed by glass. The borders of glassy pockets can be both smooth and angular, and usually marked by a line of Fe-rich melt. This melt is enriched in elements that are not admitted into anorthoclase (Ca, Fe, Mg, Ti) and depleted in Si, Al, K and to a lesser extent in Na. The vesicular glass in the pockets is a comendite-trachyte with composition quite similar to that of the matrix glass. Despite the large phenocrysts appear compositionally homogeneous at SEM, the cathodoluminescence imaging spectroscopy reveals complex growing textures. Crystals are patchy-zoned, with resorbed cores and inclusions-free rims (100-300 µm) ( . Preliminary LAM-ICP-MS analyses of anorthoclases highlighted a large trace-element compositional variation, which is also evident at the scale of the single crystal. Our interest is to understand HOW and WHY the large glass pockets-bearing anorthoclases were formed and if they were related to dissolution or rapid growth, during pre-or syn-eruption degassing processes. Textural and geochemical data are used to obtain information on: i) the evolution of the shallow reservoir; ii) relation between magma and crystal mush; iii) syn-eruptive processes of crystallization-induced degassing. Results are discussed in terms of growth mechanisms of crystals and magma dynamics immediately before or during the eruptive event.","grobid_abstract_attachment_id":44249626},"translated_abstract":null,"internal_url":"https://www.academia.edu/23855003/Magmatic_processes_revealed_by_textural_and_compositional_features_of_large_anorthoclase_crystals_from_the_Lajes_Angra_Ignimbrite_Terceira_Island_Azores_","translated_internal_url":"","created_at":"2016-03-31T00:55:38.427-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":14420859,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":44249626,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/44249626/thumbnails/1.jpg","file_name":"Magmatic_processes_revealed_by_textural_20160331-25224-48c40n.pdf","download_url":"https://www.academia.edu/attachments/44249626/download_file","bulk_download_file_name":"Magmatic_processes_revealed_by_textural.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/44249626/Magmatic_processes_revealed_by_textural_20160331-25224-48c40n-libre.pdf?1459411720=\u0026response-content-disposition=attachment%3B+filename%3DMagmatic_processes_revealed_by_textural.pdf\u0026Expires=1743974704\u0026Signature=WkNPP8yRsBZsdtPwADGGrkjIdHQv9H~Fy27T7-1eL1soApZxAJD3nUrp7DGelwjnC9DnRrZstbiLyecASQ6eGMfBQ~Eu1IilpH~vQ1iaY9wxl5aSB4CKIPVPLh~s2iz8Ju6RE8ziXgplyC98P~BEAmpr2wGIBG9xxUNqdBFq4ROOHg8Mc62Za1VEa1Gk6IO337eW~fB4kMIPsgASoRkPOt5UPnMWqWvyOGou7OiYdXyLByV9i7YHaMQfjer2ktzrvWNjedTXKdysZ86dBmlupBsTUnaXlhpXnQJ9gxPQzHoSOaDtilwjPJWd0cFABHK1hrS2XV1zCNwXgbMZ9M64Pg__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Magmatic_processes_revealed_by_textural_and_compositional_features_of_large_anorthoclase_crystals_from_the_Lajes_Angra_Ignimbrite_Terceira_Island_Azores_","translated_slug":"","page_count":2,"language":"en","content_type":"Work","summary":"Lajes-Angra Ignimbrite (LAI) is the most recent (around 21 ka) caldera-forming event produced by Pico Alto volcano at Terceira Island (Azores). Lajes-Angra Ignimbrite Formation comprises two members closely spaced in time: Lajes and Angra. The Lajes member, the most widely distributed throughout the island, was sampled at two sites: 1) at Lajes (type location), in the northern part of the island, where the succession is characterized by a thin crystal-rich basal layer (TERS 17.1) overlaid by a fine-grained welded lapilli-tuff layer and an upper partially welded coarse clast-bearing layer (TERS 17.2); 2) at São Mateus, in the south coast, where the upper layer of the succession is also partially welded (TERS 62.1). Juvenile clasts are comenditic-trachyte in composition and coarsely porphyritic, ranging from highly vesicular pumice to dense vitrophyric clasts. Mineral assemblage mainly consists of anorthoclase (Ab64-70, An\u003c7 mol%), and less abundant olivine (Fo28-45), clinopyroxene (En60-80Fs20-40), ilmenite and magnetite. Phenocrysts of anorthoclase range in size from \u003c 2mm in the crystal-rich basal layer, up to 4-5 mm in the partially welded upper layer. We found that, except for the basal layer, in the other two samples, large crystals of anorthoclase include pockets of highly vesicular melts ( ). Large crystals with similar textures are quite common in trachytic magmas at Pantelleria and in other silicic magmas. In addition to vesicular glass, these crystals also include vesicles not rimmed by glass. The borders of glassy pockets can be both smooth and angular, and usually marked by a line of Fe-rich melt. This melt is enriched in elements that are not admitted into anorthoclase (Ca, Fe, Mg, Ti) and depleted in Si, Al, K and to a lesser extent in Na. The vesicular glass in the pockets is a comendite-trachyte with composition quite similar to that of the matrix glass. Despite the large phenocrysts appear compositionally homogeneous at SEM, the cathodoluminescence imaging spectroscopy reveals complex growing textures. Crystals are patchy-zoned, with resorbed cores and inclusions-free rims (100-300 µm) ( . Preliminary LAM-ICP-MS analyses of anorthoclases highlighted a large trace-element compositional variation, which is also evident at the scale of the single crystal. Our interest is to understand HOW and WHY the large glass pockets-bearing anorthoclases were formed and if they were related to dissolution or rapid growth, during pre-or syn-eruption degassing processes. Textural and geochemical data are used to obtain information on: i) the evolution of the shallow reservoir; ii) relation between magma and crystal mush; iii) syn-eruptive processes of crystallization-induced degassing. Results are discussed in terms of growth mechanisms of crystals and magma dynamics immediately before or during the eruptive event.","impression_tracking_id":null,"owner":{"id":14420859,"first_name":"Claudia","middle_initials":null,"last_name":"D'Oriano","page_name":"CDOriano","domain_name":"ingv","created_at":"2014-07-27T18:56:54.386-07:00","display_name":"Claudia D'Oriano","url":"https://ingv.academia.edu/CDOriano"},"attachments":[{"id":44249626,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/44249626/thumbnails/1.jpg","file_name":"Magmatic_processes_revealed_by_textural_20160331-25224-48c40n.pdf","download_url":"https://www.academia.edu/attachments/44249626/download_file","bulk_download_file_name":"Magmatic_processes_revealed_by_textural.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/44249626/Magmatic_processes_revealed_by_textural_20160331-25224-48c40n-libre.pdf?1459411720=\u0026response-content-disposition=attachment%3B+filename%3DMagmatic_processes_revealed_by_textural.pdf\u0026Expires=1743974704\u0026Signature=WkNPP8yRsBZsdtPwADGGrkjIdHQv9H~Fy27T7-1eL1soApZxAJD3nUrp7DGelwjnC9DnRrZstbiLyecASQ6eGMfBQ~Eu1IilpH~vQ1iaY9wxl5aSB4CKIPVPLh~s2iz8Ju6RE8ziXgplyC98P~BEAmpr2wGIBG9xxUNqdBFq4ROOHg8Mc62Za1VEa1Gk6IO337eW~fB4kMIPsgASoRkPOt5UPnMWqWvyOGou7OiYdXyLByV9i7YHaMQfjer2ktzrvWNjedTXKdysZ86dBmlupBsTUnaXlhpXnQJ9gxPQzHoSOaDtilwjPJWd0cFABHK1hrS2XV1zCNwXgbMZ9M64Pg__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":1370,"name":"Volcanology","url":"https://www.academia.edu/Documents/in/Volcanology"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-23855003-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="23855002"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/23855002/Dynamics_of_ash_eruptions_at_Vesuvius"><img alt="Research paper thumbnail of Dynamics of ash eruptions at Vesuvius" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title">Dynamics of ash eruptions at Vesuvius</div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">ABSTRACT In the recent years, continuous ash emission activity, related to mid-low intensity, lon...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">ABSTRACT In the recent years, continuous ash emission activity, related to mid-low intensity, long lasting eruptions, has been increasingly described to occur at different volcanoes worldwide. Focusing on this type of deposits, a retrospective analysis of the stratigraphic successions at Vesuvius revealed that such type of eruptions have occurred repeatedly in the last 4000 years of activity. This type of activity has been overlooked in the past and the mechanism of ash production in these eruptions is not yet clear. The detailed study of the deposits suggests that these eruptions are dominated by discrete phases of repeated emission of a highly fragmented mixture, alternated with violent strombolian episodes. In this study we present morphological, textural and compositional data on the products of two ash eruptions representative of the whole variability of this activity at Vesuvius (Italy), occurred in the periods between the “Avellino” and “Pompeii” Pumice eruptions (AP3, 2,710±60 years B.P.) and after the 512 A.D. eruption, (AS1a). Juvenile fragments from different ash layers throughout the studied stratigraphic sections were fully characterized in terms of external morphology, particle outline parameterization, groundmass texture (in terms of Crystal and Vesicle Size Distributions) and glass composition. Volcanic ash holds information about magma dynamics within the volcanic conduit, where fragmentation occurs and eruption style is decided. Results of our investigations have been interpreted in terms of fragmentation processes, transport and dispositional mechanisms, dynamics of magma ascent ant timing of the eruption. The methodology of ash analysis used for this study has also important implications for tephrochronological studies, adding a complete parameterization of physical and textural properties of the ash to the routinely used compositional data.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="23855002"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="23855002"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 23855002; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=23855002]").text(description); $(".js-view-count[data-work-id=23855002]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 23855002; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='23855002']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=23855002]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":23855002,"title":"Dynamics of ash eruptions at Vesuvius","translated_title":"","metadata":{"abstract":"ABSTRACT In the recent years, continuous ash emission activity, related to mid-low intensity, long lasting eruptions, has been increasingly described to occur at different volcanoes worldwide. Focusing on this type of deposits, a retrospective analysis of the stratigraphic successions at Vesuvius revealed that such type of eruptions have occurred repeatedly in the last 4000 years of activity. This type of activity has been overlooked in the past and the mechanism of ash production in these eruptions is not yet clear. The detailed study of the deposits suggests that these eruptions are dominated by discrete phases of repeated emission of a highly fragmented mixture, alternated with violent strombolian episodes. In this study we present morphological, textural and compositional data on the products of two ash eruptions representative of the whole variability of this activity at Vesuvius (Italy), occurred in the periods between the “Avellino” and “Pompeii” Pumice eruptions (AP3, 2,710±60 years B.P.) and after the 512 A.D. eruption, (AS1a). Juvenile fragments from different ash layers throughout the studied stratigraphic sections were fully characterized in terms of external morphology, particle outline parameterization, groundmass texture (in terms of Crystal and Vesicle Size Distributions) and glass composition. Volcanic ash holds information about magma dynamics within the volcanic conduit, where fragmentation occurs and eruption style is decided. Results of our investigations have been interpreted in terms of fragmentation processes, transport and dispositional mechanisms, dynamics of magma ascent ant timing of the eruption. The methodology of ash analysis used for this study has also important implications for tephrochronological studies, adding a complete parameterization of physical and textural properties of the ash to the routinely used compositional data."},"translated_abstract":"ABSTRACT In the recent years, continuous ash emission activity, related to mid-low intensity, long lasting eruptions, has been increasingly described to occur at different volcanoes worldwide. Focusing on this type of deposits, a retrospective analysis of the stratigraphic successions at Vesuvius revealed that such type of eruptions have occurred repeatedly in the last 4000 years of activity. This type of activity has been overlooked in the past and the mechanism of ash production in these eruptions is not yet clear. The detailed study of the deposits suggests that these eruptions are dominated by discrete phases of repeated emission of a highly fragmented mixture, alternated with violent strombolian episodes. In this study we present morphological, textural and compositional data on the products of two ash eruptions representative of the whole variability of this activity at Vesuvius (Italy), occurred in the periods between the “Avellino” and “Pompeii” Pumice eruptions (AP3, 2,710±60 years B.P.) and after the 512 A.D. eruption, (AS1a). Juvenile fragments from different ash layers throughout the studied stratigraphic sections were fully characterized in terms of external morphology, particle outline parameterization, groundmass texture (in terms of Crystal and Vesicle Size Distributions) and glass composition. Volcanic ash holds information about magma dynamics within the volcanic conduit, where fragmentation occurs and eruption style is decided. Results of our investigations have been interpreted in terms of fragmentation processes, transport and dispositional mechanisms, dynamics of magma ascent ant timing of the eruption. The methodology of ash analysis used for this study has also important implications for tephrochronological studies, adding a complete parameterization of physical and textural properties of the ash to the routinely used compositional data.","internal_url":"https://www.academia.edu/23855002/Dynamics_of_ash_eruptions_at_Vesuvius","translated_internal_url":"","created_at":"2016-03-31T00:55:38.231-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":14420859,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[],"slug":"Dynamics_of_ash_eruptions_at_Vesuvius","translated_slug":"","page_count":null,"language":"en","content_type":"Work","summary":"ABSTRACT In the recent years, continuous ash emission activity, related to mid-low intensity, long lasting eruptions, has been increasingly described to occur at different volcanoes worldwide. Focusing on this type of deposits, a retrospective analysis of the stratigraphic successions at Vesuvius revealed that such type of eruptions have occurred repeatedly in the last 4000 years of activity. This type of activity has been overlooked in the past and the mechanism of ash production in these eruptions is not yet clear. The detailed study of the deposits suggests that these eruptions are dominated by discrete phases of repeated emission of a highly fragmented mixture, alternated with violent strombolian episodes. In this study we present morphological, textural and compositional data on the products of two ash eruptions representative of the whole variability of this activity at Vesuvius (Italy), occurred in the periods between the “Avellino” and “Pompeii” Pumice eruptions (AP3, 2,710±60 years B.P.) and after the 512 A.D. eruption, (AS1a). Juvenile fragments from different ash layers throughout the studied stratigraphic sections were fully characterized in terms of external morphology, particle outline parameterization, groundmass texture (in terms of Crystal and Vesicle Size Distributions) and glass composition. Volcanic ash holds information about magma dynamics within the volcanic conduit, where fragmentation occurs and eruption style is decided. Results of our investigations have been interpreted in terms of fragmentation processes, transport and dispositional mechanisms, dynamics of magma ascent ant timing of the eruption. The methodology of ash analysis used for this study has also important implications for tephrochronological studies, adding a complete parameterization of physical and textural properties of the ash to the routinely used compositional data.","impression_tracking_id":null,"owner":{"id":14420859,"first_name":"Claudia","middle_initials":null,"last_name":"D'Oriano","page_name":"CDOriano","domain_name":"ingv","created_at":"2014-07-27T18:56:54.386-07:00","display_name":"Claudia D'Oriano","url":"https://ingv.academia.edu/CDOriano"},"attachments":[],"research_interests":[],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-23855002-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="23855001"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/23855001/And_Their_Impact_on_Human_Activity"><img alt="Research paper thumbnail of And Their Impact on Human Activity" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title">And Their Impact on Human Activity</div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="23855001"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="23855001"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 23855001; 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-23855001-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="23855000"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/23855000/The_2nd_to_4th_century_explosive_activity_of_Vesuvius_new_data_on_the_timing_of_the_upward_migration_of_the_post_AD_79_magma_chamber"><img alt="Research paper thumbnail of The 2nd to 4th century explosive activity of Vesuvius: new data on the timing of the upward migration of the post-AD 79 magma chamber" class="work-thumbnail" src="https://attachments.academia-assets.com/44249622/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/23855000/The_2nd_to_4th_century_explosive_activity_of_Vesuvius_new_data_on_the_timing_of_the_upward_migration_of_the_post_AD_79_magma_chamber">The 2nd to 4th century explosive activity of Vesuvius: new data on the timing of the upward migration of the post-AD 79 magma chamber</a></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">We present volcanological data on the deposits of the Santa Maria Member (SMM), the eruption cycl...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">We present volcanological data on the deposits of the Santa Maria Member (SMM), the eruption cycle occurred at Vesuvius (Italy) in the period between the A.D. 79 plinian and the A.D. 472 subplinan eruptions. Historical accounts report only sporadic, poorly reliable descriptions of the volcanic activity in this period, during which a stratified sequence of ash and lapilli beds, up to 150 cm thick, with a total volume estimated around 0.15 km 3 , was widely dispersed on the outer slopes of the volcano. Stratigraphic studies and component analyses suggest that activity was characterized by mixed hydromagmatic and magmatic processes. The eruption style has been interpreted as repeated alternations of continuous and prolonged ash emission activity intercalated with short-lived, violent strombolian phases. Analyses of the bulk rock composition reveal that during the entire eruption cycle, magma maintained an homogeneous phonotephritic composition. In addition, the general trends of major and trace elements depicted by the products of the A.D. 79 and A.D. 472 eruptions converge to the SMM composition, suggesting a common mafic endmember for these eruptions. The volatile content measured in pyroxene-hosted melt inclusions indicates two main values of crystallization pressures, around 220 and 70 MPa, roughly corresponding to the previously estimated depth of the magma reservoirs of the A.D. 79 and A.D. 472 eruptions, respectively. The study of SMM eruption cycle may thus contribute to understand the processes governing the volcano reawakening immediately after a plinian event, and the timing and modalities which govern the migration of the magma reservoir.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="528c6b7c10a604fdb6197f6cc2ae6be4" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":44249622,"asset_id":23855000,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/44249622/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="23855000"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="23855000"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 23855000; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=23855000]").text(description); $(".js-view-count[data-work-id=23855000]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 23855000; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='23855000']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "528c6b7c10a604fdb6197f6cc2ae6be4" } } $('.js-work-strip[data-work-id=23855000]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":23855000,"title":"The 2nd to 4th century explosive activity of Vesuvius: new data on the timing of the upward migration of the post-AD 79 magma chamber","translated_title":"","metadata":{"ai_title_tag":"Vesuvius Eruption Cycle: Magma Migration Insights","grobid_abstract":"We present volcanological data on the deposits of the Santa Maria Member (SMM), the eruption cycle occurred at Vesuvius (Italy) in the period between the A.D. 79 plinian and the A.D. 472 subplinan eruptions. Historical accounts report only sporadic, poorly reliable descriptions of the volcanic activity in this period, during which a stratified sequence of ash and lapilli beds, up to 150 cm thick, with a total volume estimated around 0.15 km 3 , was widely dispersed on the outer slopes of the volcano. Stratigraphic studies and component analyses suggest that activity was characterized by mixed hydromagmatic and magmatic processes. The eruption style has been interpreted as repeated alternations of continuous and prolonged ash emission activity intercalated with short-lived, violent strombolian phases. Analyses of the bulk rock composition reveal that during the entire eruption cycle, magma maintained an homogeneous phonotephritic composition. In addition, the general trends of major and trace elements depicted by the products of the A.D. 79 and A.D. 472 eruptions converge to the SMM composition, suggesting a common mafic endmember for these eruptions. The volatile content measured in pyroxene-hosted melt inclusions indicates two main values of crystallization pressures, around 220 and 70 MPa, roughly corresponding to the previously estimated depth of the magma reservoirs of the A.D. 79 and A.D. 472 eruptions, respectively. The study of SMM eruption cycle may thus contribute to understand the processes governing the volcano reawakening immediately after a plinian event, and the timing and modalities which govern the migration of the magma reservoir.","grobid_abstract_attachment_id":44249622},"translated_abstract":null,"internal_url":"https://www.academia.edu/23855000/The_2nd_to_4th_century_explosive_activity_of_Vesuvius_new_data_on_the_timing_of_the_upward_migration_of_the_post_AD_79_magma_chamber","translated_internal_url":"","created_at":"2016-03-31T00:55:37.861-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":14420859,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":44249622,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/44249622/thumbnails/1.jpg","file_name":"The_2nd_to_4th_century_explosive_activit20160331-24641-11cmds5.pdf","download_url":"https://www.academia.edu/attachments/44249622/download_file","bulk_download_file_name":"The_2nd_to_4th_century_explosive_activit.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/44249622/The_2nd_to_4th_century_explosive_activit20160331-24641-11cmds5-libre.pdf?1459411722=\u0026response-content-disposition=attachment%3B+filename%3DThe_2nd_to_4th_century_explosive_activit.pdf\u0026Expires=1743974706\u0026Signature=E6ZRrFYF38TFP5Uz2~SWL3iP-9q0ahfUl3dqNShqSWiFQ1iLTJAmw6BsRnYediY7N4hCkzRL5uRQ4hRhHel-4sr14bMav7P4RS5Zscz4IzA-QR0nTAPqx4~I2gHZvf9SdEn-QVO63bQcCE4l396WtfsLLgYUpRVmIyf~gZ6zbczx0Ao0wRgx0Hq-Py4erLbUc0T4HNg~5NQFvNGmypaASxf1ysaqXcihLLextjYgMjdU5sT6YbIvpGKdDJWqTiN-pbXQwB7qjPQkAB0xSoT58WTpnwJx6TG4e8PRbiMydvaI1qhgCYIHOdRMCaW-Vo1MVd3WKqEP5vOppZNju1H5UQ__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"The_2nd_to_4th_century_explosive_activity_of_Vesuvius_new_data_on_the_timing_of_the_upward_migration_of_the_post_AD_79_magma_chamber","translated_slug":"","page_count":17,"language":"en","content_type":"Work","summary":"We present volcanological data on the deposits of the Santa Maria Member (SMM), the eruption cycle occurred at Vesuvius (Italy) in the period between the A.D. 79 plinian and the A.D. 472 subplinan eruptions. Historical accounts report only sporadic, poorly reliable descriptions of the volcanic activity in this period, during which a stratified sequence of ash and lapilli beds, up to 150 cm thick, with a total volume estimated around 0.15 km 3 , was widely dispersed on the outer slopes of the volcano. Stratigraphic studies and component analyses suggest that activity was characterized by mixed hydromagmatic and magmatic processes. The eruption style has been interpreted as repeated alternations of continuous and prolonged ash emission activity intercalated with short-lived, violent strombolian phases. Analyses of the bulk rock composition reveal that during the entire eruption cycle, magma maintained an homogeneous phonotephritic composition. In addition, the general trends of major and trace elements depicted by the products of the A.D. 79 and A.D. 472 eruptions converge to the SMM composition, suggesting a common mafic endmember for these eruptions. The volatile content measured in pyroxene-hosted melt inclusions indicates two main values of crystallization pressures, around 220 and 70 MPa, roughly corresponding to the previously estimated depth of the magma reservoirs of the A.D. 79 and A.D. 472 eruptions, respectively. The study of SMM eruption cycle may thus contribute to understand the processes governing the volcano reawakening immediately after a plinian event, and the timing and modalities which govern the migration of the magma reservoir.","impression_tracking_id":null,"owner":{"id":14420859,"first_name":"Claudia","middle_initials":null,"last_name":"D'Oriano","page_name":"CDOriano","domain_name":"ingv","created_at":"2014-07-27T18:56:54.386-07:00","display_name":"Claudia D'Oriano","url":"https://ingv.academia.edu/CDOriano"},"attachments":[{"id":44249622,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/44249622/thumbnails/1.jpg","file_name":"The_2nd_to_4th_century_explosive_activit20160331-24641-11cmds5.pdf","download_url":"https://www.academia.edu/attachments/44249622/download_file","bulk_download_file_name":"The_2nd_to_4th_century_explosive_activit.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/44249622/The_2nd_to_4th_century_explosive_activit20160331-24641-11cmds5-libre.pdf?1459411722=\u0026response-content-disposition=attachment%3B+filename%3DThe_2nd_to_4th_century_explosive_activit.pdf\u0026Expires=1743974706\u0026Signature=E6ZRrFYF38TFP5Uz2~SWL3iP-9q0ahfUl3dqNShqSWiFQ1iLTJAmw6BsRnYediY7N4hCkzRL5uRQ4hRhHel-4sr14bMav7P4RS5Zscz4IzA-QR0nTAPqx4~I2gHZvf9SdEn-QVO63bQcCE4l396WtfsLLgYUpRVmIyf~gZ6zbczx0Ao0wRgx0Hq-Py4erLbUc0T4HNg~5NQFvNGmypaASxf1ysaqXcihLLextjYgMjdU5sT6YbIvpGKdDJWqTiN-pbXQwB7qjPQkAB0xSoT58WTpnwJx6TG4e8PRbiMydvaI1qhgCYIHOdRMCaW-Vo1MVd3WKqEP5vOppZNju1H5UQ__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":409,"name":"Geophysics","url":"https://www.academia.edu/Documents/in/Geophysics"},{"id":1034,"name":"Stratigraphy","url":"https://www.academia.edu/Documents/in/Stratigraphy"},{"id":78128,"name":"Vesuvius","url":"https://www.academia.edu/Documents/in/Vesuvius"},{"id":200887,"name":"Explosive volcanic eruptions","url":"https://www.academia.edu/Documents/in/Explosive_volcanic_eruptions"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-23855000-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="23854999"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/23854999/The_onset_of_an_eruption_selective_assimilation_of_hydrothermal_minerals_during_the_opening_phase_of_the_2010_summit_eruption_of_Eyjafjallaj%C3%B6kull_volcano_Iceland"><img alt="Research paper thumbnail of The onset of an eruption: selective assimilation of hydrothermal minerals during the opening phase of the 2010 summit eruption of Eyjafjallajökull volcano, Iceland" class="work-thumbnail" src="https://attachments.academia-assets.com/44249621/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/23854999/The_onset_of_an_eruption_selective_assimilation_of_hydrothermal_minerals_during_the_opening_phase_of_the_2010_summit_eruption_of_Eyjafjallaj%C3%B6kull_volcano_Iceland">The onset of an eruption: selective assimilation of hydrothermal minerals during the opening phase of the 2010 summit eruption of Eyjafjallajökull volcano, Iceland</a></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">The 2010 summit eruption of Eyjafjallajökull volcano (Iceland) started on 14 April and continued ...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">The 2010 summit eruption of Eyjafjallajökull volcano (Iceland) started on 14 April and continued for 39 days. The whole duration of the activity can be divided into different phases, characterized by variable intensity and eruption dynamics. The opening stage of the eruption, in particular, lasted few hours, during which the magma intruded into the glacier, melting the ice to the surface. In this subglacial stage the activity was dominated by the emission of ash-poor, vapour-rich clouds, with the sedimentation of a very thin ash layer in the very proximal area. The intensity of the summit eruption gradually increased during the day, and culminated with the emergence of a 9-10 km high, dark ash-laden plume, which continued, with variable intensity, until 18 April. We focus here on the opening stage of the event (first 3-4 hours), which represents a unique opportunity to investigate the immediately pre-eruptive dynamics .</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="6c28c15cc7e42209a4de1cded46334e8" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":44249621,"asset_id":23854999,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/44249621/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="23854999"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="23854999"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 23854999; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=23854999]").text(description); $(".js-view-count[data-work-id=23854999]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 23854999; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='23854999']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "6c28c15cc7e42209a4de1cded46334e8" } } $('.js-work-strip[data-work-id=23854999]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":23854999,"title":"The onset of an eruption: selective assimilation of hydrothermal minerals during the opening phase of the 2010 summit eruption of Eyjafjallajökull volcano, Iceland","translated_title":"","metadata":{"grobid_abstract":"The 2010 summit eruption of Eyjafjallajökull volcano (Iceland) started on 14 April and continued for 39 days. The whole duration of the activity can be divided into different phases, characterized by variable intensity and eruption dynamics. The opening stage of the eruption, in particular, lasted few hours, during which the magma intruded into the glacier, melting the ice to the surface. In this subglacial stage the activity was dominated by the emission of ash-poor, vapour-rich clouds, with the sedimentation of a very thin ash layer in the very proximal area. The intensity of the summit eruption gradually increased during the day, and culminated with the emergence of a 9-10 km high, dark ash-laden plume, which continued, with variable intensity, until 18 April. We focus here on the opening stage of the event (first 3-4 hours), which represents a unique opportunity to investigate the immediately pre-eruptive dynamics .","grobid_abstract_attachment_id":44249621},"translated_abstract":null,"internal_url":"https://www.academia.edu/23854999/The_onset_of_an_eruption_selective_assimilation_of_hydrothermal_minerals_during_the_opening_phase_of_the_2010_summit_eruption_of_Eyjafjallaj%C3%B6kull_volcano_Iceland","translated_internal_url":"","created_at":"2016-03-31T00:55:37.660-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":14420859,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":44249621,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/44249621/thumbnails/1.jpg","file_name":"The_onset_of_an_eruption_selective_assim20160331-30246-mm74ls.pdf","download_url":"https://www.academia.edu/attachments/44249621/download_file","bulk_download_file_name":"The_onset_of_an_eruption_selective_assim.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/44249621/The_onset_of_an_eruption_selective_assim20160331-30246-mm74ls-libre.pdf?1459411720=\u0026response-content-disposition=attachment%3B+filename%3DThe_onset_of_an_eruption_selective_assim.pdf\u0026Expires=1743974706\u0026Signature=ULYlmps6JyxGmd~EU~J0GvSFqtogWfThQ49PclpJGtgNG74TwKzh~Xq72rsM4hMpl3KEzu-pQzLqNGru3swtlj6NR8XaBeHS7y3E41mq9ahk1bTs8lWPoae4mn6KLV7jmWYbqFzAI68qzIri52sYE2zTmXSsiGWVbWHLw~uLzXobtIXWhr8Gnj3sVO7NsJFhQeMc4JSD9weARadHUrv6IG3U8kEthQyJ30mYR28bruj7DFLFojIhaiqCTV93zIPhbg7nc5itYJVdvCFydnTDH7EUwBoV6eSDGbsgxEZLeHi4LHUbFcrkpcCKqKAjCgb4ZKRJCHp0vPz75WzhDPTUxw__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"The_onset_of_an_eruption_selective_assimilation_of_hydrothermal_minerals_during_the_opening_phase_of_the_2010_summit_eruption_of_Eyjafjallajökull_volcano_Iceland","translated_slug":"","page_count":2,"language":"en","content_type":"Work","summary":"The 2010 summit eruption of Eyjafjallajökull volcano (Iceland) started on 14 April and continued for 39 days. The whole duration of the activity can be divided into different phases, characterized by variable intensity and eruption dynamics. The opening stage of the eruption, in particular, lasted few hours, during which the magma intruded into the glacier, melting the ice to the surface. In this subglacial stage the activity was dominated by the emission of ash-poor, vapour-rich clouds, with the sedimentation of a very thin ash layer in the very proximal area. The intensity of the summit eruption gradually increased during the day, and culminated with the emergence of a 9-10 km high, dark ash-laden plume, which continued, with variable intensity, until 18 April. We focus here on the opening stage of the event (first 3-4 hours), which represents a unique opportunity to investigate the immediately pre-eruptive dynamics .","impression_tracking_id":null,"owner":{"id":14420859,"first_name":"Claudia","middle_initials":null,"last_name":"D'Oriano","page_name":"CDOriano","domain_name":"ingv","created_at":"2014-07-27T18:56:54.386-07:00","display_name":"Claudia D'Oriano","url":"https://ingv.academia.edu/CDOriano"},"attachments":[{"id":44249621,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/44249621/thumbnails/1.jpg","file_name":"The_onset_of_an_eruption_selective_assim20160331-30246-mm74ls.pdf","download_url":"https://www.academia.edu/attachments/44249621/download_file","bulk_download_file_name":"The_onset_of_an_eruption_selective_assim.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/44249621/The_onset_of_an_eruption_selective_assim20160331-30246-mm74ls-libre.pdf?1459411720=\u0026response-content-disposition=attachment%3B+filename%3DThe_onset_of_an_eruption_selective_assim.pdf\u0026Expires=1743974706\u0026Signature=ULYlmps6JyxGmd~EU~J0GvSFqtogWfThQ49PclpJGtgNG74TwKzh~Xq72rsM4hMpl3KEzu-pQzLqNGru3swtlj6NR8XaBeHS7y3E41mq9ahk1bTs8lWPoae4mn6KLV7jmWYbqFzAI68qzIri52sYE2zTmXSsiGWVbWHLw~uLzXobtIXWhr8Gnj3sVO7NsJFhQeMc4JSD9weARadHUrv6IG3U8kEthQyJ30mYR28bruj7DFLFojIhaiqCTV93zIPhbg7nc5itYJVdvCFydnTDH7EUwBoV6eSDGbsgxEZLeHi4LHUbFcrkpcCKqKAjCgb4ZKRJCHp0vPz75WzhDPTUxw__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-23854999-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="23854998"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/23854998/Past_and_present_mid_intensity_explosive_eruptions_of_Italian_volcanoes_and_their_impact_on_human_activity"><img alt="Research paper thumbnail of Past and present mid-intensity explosive eruptions of Italian volcanoes and their impact on human activity" class="work-thumbnail" src="https://attachments.academia-assets.com/44249624/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/23854998/Past_and_present_mid_intensity_explosive_eruptions_of_Italian_volcanoes_and_their_impact_on_human_activity">Past and present mid-intensity explosive eruptions of Italian volcanoes and their impact on human activity</a></div><div class="wp-workCard_item"><span>Journal of the Virtual Explorer</span><span>, 2010</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Active Italian volcanoes are characterized by a large variability of eruptive mechanisms, from qu...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Active Italian volcanoes are characterized by a large variability of eruptive mechanisms, from quiet lava effusions to catastrophic ignimbritic eruptions. The impact of volcanic activity, and in particular of explosive activity, is clearly related to the intensity and magnitude of the eruptions, varying from an incidental interference with everyday life up to devastating consequences on civilizations. While the largest events have usually monopolized the interest of volcanologists and historians, the modalities and impact of mid intensity eruptions have not been investigated in so much detail. In addition, the frequency of occurrence of mid intensity eruptions is by far higher than that of the largest events, so making their study of primary importance for the assessment of the impact of volcanic activity on environment and human life.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="00d337b09ce3da5acda8e6904c7536e1" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":44249624,"asset_id":23854998,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/44249624/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="23854998"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="23854998"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 23854998; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=23854998]").text(description); $(".js-view-count[data-work-id=23854998]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 23854998; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='23854998']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "00d337b09ce3da5acda8e6904c7536e1" } } $('.js-work-strip[data-work-id=23854998]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":23854998,"title":"Past and present mid-intensity explosive eruptions of Italian volcanoes and their impact on human activity","translated_title":"","metadata":{"ai_title_tag":"Mid-Intensity Explosive Eruptions in Italy","grobid_abstract":"Active Italian volcanoes are characterized by a large variability of eruptive mechanisms, from quiet lava effusions to catastrophic ignimbritic eruptions. The impact of volcanic activity, and in particular of explosive activity, is clearly related to the intensity and magnitude of the eruptions, varying from an incidental interference with everyday life up to devastating consequences on civilizations. While the largest events have usually monopolized the interest of volcanologists and historians, the modalities and impact of mid intensity eruptions have not been investigated in so much detail. In addition, the frequency of occurrence of mid intensity eruptions is by far higher than that of the largest events, so making their study of primary importance for the assessment of the impact of volcanic activity on environment and human life.","publication_date":{"day":null,"month":null,"year":2010,"errors":{}},"publication_name":"Journal of the Virtual Explorer","grobid_abstract_attachment_id":44249624},"translated_abstract":null,"internal_url":"https://www.academia.edu/23854998/Past_and_present_mid_intensity_explosive_eruptions_of_Italian_volcanoes_and_their_impact_on_human_activity","translated_internal_url":"","created_at":"2016-03-31T00:55:37.476-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":14420859,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":44249624,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/44249624/thumbnails/1.jpg","file_name":"Past_and_present_mid-intensity_explosive20160331-25224-jnn1st.pdf","download_url":"https://www.academia.edu/attachments/44249624/download_file","bulk_download_file_name":"Past_and_present_mid_intensity_explosive.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/44249624/Past_and_present_mid-intensity_explosive20160331-25224-jnn1st-libre.pdf?1459411724=\u0026response-content-disposition=attachment%3B+filename%3DPast_and_present_mid_intensity_explosive.pdf\u0026Expires=1743974706\u0026Signature=OTtAtd7HqdhowdlXmh6FL6fuJephMHk16QtXzUIY3NfHauQ0rDeoznm2b1grBPdYX5wD0IZqgvqG~2VirTiaIT6VbWa~52SBhS9p40PDEgNJydI6pzfSFZYSoOMxKu7jke6dKC9VClINlJXDr95-j55ElHPxBov~q1JA0oWPXPZFaZ782g-1q5W7viENYm-9j0HlS23ryu~6dZOd2jzLGjFNli-HB8X33njIzuEZINmmtVATygqlXgZcqQ8H7LyaLltlmX19TL2l~WBI80FLPiWFrA-hDPCJ7FM-sI8SBesD2fy9nacfFQt4Zy9ycceRDIFFB1TlNGd3iPpmJ~5s3w__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Past_and_present_mid_intensity_explosive_eruptions_of_Italian_volcanoes_and_their_impact_on_human_activity","translated_slug":"","page_count":32,"language":"en","content_type":"Work","summary":"Active Italian volcanoes are characterized by a large variability of eruptive mechanisms, from quiet lava effusions to catastrophic ignimbritic eruptions. The impact of volcanic activity, and in particular of explosive activity, is clearly related to the intensity and magnitude of the eruptions, varying from an incidental interference with everyday life up to devastating consequences on civilizations. While the largest events have usually monopolized the interest of volcanologists and historians, the modalities and impact of mid intensity eruptions have not been investigated in so much detail. In addition, the frequency of occurrence of mid intensity eruptions is by far higher than that of the largest events, so making their study of primary importance for the assessment of the impact of volcanic activity on environment and human life.","impression_tracking_id":null,"owner":{"id":14420859,"first_name":"Claudia","middle_initials":null,"last_name":"D'Oriano","page_name":"CDOriano","domain_name":"ingv","created_at":"2014-07-27T18:56:54.386-07:00","display_name":"Claudia D'Oriano","url":"https://ingv.academia.edu/CDOriano"},"attachments":[{"id":44249624,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/44249624/thumbnails/1.jpg","file_name":"Past_and_present_mid-intensity_explosive20160331-25224-jnn1st.pdf","download_url":"https://www.academia.edu/attachments/44249624/download_file","bulk_download_file_name":"Past_and_present_mid_intensity_explosive.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/44249624/Past_and_present_mid-intensity_explosive20160331-25224-jnn1st-libre.pdf?1459411724=\u0026response-content-disposition=attachment%3B+filename%3DPast_and_present_mid_intensity_explosive.pdf\u0026Expires=1743974706\u0026Signature=OTtAtd7HqdhowdlXmh6FL6fuJephMHk16QtXzUIY3NfHauQ0rDeoznm2b1grBPdYX5wD0IZqgvqG~2VirTiaIT6VbWa~52SBhS9p40PDEgNJydI6pzfSFZYSoOMxKu7jke6dKC9VClINlJXDr95-j55ElHPxBov~q1JA0oWPXPZFaZ782g-1q5W7viENYm-9j0HlS23ryu~6dZOd2jzLGjFNli-HB8X33njIzuEZINmmtVATygqlXgZcqQ8H7LyaLltlmX19TL2l~WBI80FLPiWFrA-hDPCJ7FM-sI8SBesD2fy9nacfFQt4Zy9ycceRDIFFB1TlNGd3iPpmJ~5s3w__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry"},{"id":409,"name":"Geophysics","url":"https://www.academia.edu/Documents/in/Geophysics"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-23854998-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="23854997"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/23854997/Petrography_mineralogy_and_geochemistry_of_a_primitive_pumice_from_Stromboli_implications_for_the_deep_feeding_system"><img alt="Research paper thumbnail of Petrography, mineralogy and geochemistry of a primitive pumice from Stromboli: implications for the deep feeding system" class="work-thumbnail" src="https://attachments.academia-assets.com/44249625/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/23854997/Petrography_mineralogy_and_geochemistry_of_a_primitive_pumice_from_Stromboli_implications_for_the_deep_feeding_system">Petrography, mineralogy and geochemistry of a primitive pumice from Stromboli: implications for the deep feeding system</a></div><div class="wp-workCard_item"><span>European Journal of Mineralogy</span><span>, 2011</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">We describe the field relations, petrographic, mineralogical and geochemical characteristics of a...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">We describe the field relations, petrographic, mineralogical and geochemical characteristics of an exceptional ''golden'' pumice belonging to a tephra layer exposed on the summit area of Stromboli volcano, Italy. Pumice sample PST-9 comes from a fallout deposit older than a spatter agglutinate sequence emplaced during the twentieth century. The eruption that produced it had a size exceeding that of intermediate paroxysms but was smaller than large-scale, spatter-forming, paroxysms from the sixteenth century and 1930 A.D. Lapilli are strongly vesicular and crystal-poor, similar to other ''golden'' pumices. Modal proportions include 89 vol% glass, 8 vol% clinopyroxene, 1-2 vol% olivine and 1-2 vol% plagioclase. Plagioclase is represented by reacted crystals coming from the shallow resident magma and incorporated in the pumice during eruption. A total of 74 and 44 crystals of olivine and clinopyroxene, respectively, were examined and 187 and 99 electron microprobe analyses obtained. Fo in olivine ranges between 70 and 92 mol% and Fs in clinopyroxene between 3 and 13 mol%. PST-9 hosts a higher proportion of Fo-rich olivine and Fs-poor clinopyroxene than the other ''golden'' pumices. Groundmass glasses are basaltic (Mg# ¼ 66-69), as are most rim glasses around olivine and clinopyroxene, and glass inclusions in clinopyroxene. They are more primitive than in the other ''golden'' pumices. A few rim glasses and glass inclusions are shoshonitic (Mg# ¼ 45-50). Most glass inclusions in olivine have CaO/Al 2 O 3 higher than the other glasses and the whole-rock. PST-9 has the highest bulk MgO, CaO, Mg# and CaO/Al 2 O 3 and the lowest FeO t of all ''golden'' pumices analysed to date. Analysis of Fe-Mg partitioning between olivine, clinopyroxene and melt allows three crystallization stages to be recognized. The first involves primitive mantle-derived melts (Mg# ¼ 74-80), the second basaltic melts represented by groundmass glasses and the third is associated with more evolved melts represented by the shoshonitic glasses. The population of crystals in ''golden'' pumices is heterogeneous not only because of crystal incorporation from the shallow resident magma, but also because of pre-eruptive recharge of the deep reservoir with primitive melts. Differences between PST-9 and the other ''golden'' pumices in terms of groundmass glass composition and distribution of olivine and clinopyroxene compositions reflect contrasted replenishment rates of the deep reservoir with primitive liquids. Gabbroic inclusions in a clinopyroxene crystal provide a direct illustration of melt wall-rock interaction and stress the variability of the deep reservoir in terms of temperature, crystallinity and phase assemblages. Deep crystallization of plagioclase should be considered as a possibility at Stromboli. PST-9 is exceptionally well representative of the early magmatic evolution of ''golden'' pumices.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="a8c81650036010407acd5d2bb0b99430" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":44249625,"asset_id":23854997,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/44249625/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="23854997"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="23854997"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 23854997; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=23854997]").text(description); $(".js-view-count[data-work-id=23854997]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 23854997; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='23854997']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "a8c81650036010407acd5d2bb0b99430" } } $('.js-work-strip[data-work-id=23854997]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":23854997,"title":"Petrography, mineralogy and geochemistry of a primitive pumice from Stromboli: implications for the deep feeding system","translated_title":"","metadata":{"grobid_abstract":"We describe the field relations, petrographic, mineralogical and geochemical characteristics of an exceptional ''golden'' pumice belonging to a tephra layer exposed on the summit area of Stromboli volcano, Italy. Pumice sample PST-9 comes from a fallout deposit older than a spatter agglutinate sequence emplaced during the twentieth century. The eruption that produced it had a size exceeding that of intermediate paroxysms but was smaller than large-scale, spatter-forming, paroxysms from the sixteenth century and 1930 A.D. Lapilli are strongly vesicular and crystal-poor, similar to other ''golden'' pumices. Modal proportions include 89 vol% glass, 8 vol% clinopyroxene, 1-2 vol% olivine and 1-2 vol% plagioclase. Plagioclase is represented by reacted crystals coming from the shallow resident magma and incorporated in the pumice during eruption. A total of 74 and 44 crystals of olivine and clinopyroxene, respectively, were examined and 187 and 99 electron microprobe analyses obtained. Fo in olivine ranges between 70 and 92 mol% and Fs in clinopyroxene between 3 and 13 mol%. PST-9 hosts a higher proportion of Fo-rich olivine and Fs-poor clinopyroxene than the other ''golden'' pumices. Groundmass glasses are basaltic (Mg# ¼ 66-69), as are most rim glasses around olivine and clinopyroxene, and glass inclusions in clinopyroxene. They are more primitive than in the other ''golden'' pumices. A few rim glasses and glass inclusions are shoshonitic (Mg# ¼ 45-50). Most glass inclusions in olivine have CaO/Al 2 O 3 higher than the other glasses and the whole-rock. PST-9 has the highest bulk MgO, CaO, Mg# and CaO/Al 2 O 3 and the lowest FeO t of all ''golden'' pumices analysed to date. Analysis of Fe-Mg partitioning between olivine, clinopyroxene and melt allows three crystallization stages to be recognized. The first involves primitive mantle-derived melts (Mg# ¼ 74-80), the second basaltic melts represented by groundmass glasses and the third is associated with more evolved melts represented by the shoshonitic glasses. The population of crystals in ''golden'' pumices is heterogeneous not only because of crystal incorporation from the shallow resident magma, but also because of pre-eruptive recharge of the deep reservoir with primitive melts. Differences between PST-9 and the other ''golden'' pumices in terms of groundmass glass composition and distribution of olivine and clinopyroxene compositions reflect contrasted replenishment rates of the deep reservoir with primitive liquids. Gabbroic inclusions in a clinopyroxene crystal provide a direct illustration of melt wall-rock interaction and stress the variability of the deep reservoir in terms of temperature, crystallinity and phase assemblages. Deep crystallization of plagioclase should be considered as a possibility at Stromboli. PST-9 is exceptionally well representative of the early magmatic evolution of ''golden'' pumices.","publication_date":{"day":null,"month":null,"year":2011,"errors":{}},"publication_name":"European Journal of Mineralogy","grobid_abstract_attachment_id":44249625},"translated_abstract":null,"internal_url":"https://www.academia.edu/23854997/Petrography_mineralogy_and_geochemistry_of_a_primitive_pumice_from_Stromboli_implications_for_the_deep_feeding_system","translated_internal_url":"","created_at":"2016-03-31T00:55:37.292-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":14420859,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":44249625,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/44249625/thumbnails/1.jpg","file_name":"Petrography_mineralogy_and_geochemistry_20160331-9958-22xsi7.pdf","download_url":"https://www.academia.edu/attachments/44249625/download_file","bulk_download_file_name":"Petrography_mineralogy_and_geochemistry.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/44249625/Petrography_mineralogy_and_geochemistry_20160331-9958-22xsi7-libre.pdf?1459411723=\u0026response-content-disposition=attachment%3B+filename%3DPetrography_mineralogy_and_geochemistry.pdf\u0026Expires=1743974706\u0026Signature=BwvHk472pRz7GP8XzxUvYxlxehRUo91cipfK7B~huXE0pG9D22MpX0i33FokdEaFGC-qII9QCPMa65b55GnjBnSjyDBYQuBibNQBdHApbSuNp7Eq7U1QDl-OXjY6ZQjkJ2uC7wZB1pPSxSKM1V6XjrRbO-kEVinQSQhmlOdG1hjiBl~oXPopcf1WEe11hZlTP4scK3nUcDN2n1RyKCmFqg~F1ACPObYfZfjK2ee8sdNqPfPqqvBJXgNZ9Acgx9GuBLfAvKrV5~PA9VNuua32NdowkwI~LYafi0iIUouSyJh7p8BI5I7trp8PGd0vV9w~Gl5LqYCsUF-Flao~lzVj0A__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Petrography_mineralogy_and_geochemistry_of_a_primitive_pumice_from_Stromboli_implications_for_the_deep_feeding_system","translated_slug":"","page_count":19,"language":"en","content_type":"Work","summary":"We describe the field relations, petrographic, mineralogical and geochemical characteristics of an exceptional ''golden'' pumice belonging to a tephra layer exposed on the summit area of Stromboli volcano, Italy. Pumice sample PST-9 comes from a fallout deposit older than a spatter agglutinate sequence emplaced during the twentieth century. The eruption that produced it had a size exceeding that of intermediate paroxysms but was smaller than large-scale, spatter-forming, paroxysms from the sixteenth century and 1930 A.D. Lapilli are strongly vesicular and crystal-poor, similar to other ''golden'' pumices. Modal proportions include 89 vol% glass, 8 vol% clinopyroxene, 1-2 vol% olivine and 1-2 vol% plagioclase. Plagioclase is represented by reacted crystals coming from the shallow resident magma and incorporated in the pumice during eruption. A total of 74 and 44 crystals of olivine and clinopyroxene, respectively, were examined and 187 and 99 electron microprobe analyses obtained. Fo in olivine ranges between 70 and 92 mol% and Fs in clinopyroxene between 3 and 13 mol%. PST-9 hosts a higher proportion of Fo-rich olivine and Fs-poor clinopyroxene than the other ''golden'' pumices. Groundmass glasses are basaltic (Mg# ¼ 66-69), as are most rim glasses around olivine and clinopyroxene, and glass inclusions in clinopyroxene. They are more primitive than in the other ''golden'' pumices. A few rim glasses and glass inclusions are shoshonitic (Mg# ¼ 45-50). Most glass inclusions in olivine have CaO/Al 2 O 3 higher than the other glasses and the whole-rock. PST-9 has the highest bulk MgO, CaO, Mg# and CaO/Al 2 O 3 and the lowest FeO t of all ''golden'' pumices analysed to date. Analysis of Fe-Mg partitioning between olivine, clinopyroxene and melt allows three crystallization stages to be recognized. The first involves primitive mantle-derived melts (Mg# ¼ 74-80), the second basaltic melts represented by groundmass glasses and the third is associated with more evolved melts represented by the shoshonitic glasses. The population of crystals in ''golden'' pumices is heterogeneous not only because of crystal incorporation from the shallow resident magma, but also because of pre-eruptive recharge of the deep reservoir with primitive melts. Differences between PST-9 and the other ''golden'' pumices in terms of groundmass glass composition and distribution of olivine and clinopyroxene compositions reflect contrasted replenishment rates of the deep reservoir with primitive liquids. Gabbroic inclusions in a clinopyroxene crystal provide a direct illustration of melt wall-rock interaction and stress the variability of the deep reservoir in terms of temperature, crystallinity and phase assemblages. Deep crystallization of plagioclase should be considered as a possibility at Stromboli. PST-9 is exceptionally well representative of the early magmatic evolution of ''golden'' pumices.","impression_tracking_id":null,"owner":{"id":14420859,"first_name":"Claudia","middle_initials":null,"last_name":"D'Oriano","page_name":"CDOriano","domain_name":"ingv","created_at":"2014-07-27T18:56:54.386-07:00","display_name":"Claudia D'Oriano","url":"https://ingv.academia.edu/CDOriano"},"attachments":[{"id":44249625,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/44249625/thumbnails/1.jpg","file_name":"Petrography_mineralogy_and_geochemistry_20160331-9958-22xsi7.pdf","download_url":"https://www.academia.edu/attachments/44249625/download_file","bulk_download_file_name":"Petrography_mineralogy_and_geochemistry.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/44249625/Petrography_mineralogy_and_geochemistry_20160331-9958-22xsi7-libre.pdf?1459411723=\u0026response-content-disposition=attachment%3B+filename%3DPetrography_mineralogy_and_geochemistry.pdf\u0026Expires=1743974706\u0026Signature=BwvHk472pRz7GP8XzxUvYxlxehRUo91cipfK7B~huXE0pG9D22MpX0i33FokdEaFGC-qII9QCPMa65b55GnjBnSjyDBYQuBibNQBdHApbSuNp7Eq7U1QDl-OXjY6ZQjkJ2uC7wZB1pPSxSKM1V6XjrRbO-kEVinQSQhmlOdG1hjiBl~oXPopcf1WEe11hZlTP4scK3nUcDN2n1RyKCmFqg~F1ACPObYfZfjK2ee8sdNqPfPqqvBJXgNZ9Acgx9GuBLfAvKrV5~PA9VNuua32NdowkwI~LYafi0iIUouSyJh7p8BI5I7trp8PGd0vV9w~Gl5LqYCsUF-Flao~lzVj0A__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":407,"name":"Geochemistry","url":"https://www.academia.edu/Documents/in/Geochemistry"},{"id":279027,"name":"European","url":"https://www.academia.edu/Documents/in/European"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-23854997-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="23854996"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/23854996/Changes_in_eruptive_style_during_the_A_D_1538_Monte_Nuovo_eruption_Phlegrean_Fields_Italy_the_role_of_syn_eruptive_crystallization"><img alt="Research paper thumbnail of Changes in eruptive style during the A.D. 1538 Monte Nuovo eruption (Phlegrean Fields, Italy): the role of syn-eruptive crystallization" class="work-thumbnail" src="https://attachments.academia-assets.com/44249623/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/23854996/Changes_in_eruptive_style_during_the_A_D_1538_Monte_Nuovo_eruption_Phlegrean_Fields_Italy_the_role_of_syn_eruptive_crystallization">Changes in eruptive style during the A.D. 1538 Monte Nuovo eruption (Phlegrean Fields, Italy): the role of syn-eruptive crystallization</a></div><div class="wp-workCard_item"><span>Bulletin of Volcanology</span><span>, 2005</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="01c71c36e36fbe60ef85e4c81fb6ddce" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":44249623,"asset_id":23854996,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/44249623/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="23854996"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="23854996"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 23854996; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=23854996]").text(description); $(".js-view-count[data-work-id=23854996]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 23854996; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='23854996']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "01c71c36e36fbe60ef85e4c81fb6ddce" } } $('.js-work-strip[data-work-id=23854996]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":23854996,"title":"Changes in eruptive style during the A.D. 1538 Monte Nuovo eruption (Phlegrean Fields, Italy): the role of syn-eruptive crystallization","translated_title":"","metadata":{"ai_abstract":"The Monte Nuovo eruption, occurring from September 29 to October 6, 1538, represents a significant volcanic event at Phlegrean Fields, featuring distinct phases of eruption including phreatomagmatic activity and Vulcanian explosions. This research examines the characteristics of the eruptive products, highlighting differences in texture and composition related to crystallization processes occurring during the eruption. Results indicate that syn-eruptive degassing and crystallization played crucial roles in transitioning from one eruptive style to another, underscoring the influence of magma properties on volcanic dynamics.","ai_title_tag":"Eruptive Style Changes in 1538 Monte Nuovo","publication_date":{"day":null,"month":null,"year":2005,"errors":{}},"publication_name":"Bulletin of Volcanology"},"translated_abstract":null,"internal_url":"https://www.academia.edu/23854996/Changes_in_eruptive_style_during_the_A_D_1538_Monte_Nuovo_eruption_Phlegrean_Fields_Italy_the_role_of_syn_eruptive_crystallization","translated_internal_url":"","created_at":"2016-03-31T00:55:37.095-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":14420859,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":44249623,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/44249623/thumbnails/1.jpg","file_name":"Changes_in_eruptive_style_during_the_A.D20160331-730-1nlvvhu.pdf","download_url":"https://www.academia.edu/attachments/44249623/download_file","bulk_download_file_name":"Changes_in_eruptive_style_during_the_A_D.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/44249623/Changes_in_eruptive_style_during_the_A.D20160331-730-1nlvvhu-libre.pdf?1459411721=\u0026response-content-disposition=attachment%3B+filename%3DChanges_in_eruptive_style_during_the_A_D.pdf\u0026Expires=1743974706\u0026Signature=aBwlamsY4AcH4AJtHyUBIbMVhohYSr1vhfyu92NUl2OBi~MEW09x4JiJibJxh7YHrGS~hZ3~IkftQ8O8cz4Du2PJfMtqQ9QWWftj1x8XnB2g5-HG6q7ReiJyCcEo7yJ3G4DlyHuITTFDlwtk3BrRoucQ-ge2KOAR8emDzEzUNqsXBEF2uUAVvHDTP2CP5YESCG8BGwoGtPoXIvQqgE6-V-E36q7Fh6K54ieRi9UexcsvI4KNBhRMhVnkVZb6lb1C-nrPuUS7zCD51rmSDhgtwp0h2pSGncB3hdMjZYbAWMu4tKmDL1Dg1Q8R6h374SIHoeKwbgd4OFvpaOFxJOgymg__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Changes_in_eruptive_style_during_the_A_D_1538_Monte_Nuovo_eruption_Phlegrean_Fields_Italy_the_role_of_syn_eruptive_crystallization","translated_slug":"","page_count":21,"language":"en","content_type":"Work","summary":null,"impression_tracking_id":null,"owner":{"id":14420859,"first_name":"Claudia","middle_initials":null,"last_name":"D'Oriano","page_name":"CDOriano","domain_name":"ingv","created_at":"2014-07-27T18:56:54.386-07:00","display_name":"Claudia D'Oriano","url":"https://ingv.academia.edu/CDOriano"},"attachments":[{"id":44249623,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/44249623/thumbnails/1.jpg","file_name":"Changes_in_eruptive_style_during_the_A.D20160331-730-1nlvvhu.pdf","download_url":"https://www.academia.edu/attachments/44249623/download_file","bulk_download_file_name":"Changes_in_eruptive_style_during_the_A_D.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/44249623/Changes_in_eruptive_style_during_the_A.D20160331-730-1nlvvhu-libre.pdf?1459411721=\u0026response-content-disposition=attachment%3B+filename%3DChanges_in_eruptive_style_during_the_A_D.pdf\u0026Expires=1743974706\u0026Signature=aBwlamsY4AcH4AJtHyUBIbMVhohYSr1vhfyu92NUl2OBi~MEW09x4JiJibJxh7YHrGS~hZ3~IkftQ8O8cz4Du2PJfMtqQ9QWWftj1x8XnB2g5-HG6q7ReiJyCcEo7yJ3G4DlyHuITTFDlwtk3BrRoucQ-ge2KOAR8emDzEzUNqsXBEF2uUAVvHDTP2CP5YESCG8BGwoGtPoXIvQqgE6-V-E36q7Fh6K54ieRi9UexcsvI4KNBhRMhVnkVZb6lb1C-nrPuUS7zCD51rmSDhgtwp0h2pSGncB3hdMjZYbAWMu4tKmDL1Dg1Q8R6h374SIHoeKwbgd4OFvpaOFxJOgymg__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":406,"name":"Geology","url":"https://www.academia.edu/Documents/in/Geology"},{"id":322085,"name":"Pyroclastic Flow","url":"https://www.academia.edu/Documents/in/Pyroclastic_Flow"},{"id":709300,"name":"Trace element","url":"https://www.academia.edu/Documents/in/Trace_element"},{"id":1228946,"name":"Physical Properties","url":"https://www.academia.edu/Documents/in/Physical_Properties"},{"id":1474826,"name":"Crystal Size Distribution","url":"https://www.academia.edu/Documents/in/Crystal_Size_Distribution"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-23854996-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="23854995"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/23854995/Eruptive_scenario_of_ash_dominated_events_at_Vesuvius_the_AP3_eruption_2_710_60_years_BP_"><img alt="Research paper thumbnail of Eruptive scenario of ash-dominated events at Vesuvius: the AP3 eruption (2,710±60 years BP)" class="work-thumbnail" src="https://attachments.academia-assets.com/44249620/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/23854995/Eruptive_scenario_of_ash_dominated_events_at_Vesuvius_the_AP3_eruption_2_710_60_years_BP_">Eruptive scenario of ash-dominated events at Vesuvius: the AP3 eruption (2,710±60 years BP)</a></div><div class="wp-workCard_item"><div class="carousel-container carousel-container--sm" id="profile-work-23854995-figures"><div class="prev-slide-container js-prev-button-container"><button aria-label="Previous" class="carousel-navigation-button js-profile-work-23854995-figures-prev"><span class="material-symbols-outlined" style="font-size: 24px" translate="no">arrow_back_ios</span></button></div><div class="slides-container js-slides-container"><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/21944412/figure-1-eruptive-scenario-of-ash-dominated-events-at"><img alt="" class="figure-slide-image" src="https://figures.academia-assets.com/44249620/figure_001.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/21944413/figure-2-eruptive-scenario-of-ash-dominated-events-at"><img alt="" class="figure-slide-image" src="https://figures.academia-assets.com/44249620/figure_002.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/21944414/figure-3-fic-images-of-ap-ash-fragments-selected-in-the-size"><img alt="Fic. 2. Images of AP3 ash fragments selected in the size range of 1-0.5 mm a) glassy, poorly vesicular; b) coalescent vesicles in a mod- erately vesicular crystal-rich fragments (red arrows follow the coalescence paths); c) pumice-like portion of magma including carry- ing a dense, microlite-rich enclave. " class="figure-slide-image" src="https://figures.academia-assets.com/44249620/figure_003.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/21944415/figure-4-fic-frequency-histogram-of-the-measured-shape"><img alt="Fic. 3. Frequency histogram of the measured shape parameters on ash samples collected along the stratigraphic succession. On the vertical axis data correspond to the % of the total number of clasts analysed for each sample. " class="figure-slide-image" src="https://figures.academia-assets.com/44249620/figure_004.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/21944417/figure-5-fic-different-types-of-outlines-discriminated-on"><img alt="Fic. 4. Different types of outlines discriminated on the base of the cluster tree analyses for the samples from the S1 (proximal) section. Hs = high spherical; sk = sub rounded; Ls = low spher- ical; va = very angular. Number indicate the % abundance of each type respect to the total of investigated clasts for each sample. " class="figure-slide-image" src="https://figures.academia-assets.com/44249620/figure_005.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/21944419/figure-4-fic-different-types-of-outlines-discriminated-on"><img alt="Fic. 5. Different types of outlines discriminated on the base of the cluster tree analyses for the samples from the S2 (distal) sec- tion. Numbers as in Figure 4. " class="figure-slide-image" src="https://figures.academia-assets.com/44249620/figure_006.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/21944421/figure-7-eruptive-scenario-of-ash-dominated-events-at"><img alt="" class="figure-slide-image" src="https://figures.academia-assets.com/44249620/figure_007.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/21944424/figure-8-fic-abundance-of-the-total-of-the-four-different"><img alt="Fic. 7. Abundance (% of the total) of the four different types of fragments in the analysed samples. " class="figure-slide-image" src="https://figures.academia-assets.com/44249620/figure_008.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/21944426/figure-9-eruptive-scenario-of-ash-dominated-events-at"><img alt="" class="figure-slide-image" src="https://figures.academia-assets.com/44249620/figure_009.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/21944427/figure-10-fic-curves-of-crystal-size-distribution-for"><img alt="Fic. 9. Curves of Crystal Size Distribution for plagioclase mi- crolites in the analysed samples. " class="figure-slide-image" src="https://figures.academia-assets.com/44249620/figure_010.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/21944428/table-1-mean-values-and-standard-deviation-in-bracket-of-the"><img alt="TABLE 1. Mean values and standard deviation (in bracket) of the measured shape parameters for each investigated layer. " class="figure-slide-image" src="https://figures.academia-assets.com/44249620/table_001.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/21944429/table-2-results-of-the-principal-component-analyses"><img alt="TaBLE 2. Results of the principal component analyses. " class="figure-slide-image" src="https://figures.academia-assets.com/44249620/table_002.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/21944430/table-4-averaged-glass-composition-number-of-analysis"><img alt="TaBLeE 3. Averaged glass composition. n = number of analysis; o = standard deviation. Five clasts were selected from each investigated sample, in order to obtain quantitative information on ground- mass texture. We consider only the mve fragments with similar vesicularity index (40-54 vol.%), which represent the most abundant type in all the investigated samples, except for the VSM54. Plagioclase is the unique miner- alogical phase considered for this textural study. Table 4 summarizes the main 2 D and 3D textural data. Leucite, the other abundant microlite phase, was not considered Analyses of the glass composition were performed on ash fragments selected from the mvc, mvc and pve types, while pcr fragments were difficult to analyse for the very low amount of glass between crystals. Clast- " class="figure-slide-image" src="https://figures.academia-assets.com/44249620/table_003.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/21944431/table-4-plagioclase-parameters-derived-from-the-crystals"><img alt="TaBLe 4. Plagioclase parameters derived from the crystals size distributions analyses. ® = fraction of microlites (vol.%), G = Average growth rate (mm/sec); tT = time for crystals growth (sec); 3G t = crystals average dominant size (Cashman 1992); Na = number of microlites per unit area (mm-2); n° = nuclei number density (mm-4). " class="figure-slide-image" src="https://figures.academia-assets.com/44249620/table_004.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/21944432/table-5-proposed-eruption-scenario-for-ash-dominated"><img alt="TaBLE 5. Proposed eruption scenario for ash-dominated eruptions at Vesuvius. Eruptive scenario of ash-dominated events at Vesuvius: the AP3 eruption (2,710 + 60 years BP) " class="figure-slide-image" src="https://figures.academia-assets.com/44249620/table_005.jpg" /></a></figure></div><div class="next-slide-container js-next-button-container"><button aria-label="Next" class="carousel-navigation-button js-profile-work-23854995-figures-next"><span class="material-symbols-outlined" style="font-size: 24px" translate="no">arrow_forward_ios</span></button></div></div></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="e3b45f08a2be41d35408f5ddfb503007" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":44249620,"asset_id":23854995,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/44249620/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="23854995"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="23854995"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 23854995; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=23854995]").text(description); $(".js-view-count[data-work-id=23854995]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 23854995; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='23854995']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "e3b45f08a2be41d35408f5ddfb503007" } } $('.js-work-strip[data-work-id=23854995]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":23854995,"title":"Eruptive scenario of ash-dominated events at Vesuvius: the AP3 eruption (2,710±60 years BP)","translated_title":"","metadata":{"ai_abstract":"Eruptive scenarios dominated by ash emission at Vesuvius have significant implications for understanding volcanic risks. The AP3 eruption, dated 2,710±60 years BP, illustrates mechanisms of ash production influenced by magma-water interactions. 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-23854994-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="12941618"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/12941618/Ash_production_within_a_pyroclastic_flow_grain_size_variations_due_to_mechanical_grinding"><img alt="Research paper thumbnail of Ash production within a pyroclastic flow: grain-size variations due to mechanical grinding" class="work-thumbnail" src="https://attachments.academia-assets.com/45834391/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/12941618/Ash_production_within_a_pyroclastic_flow_grain_size_variations_due_to_mechanical_grinding">Ash production within a pyroclastic flow: grain-size variations due to mechanical grinding</a></div><div class="wp-workCard_item wp-workCard--coauthors"><span>by </span><span><a class="" data-click-track="profile-work-strip-authors" href="https://unica-it.academia.edu/FMundula">F. Mundula</a> and <a class="" data-click-track="profile-work-strip-authors" href="https://ingv.academia.edu/CDOriano">Claudia D'Oriano</a></span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Pyroclastic flow deposits are generally characterized by a large amount of ash. Direct observatio...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Pyroclastic flow deposits are generally characterized by a large amount of ash. Direct observations and stratigraphic studies suggest that a portion of the ash fraction of pyroclastic flow deposits is generated during the transport, by abrasion and collision of largest particles. Conversely, part of the fine grained particles is generally elutriated during transport of the eruptive cloud. Due to their widespread dispersal and low sedimentation rate, ash particles represent a potential risk for living beings and environment. The knowledge of the initial grainsize distribution of an eruptive mixture is of fundamental importance for estimating physical parameters, such as intensity, magnitude and style of an eruption, and represents a basic input parameter for models of column dynamics and transport. In order to study the effect of particle collision and abrasion on the evolution of the particle-size distribution of a pyroclastic mixture,and to relate the production of ash to the evolution of particles shape, we performed grinding experiments using the Los Angeles test. This apparatus allows simulating the process of particle-particle interaction/collision and consequent abrasion and rupture. Starting material consists of three samples from Vesuvius eruptions, representing three end-members in term of textural features of the juvenile material (scoriae vs pumices) and of components that constitute the flow (whole sample vs selected scoriae): VS17 was collected at a proximal site from a flow unit of the subplinian Pollena eruption (472 DC) and represents an example of coarse-grained, lithic rich, matrix supported deposit mainly constituted by scoriaceous juvenile material; C24bis is constituted by juvenile, dm-sized, moderately vesicular scoria-like bombs, selected from a proximal pyroclastic flow deposit of the Pollena eruption (472 DC); while sample VSM80-81 is constituted by cm-sized, highly vesicular pumices from the fallout deposit of the plinian Mercato eruption (8000 yr BP). Three cycles of mechanical grinding were performed on each sample, with a duration of 3, 10 and 30 min, respectively. After each cycle, grain size analyses of experimental products were performed and an aliquot (few grams) of the resulting material from size-classes between -4 and 2 phi collected for morphological studies. In this way, the variation of the shape of the clasts and times of abrasion (roughly corresponding to the runout of the flow) can be correlated. Data are discussed in terms of enrichment in fine grained material with respect to untreated samples, revealing a strong effect of grinding duration and, surprisingly, only a minor control of material properties. Large amounts of ash are produced in the range 3 to 10 phi, with a net increase inside the smaller sizes of up to 2000%. Shape analysis were performed on a subset of 30-50 clasts from each size interval between -4 and 2 phi collected at the end of each experimental run. As good shape descriptors we consider the excess perimeter (?P) and defect area (?A), which well account for the fractured/angular (large ?P and small ?A) and lobate/rounded (large ?A and small ?P) shapes. As we could expect, clast roundness well correlates increasing experimental time with the most of the shape variation occurring immediately after short times of grinding. Grain size and shape data are useful to recognize and quantify co-ignimbrite ash early separated from pyroclastic flows and dispersed over larger areas by different transport mechanisms.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="2543f39024d25b4efd070ef2670cb653" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":45834391,"asset_id":12941618,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/45834391/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="12941618"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="12941618"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 12941618; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=12941618]").text(description); $(".js-view-count[data-work-id=12941618]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 12941618; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='12941618']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "2543f39024d25b4efd070ef2670cb653" } } $('.js-work-strip[data-work-id=12941618]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":12941618,"title":"Ash production within a pyroclastic flow: grain-size variations due to mechanical grinding","translated_title":"","metadata":{"ai_title_tag":"Ash Production from Pyroclastic Flow Grinding","grobid_abstract":"Pyroclastic flow deposits are generally characterized by a large amount of ash. 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In order to study the effect of particle collision and abrasion on the evolution of the particle-size distribution of a pyroclastic mixture,and to relate the production of ash to the evolution of particles shape, we performed grinding experiments using the Los Angeles test. This apparatus allows simulating the process of particle-particle interaction/collision and consequent abrasion and rupture. Starting material consists of three samples from Vesuvius eruptions, representing three end-members in term of textural features of the juvenile material (scoriae vs pumices) and of components that constitute the flow (whole sample vs selected scoriae): VS17 was collected at a proximal site from a flow unit of the subplinian Pollena eruption (472 DC) and represents an example of coarse-grained, lithic rich, matrix supported deposit mainly constituted by scoriaceous juvenile material; C24bis is constituted by juvenile, dm-sized, moderately vesicular scoria-like bombs, selected from a proximal pyroclastic flow deposit of the Pollena eruption (472 DC); while sample VSM80-81 is constituted by cm-sized, highly vesicular pumices from the fallout deposit of the plinian Mercato eruption (8000 yr BP). Three cycles of mechanical grinding were performed on each sample, with a duration of 3, 10 and 30 min, respectively. After each cycle, grain size analyses of experimental products were performed and an aliquot (few grams) of the resulting material from size-classes between -4 and 2 phi collected for morphological studies. In this way, the variation of the shape of the clasts and times of abrasion (roughly corresponding to the runout of the flow) can be correlated. Data are discussed in terms of enrichment in fine grained material with respect to untreated samples, revealing a strong effect of grinding duration and, surprisingly, only a minor control of material properties. Large amounts of ash are produced in the range 3 to 10 phi, with a net increase inside the smaller sizes of up to 2000%. Shape analysis were performed on a subset of 30-50 clasts from each size interval between -4 and 2 phi collected at the end of each experimental run. As good shape descriptors we consider the excess perimeter (?P) and defect area (?A), which well account for the fractured/angular (large ?P and small ?A) and lobate/rounded (large ?A and small ?P) shapes. As we could expect, clast roundness well correlates increasing experimental time with the most of the shape variation occurring immediately after short times of grinding. 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Direct observations and stratigraphic studies suggest that a portion of the ash fraction of pyroclastic flow deposits is generated during the transport, by abrasion and collision of largest particles. Conversely, part of the fine grained particles is generally elutriated during transport of the eruptive cloud. Due to their widespread dispersal and low sedimentation rate, ash particles represent a potential risk for living beings and environment. The knowledge of the initial grainsize distribution of an eruptive mixture is of fundamental importance for estimating physical parameters, such as intensity, magnitude and style of an eruption, and represents a basic input parameter for models of column dynamics and transport. In order to study the effect of particle collision and abrasion on the evolution of the particle-size distribution of a pyroclastic mixture,and to relate the production of ash to the evolution of particles shape, we performed grinding experiments using the Los Angeles test. This apparatus allows simulating the process of particle-particle interaction/collision and consequent abrasion and rupture. Starting material consists of three samples from Vesuvius eruptions, representing three end-members in term of textural features of the juvenile material (scoriae vs pumices) and of components that constitute the flow (whole sample vs selected scoriae): VS17 was collected at a proximal site from a flow unit of the subplinian Pollena eruption (472 DC) and represents an example of coarse-grained, lithic rich, matrix supported deposit mainly constituted by scoriaceous juvenile material; C24bis is constituted by juvenile, dm-sized, moderately vesicular scoria-like bombs, selected from a proximal pyroclastic flow deposit of the Pollena eruption (472 DC); while sample VSM80-81 is constituted by cm-sized, highly vesicular pumices from the fallout deposit of the plinian Mercato eruption (8000 yr BP). Three cycles of mechanical grinding were performed on each sample, with a duration of 3, 10 and 30 min, respectively. After each cycle, grain size analyses of experimental products were performed and an aliquot (few grams) of the resulting material from size-classes between -4 and 2 phi collected for morphological studies. In this way, the variation of the shape of the clasts and times of abrasion (roughly corresponding to the runout of the flow) can be correlated. Data are discussed in terms of enrichment in fine grained material with respect to untreated samples, revealing a strong effect of grinding duration and, surprisingly, only a minor control of material properties. Large amounts of ash are produced in the range 3 to 10 phi, with a net increase inside the smaller sizes of up to 2000%. Shape analysis were performed on a subset of 30-50 clasts from each size interval between -4 and 2 phi collected at the end of each experimental run. As good shape descriptors we consider the excess perimeter (?P) and defect area (?A), which well account for the fractured/angular (large ?P and small ?A) and lobate/rounded (large ?A and small ?P) shapes. As we could expect, clast roundness well correlates increasing experimental time with the most of the shape variation occurring immediately after short times of grinding. Grain size and shape data are useful to recognize and quantify co-ignimbrite ash early separated from pyroclastic flows and dispersed over larger areas by different transport mechanisms.","impression_tracking_id":null,"owner":{"id":32123250,"first_name":"F.","middle_initials":null,"last_name":"Mundula","page_name":"FMundula","domain_name":"unica-it","created_at":"2015-06-12T02:01:26.207-07:00","display_name":"F. 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Bertagnini</a> and <a class="" data-click-track="profile-work-strip-authors" href="https://ingv.academia.edu/CDOriano">Claudia D'Oriano</a></span></div><div class="wp-workCard_item"><span>Geophysical Research Letters</span><span>, 2012</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">ABSTRACT 1] Textures, petrography and geochemical compositions of products emitted during the ons...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">ABSTRACT 1] Textures, petrography and geochemical compositions of products emitted during the onset of the 2011–2012 sub-marine eruption (15 October, 2011) off the coast of El Hierro have been investigated to get information on interaction mechanism between the first rising magma and the crust during the onset of the eruption as well as to get information on magma storage and plumbing systems beneath El Hierro volcano. Studied products consist of 5–50 cm bombs with an outer black to greenish, vesicular crust with bulk basanite composition containing pumiceous xenoliths (xenopumices). Our results show that xenopumices are much more hetero-geneous that previously observed, since consist of a macro-scale mingling of a gray trachyte and white rhyolite. We interpreted xenopumices as resulting from the interaction (heating) between the basanitic magma feeding the eruption, a stagnant trachytic magma pocket/s and an associated hydro-thermally altered halo with rhyolitic composition. Our find-ings confirm the importance of the study of the early products of an eruption since they can contain crucial information on the plumbing system geometry and the mechanism of magma ascent. 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Bertagnini</a> and <a class="" data-click-track="profile-work-strip-authors" href="https://ingv.academia.edu/CDOriano">Claudia D'Oriano</a></span></div><div class="wp-workCard_item"><span>Scientific Reports</span><span>, 2014</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="19fc2efe0259d423329a8fbcb274aef8" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":39177547,"asset_id":16777160,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/39177547/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="16777160"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="16777160"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 16777160; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=16777160]").text(description); $(".js-view-count[data-work-id=16777160]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 16777160; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='16777160']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "19fc2efe0259d423329a8fbcb274aef8" } } $('.js-work-strip[data-work-id=16777160]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":16777160,"title":"Identifying recycled ash in basaltic eruptions","translated_title":"","metadata":{"ai_abstract":"This study investigates the characteristics and significance of recycled ash in basaltic eruptions. 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The deposits of this<br />eruption consist of an alternation of massive and thinly laminated ash layers and minor well sorted lapilli beds,<br />reflecting the pulsatory injection into the atmosphere of<br />variably concentrated ash-plumes alternating with Violent<br />Strombolian stages. Despite its nearly constant chemical<br />composition, the juvenile material shows variable external<br />clast morphologies and groundmass textures, reflecting the<br />fragmentation of a magma body with lateral and/or vertical<br />gradients in both vesicularity and crystal content. Glass<br />compositions and mineralogical assemblages indicate that the<br />eruption was fed by rather homogeneous phonotephritic<br />magma batches rising from a reservoir located at ~ 4 km<br />(100 MPa) depth, with fluctuations between magma delivery<br />and magma discharge. Using crystal size distribution (CSD)<br />analyses of plagioclase and leucite microlites, we estimate that<br />the transit time of the magma in the conduit was on the order<br />of ~ 2 days, corresponding to an ascent rate of around 2×<br />10−2 ms−1. Accordingly, assuming a typical conduit diameter<br />for this type of eruption, the minimum duration of the AS1a<br />event is between about 1.5 and 6 years. Magma fragmentation<br />occurred in an inertially driven regime that, in a magma<br />with low viscosity and surface tension, can act also under<br />conditions of slow ascent.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="0956e6172715b5918d61383af8016995" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":35229015,"asset_id":8899852,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/35229015/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="8899852"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="8899852"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 8899852; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=8899852]").text(description); $(".js-view-count[data-work-id=8899852]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 8899852; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='8899852']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "0956e6172715b5918d61383af8016995" } } $('.js-work-strip[data-work-id=8899852]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":8899852,"title":"Dynamics of ash-dominated eruptions at Vesuvius: the post-512 AD AS1a event","translated_title":"","metadata":{"abstract":"Recent stratigraphic studies at Vesuvius have\nrevealed that, during the past 4,000 years, long lasting,\nmoderate to low-intensity eruptions, associated with continuous\nor pulsating ash emission, have repeatedly occurred.\nThe present work focuses on the AS1a eruption, the\nfirst of a series of ash-dominated explosive episodes which\ncharacterized the period between the two Subplinian\neruptions of 472 AD and 1631 AD. The deposits of this\neruption consist of an alternation of massive and thinly laminated ash layers and minor well sorted lapilli beds,\nreflecting the pulsatory injection into the atmosphere of\nvariably concentrated ash-plumes alternating with Violent\nStrombolian stages. Despite its nearly constant chemical\ncomposition, the juvenile material shows variable external\nclast morphologies and groundmass textures, reflecting the\nfragmentation of a magma body with lateral and/or vertical\ngradients in both vesicularity and crystal content. Glass\ncompositions and mineralogical assemblages indicate that the\neruption was fed by rather homogeneous phonotephritic\nmagma batches rising from a reservoir located at ~ 4 km\n(100 MPa) depth, with fluctuations between magma delivery\nand magma discharge. Using crystal size distribution (CSD)\nanalyses of plagioclase and leucite microlites, we estimate that\nthe transit time of the magma in the conduit was on the order\nof ~ 2 days, corresponding to an ascent rate of around 2×\n10−2 ms−1. Accordingly, assuming a typical conduit diameter\nfor this type of eruption, the minimum duration of the AS1a\nevent is between about 1.5 and 6 years. Magma fragmentation\noccurred in an inertially driven regime that, in a magma\nwith low viscosity and surface tension, can act also under\nconditions of slow ascent."},"translated_abstract":"Recent stratigraphic studies at Vesuvius have\nrevealed that, during the past 4,000 years, long lasting,\nmoderate to low-intensity eruptions, associated with continuous\nor pulsating ash emission, have repeatedly occurred.\nThe present work focuses on the AS1a eruption, the\nfirst of a series of ash-dominated explosive episodes which\ncharacterized the period between the two Subplinian\neruptions of 472 AD and 1631 AD. The deposits of this\neruption consist of an alternation of massive and thinly laminated ash layers and minor well sorted lapilli beds,\nreflecting the pulsatory injection into the atmosphere of\nvariably concentrated ash-plumes alternating with Violent\nStrombolian stages. Despite its nearly constant chemical\ncomposition, the juvenile material shows variable external\nclast morphologies and groundmass textures, reflecting the\nfragmentation of a magma body with lateral and/or vertical\ngradients in both vesicularity and crystal content. Glass\ncompositions and mineralogical assemblages indicate that the\neruption was fed by rather homogeneous phonotephritic\nmagma batches rising from a reservoir located at ~ 4 km\n(100 MPa) depth, with fluctuations between magma delivery\nand magma discharge. Using crystal size distribution (CSD)\nanalyses of plagioclase and leucite microlites, we estimate that\nthe transit time of the magma in the conduit was on the order\nof ~ 2 days, corresponding to an ascent rate of around 2×\n10−2 ms−1. Accordingly, assuming a typical conduit diameter\nfor this type of eruption, the minimum duration of the AS1a\nevent is between about 1.5 and 6 years. Magma fragmentation\noccurred in an inertially driven regime that, in a magma\nwith low viscosity and surface tension, can act also under\nconditions of slow ascent.","internal_url":"https://www.academia.edu/8899852/Dynamics_of_ash_dominated_eruptions_at_Vesuvius_the_post_512_AD_AS1a_event","translated_internal_url":"","created_at":"2014-10-21T20:23:43.920-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":14420859,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":7992065,"work_id":8899852,"tagging_user_id":14420859,"tagged_user_id":36210384,"co_author_invite_id":null,"email":"a***i@ingv.it","display_order":0,"name":"A. Bertagnini","title":"Dynamics of ash-dominated eruptions at Vesuvius: the post-512 AD AS1a event"},{"id":18172523,"work_id":8899852,"tagging_user_id":14420859,"tagged_user_id":37146682,"co_author_invite_id":null,"email":"p***e@plymouth.ac.uk","display_order":4194304,"name":"P. 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The deposits of this\neruption consist of an alternation of massive and thinly laminated ash layers and minor well sorted lapilli beds,\nreflecting the pulsatory injection into the atmosphere of\nvariably concentrated ash-plumes alternating with Violent\nStrombolian stages. Despite its nearly constant chemical\ncomposition, the juvenile material shows variable external\nclast morphologies and groundmass textures, reflecting the\nfragmentation of a magma body with lateral and/or vertical\ngradients in both vesicularity and crystal content. Glass\ncompositions and mineralogical assemblages indicate that the\neruption was fed by rather homogeneous phonotephritic\nmagma batches rising from a reservoir located at ~ 4 km\n(100 MPa) depth, with fluctuations between magma delivery\nand magma discharge. Using crystal size distribution (CSD)\nanalyses of plagioclase and leucite microlites, we estimate that\nthe transit time of the magma in the conduit was on the order\nof ~ 2 days, corresponding to an ascent rate of around 2×\n10−2 ms−1. Accordingly, assuming a typical conduit diameter\nfor this type of eruption, the minimum duration of the AS1a\nevent is between about 1.5 and 6 years. Magma fragmentation\noccurred in an inertially driven regime that, in a magma\nwith low viscosity and surface tension, can act also under\nconditions of slow ascent.","impression_tracking_id":null,"owner":{"id":14420859,"first_name":"Claudia","middle_initials":null,"last_name":"D'Oriano","page_name":"CDOriano","domain_name":"ingv","created_at":"2014-07-27T18:56:54.386-07:00","display_name":"Claudia D'Oriano","url":"https://ingv.academia.edu/CDOriano"},"attachments":[{"id":35229015,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/35229015/thumbnails/1.jpg","file_name":"DOriano_et_al_2011.pdf","download_url":"https://www.academia.edu/attachments/35229015/download_file","bulk_download_file_name":"Dynamics_of_ash_dominated_eruptions_at_V.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/35229015/DOriano_et_al_2011-libre.pdf?1413948161=\u0026response-content-disposition=attachment%3B+filename%3DDynamics_of_ash_dominated_eruptions_at_V.pdf\u0026Expires=1743974710\u0026Signature=ch3Nz2~7LeJYSrk2L1BrFwuxDUCso7N3qGymKaSNuiYiTuZ5sJt0jrY1uj5MOPyEU~7yfDS~WkhhicBwLxRGJwczvg6JlS~7bXJ6rJdC6oBIFfo6ij084NcaHtqmLW1MUgBV~Toy3i6bETorm4OR4bjNadL1RzEFjY-1f3hsDHEig8gAwkM-0rm6i2y-vzWbngvNB5hMsMTE7CtzC9VKuk-7WuKpuTgpb1P~NDuQsPVXywCjIVBoQlX6b-nkQNGiJe10cUsyTaKsEVtsbt5rUwjX~Qfnr5SQn9VMPZW7YXXEfpc12iCYd5AO3-Dwwz5Uvk3TS2nvpSSPnkVMblQVrw__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":1370,"name":"Volcanology","url":"https://www.academia.edu/Documents/in/Volcanology"},{"id":78128,"name":"Vesuvius","url":"https://www.academia.edu/Documents/in/Vesuvius"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-8899852-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="8899826"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/8899826/Effects_of_experimental_reheating_of_natural_basaltic_ash_at_different_temperatures_and_redox_conditions"><img alt="Research paper thumbnail of Effects of experimental reheating of natural basaltic ash at different temperatures and redox conditions" class="work-thumbnail" src="https://attachments.academia-assets.com/35228999/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/8899826/Effects_of_experimental_reheating_of_natural_basaltic_ash_at_different_temperatures_and_redox_conditions">Effects of experimental reheating of natural basaltic ash at different temperatures and redox conditions</a></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">A set of experiments have been performed on volcanic materials from Etna, Stromboli and Vesuvius ...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">A set of experiments have been performed on<br />volcanic materials from Etna, Stromboli and Vesuvius in<br />order to evaluate how the exposure to thermal and redox<br />conditions close to that of active craters affects the texture<br />and composition of juvenile pyroclasts. Selected samples<br />were placed within a quartz tube, in presence of air or<br />under vacuum, and kept at T between 700 and 1,130 C, for<br />variable time (40 min to 12 h). Results show that reheating<br />reactivates the melt, which, through processes of chemical<br />and thermal diffusion, reaches new equilibrium conditions.<br />In all the experiments performed at T = 700–750 C, a<br />large number of crystal nuclei and spherulites grows in the<br />groundmass, suggesting conditions of high undercooling.<br />This process creates textural heterogeneities at the scale of<br />few microns but only limited changes of groundmass<br />composition, which remains clustered around that of the<br />natural glasses. Reheating at T = 1,000–1,050 C promotes<br />massive groundmass crystallization, with a different<br />mineral assemblage as a function of the redox conditions. Morphological modifications of clasts, from softening to<br />sintering as temperature increases, occur under these conditions,<br />accompanied by progressive smoothing of external<br />surfaces, and a reduction in size and abundance of vesicles,<br />until the complete obliteration of the pre-existing vesicularity.<br />The transition from sintering to welding, characteristic<br />of high temperature, is influenced by redox conditions.<br />Experiments at T = 1,100–1,130 C and under vacuum<br />produce groundmass textures and glass compositions similar<br />to that of the respective starting material. Collapse and<br />welding of the clasts cause significant densification of the<br />whole charge. At the same temperature, but in presence of<br />air, experimental products at least result sintered and show<br />holocrystalline groundmass. In all experiments, sublimates<br />grow on the external surfaces of the clasts or form a lining<br />on the bubble walls. Their shape and composition is a<br />function of temperature and fO2 and the abundance of<br />sublimates shows a peak at 1,000 C. The identification of<br />the features recorded by pyroclasts during complex heating–<br />cooling cycles allows reconstructing the complete<br />clasts history before their final emplacement, during<br />weakly explosive volcanic activity. This has a strong<br />implication on the characterization of primary juvenile<br />material and on the interpretation of eruption dynamics.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="0435ccc572ec492967928f1ebcb4a237" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":35228999,"asset_id":8899826,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/35228999/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="8899826"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="8899826"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 8899826; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=8899826]").text(description); $(".js-view-count[data-work-id=8899826]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 8899826; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='8899826']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "0435ccc572ec492967928f1ebcb4a237" } } $('.js-work-strip[data-work-id=8899826]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":8899826,"title":"Effects of experimental reheating of natural basaltic ash at different temperatures and redox conditions","translated_title":"","metadata":{"abstract":"A set of experiments have been performed on\nvolcanic materials from Etna, Stromboli and Vesuvius in\norder to evaluate how the exposure to thermal and redox\nconditions close to that of active craters affects the texture\nand composition of juvenile pyroclasts. Selected samples\nwere placed within a quartz tube, in presence of air or\nunder vacuum, and kept at T between 700 and 1,130 \u0003C, for\nvariable time (40 min to 12 h). Results show that reheating\nreactivates the melt, which, through processes of chemical\nand thermal diffusion, reaches new equilibrium conditions.\nIn all the experiments performed at T = 700–750 \u0003C, a\nlarge number of crystal nuclei and spherulites grows in the\ngroundmass, suggesting conditions of high undercooling.\nThis process creates textural heterogeneities at the scale of\nfew microns but only limited changes of groundmass\ncomposition, which remains clustered around that of the\nnatural glasses. Reheating at T = 1,000–1,050 \u0003C promotes\nmassive groundmass crystallization, with a different\nmineral assemblage as a function of the redox conditions. Morphological modifications of clasts, from softening to\nsintering as temperature increases, occur under these conditions,\naccompanied by progressive smoothing of external\nsurfaces, and a reduction in size and abundance of vesicles,\nuntil the complete obliteration of the pre-existing vesicularity.\nThe transition from sintering to welding, characteristic\nof high temperature, is influenced by redox conditions.\nExperiments at T = 1,100–1,130 \u0003C and under vacuum\nproduce groundmass textures and glass compositions similar\nto that of the respective starting material. Collapse and\nwelding of the clasts cause significant densification of the\nwhole charge. At the same temperature, but in presence of\nair, experimental products at least result sintered and show\nholocrystalline groundmass. In all experiments, sublimates\ngrow on the external surfaces of the clasts or form a lining\non the bubble walls. Their shape and composition is a\nfunction of temperature and fO2 and the abundance of\nsublimates shows a peak at 1,000 \u0003C. The identification of\nthe features recorded by pyroclasts during complex heating–\ncooling cycles allows reconstructing the complete\nclasts history before their final emplacement, during\nweakly explosive volcanic activity. This has a strong\nimplication on the characterization of primary juvenile\nmaterial and on the interpretation of eruption dynamics.","ai_title_tag":"Reheating Effects on Basaltic Ash Textures"},"translated_abstract":"A set of experiments have been performed on\nvolcanic materials from Etna, Stromboli and Vesuvius in\norder to evaluate how the exposure to thermal and redox\nconditions close to that of active craters affects the texture\nand composition of juvenile pyroclasts. Selected samples\nwere placed within a quartz tube, in presence of air or\nunder vacuum, and kept at T between 700 and 1,130 \u0003C, for\nvariable time (40 min to 12 h). Results show that reheating\nreactivates the melt, which, through processes of chemical\nand thermal diffusion, reaches new equilibrium conditions.\nIn all the experiments performed at T = 700–750 \u0003C, a\nlarge number of crystal nuclei and spherulites grows in the\ngroundmass, suggesting conditions of high undercooling.\nThis process creates textural heterogeneities at the scale of\nfew microns but only limited changes of groundmass\ncomposition, which remains clustered around that of the\nnatural glasses. Reheating at T = 1,000–1,050 \u0003C promotes\nmassive groundmass crystallization, with a different\nmineral assemblage as a function of the redox conditions. Morphological modifications of clasts, from softening to\nsintering as temperature increases, occur under these conditions,\naccompanied by progressive smoothing of external\nsurfaces, and a reduction in size and abundance of vesicles,\nuntil the complete obliteration of the pre-existing vesicularity.\nThe transition from sintering to welding, characteristic\nof high temperature, is influenced by redox conditions.\nExperiments at T = 1,100–1,130 \u0003C and under vacuum\nproduce groundmass textures and glass compositions similar\nto that of the respective starting material. Collapse and\nwelding of the clasts cause significant densification of the\nwhole charge. At the same temperature, but in presence of\nair, experimental products at least result sintered and show\nholocrystalline groundmass. In all experiments, sublimates\ngrow on the external surfaces of the clasts or form a lining\non the bubble walls. Their shape and composition is a\nfunction of temperature and fO2 and the abundance of\nsublimates shows a peak at 1,000 \u0003C. The identification of\nthe features recorded by pyroclasts during complex heating–\ncooling cycles allows reconstructing the complete\nclasts history before their final emplacement, during\nweakly explosive volcanic activity. This has a strong\nimplication on the characterization of primary juvenile\nmaterial and on the interpretation of eruption dynamics.","internal_url":"https://www.academia.edu/8899826/Effects_of_experimental_reheating_of_natural_basaltic_ash_at_different_temperatures_and_redox_conditions","translated_internal_url":"","created_at":"2014-10-21T20:21:36.111-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":14420859,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":35228999,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/35228999/thumbnails/1.jpg","file_name":"DOriano_et_al_CMP2012.pdf","download_url":"https://www.academia.edu/attachments/35228999/download_file","bulk_download_file_name":"Effects_of_experimental_reheating_of_nat.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/35228999/DOriano_et_al_CMP2012-libre.pdf?1413948071=\u0026response-content-disposition=attachment%3B+filename%3DEffects_of_experimental_reheating_of_nat.pdf\u0026Expires=1743974710\u0026Signature=VoHgJlq-uWPQirTjUiWLf5zkXJANZ94l8eRIdHV4L9SR6D2n4ql0uxSDF5h-leQ-l-HjMPa7BZnwKRRuOvv~V5ZjKissF4h0XIwS0Z0HUkh-xzK1XuMSoJSMPVz5luUSMBpet-KHYiBswMPiDjva-QA10U8x6QpEA4wQQoqKnkncsfhfsCPldnMIUu0VDiMrsluVdEuQ-VM5AfxnEsTFQjHG0kp1Jj-xNH3yqTawctZDFlGiw4nkLpRTfl7U8MaBEYbwwlhChqyl9cQhZjifPdYdD7o3NJeL8wirtEkXqUpkWSdbhmJGzE8FW8KITBdgh8~JT25EoFaECGF8ADJXBQ__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Effects_of_experimental_reheating_of_natural_basaltic_ash_at_different_temperatures_and_redox_conditions","translated_slug":"","page_count":21,"language":"en","content_type":"Work","summary":"A set of experiments have been performed on\nvolcanic materials from Etna, Stromboli and Vesuvius in\norder to evaluate how the exposure to thermal and redox\nconditions close to that of active craters affects the texture\nand composition of juvenile pyroclasts. Selected samples\nwere placed within a quartz tube, in presence of air or\nunder vacuum, and kept at T between 700 and 1,130 \u0003C, for\nvariable time (40 min to 12 h). Results show that reheating\nreactivates the melt, which, through processes of chemical\nand thermal diffusion, reaches new equilibrium conditions.\nIn all the experiments performed at T = 700–750 \u0003C, a\nlarge number of crystal nuclei and spherulites grows in the\ngroundmass, suggesting conditions of high undercooling.\nThis process creates textural heterogeneities at the scale of\nfew microns but only limited changes of groundmass\ncomposition, which remains clustered around that of the\nnatural glasses. Reheating at T = 1,000–1,050 \u0003C promotes\nmassive groundmass crystallization, with a different\nmineral assemblage as a function of the redox conditions. Morphological modifications of clasts, from softening to\nsintering as temperature increases, occur under these conditions,\naccompanied by progressive smoothing of external\nsurfaces, and a reduction in size and abundance of vesicles,\nuntil the complete obliteration of the pre-existing vesicularity.\nThe transition from sintering to welding, characteristic\nof high temperature, is influenced by redox conditions.\nExperiments at T = 1,100–1,130 \u0003C and under vacuum\nproduce groundmass textures and glass compositions similar\nto that of the respective starting material. Collapse and\nwelding of the clasts cause significant densification of the\nwhole charge. At the same temperature, but in presence of\nair, experimental products at least result sintered and show\nholocrystalline groundmass. In all experiments, sublimates\ngrow on the external surfaces of the clasts or form a lining\non the bubble walls. Their shape and composition is a\nfunction of temperature and fO2 and the abundance of\nsublimates shows a peak at 1,000 \u0003C. The identification of\nthe features recorded by pyroclasts during complex heating–\ncooling cycles allows reconstructing the complete\nclasts history before their final emplacement, during\nweakly explosive volcanic activity. This has a strong\nimplication on the characterization of primary juvenile\nmaterial and on the interpretation of eruption dynamics.","impression_tracking_id":null,"owner":{"id":14420859,"first_name":"Claudia","middle_initials":null,"last_name":"D'Oriano","page_name":"CDOriano","domain_name":"ingv","created_at":"2014-07-27T18:56:54.386-07:00","display_name":"Claudia D'Oriano","url":"https://ingv.academia.edu/CDOriano"},"attachments":[{"id":35228999,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/35228999/thumbnails/1.jpg","file_name":"DOriano_et_al_CMP2012.pdf","download_url":"https://www.academia.edu/attachments/35228999/download_file","bulk_download_file_name":"Effects_of_experimental_reheating_of_nat.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/35228999/DOriano_et_al_CMP2012-libre.pdf?1413948071=\u0026response-content-disposition=attachment%3B+filename%3DEffects_of_experimental_reheating_of_nat.pdf\u0026Expires=1743974710\u0026Signature=VoHgJlq-uWPQirTjUiWLf5zkXJANZ94l8eRIdHV4L9SR6D2n4ql0uxSDF5h-leQ-l-HjMPa7BZnwKRRuOvv~V5ZjKissF4h0XIwS0Z0HUkh-xzK1XuMSoJSMPVz5luUSMBpet-KHYiBswMPiDjva-QA10U8x6QpEA4wQQoqKnkncsfhfsCPldnMIUu0VDiMrsluVdEuQ-VM5AfxnEsTFQjHG0kp1Jj-xNH3yqTawctZDFlGiw4nkLpRTfl7U8MaBEYbwwlhChqyl9cQhZjifPdYdD7o3NJeL8wirtEkXqUpkWSdbhmJGzE8FW8KITBdgh8~JT25EoFaECGF8ADJXBQ__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":51810,"name":"Experimental petrology and volcanology","url":"https://www.academia.edu/Documents/in/Experimental_petrology_and_volcanology"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-8899826-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="8899802"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/8899802/Identifying_recycled_ash_in_basaltic_eruptions"><img alt="Research paper thumbnail of Identifying recycled ash in basaltic eruptions" class="work-thumbnail" src="https://attachments.academia-assets.com/35228958/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/8899802/Identifying_recycled_ash_in_basaltic_eruptions">Identifying recycled ash in basaltic eruptions</a></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Deposits of mid-intensity basaltic explosive eruptions are characterized by the coexistence of di...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Deposits of mid-intensity basaltic explosive eruptions are characterized by the coexistence of different types<br />of juvenile clasts, which show a large variability of external properties and texture, reflecting alternatively the<br />effects of primary processes related to magma storage or ascent, or of syn-eruptive modifications occurred<br />during or immediately after their ejection. If fragments fall back within the crater area before being<br />re-ejected during the ensuing activity, they are subject to thermally- and chemically-induced alterations.<br />These ‘recycled’ clasts can be considered as cognate lithic for the eruption/explosion they derive. Their exact<br />identification has consequences for a correct interpretation of eruption dynamics, with important<br />implications for hazard assessment. On ash erupted during selected basaltic eruptions (at Stromboli, Etna,<br />Vesuvius, Gaua-Vanuatu), we have identified a set of characteristics that can be associated with the<br />occurrence of intra-crater recycling processes, based also on the comparison with results of reheating<br />experiments performed on primary juvenile material, at variable temperature and under different redox<br />conditions.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="b71721d64f6e7df7aa71cb510e7ba252" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":35228958,"asset_id":8899802,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/35228958/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="8899802"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="8899802"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 8899802; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=8899802]").text(description); $(".js-view-count[data-work-id=8899802]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 8899802; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='8899802']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "b71721d64f6e7df7aa71cb510e7ba252" } } $('.js-work-strip[data-work-id=8899802]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":8899802,"title":"Identifying recycled ash in basaltic eruptions","translated_title":"","metadata":{"abstract":"Deposits of mid-intensity basaltic explosive eruptions are characterized by the coexistence of different types\nof juvenile clasts, which show a large variability of external properties and texture, reflecting alternatively the\neffects of primary processes related to magma storage or ascent, or of syn-eruptive modifications occurred\nduring or immediately after their ejection. If fragments fall back within the crater area before being\nre-ejected during the ensuing activity, they are subject to thermally- and chemically-induced alterations.\nThese ‘recycled’ clasts can be considered as cognate lithic for the eruption/explosion they derive. Their exact\nidentification has consequences for a correct interpretation of eruption dynamics, with important\nimplications for hazard assessment. On ash erupted during selected basaltic eruptions (at Stromboli, Etna,\nVesuvius, Gaua-Vanuatu), we have identified a set of characteristics that can be associated with the\noccurrence of intra-crater recycling processes, based also on the comparison with results of reheating\nexperiments performed on primary juvenile material, at variable temperature and under different redox\nconditions.","ai_title_tag":"Identifying Recycled Ash in Basaltic Explosions"},"translated_abstract":"Deposits of mid-intensity basaltic explosive eruptions are characterized by the coexistence of different types\nof juvenile clasts, which show a large variability of external properties and texture, reflecting alternatively the\neffects of primary processes related to magma storage or ascent, or of syn-eruptive modifications occurred\nduring or immediately after their ejection. If fragments fall back within the crater area before being\nre-ejected during the ensuing activity, they are subject to thermally- and chemically-induced alterations.\nThese ‘recycled’ clasts can be considered as cognate lithic for the eruption/explosion they derive. Their exact\nidentification has consequences for a correct interpretation of eruption dynamics, with important\nimplications for hazard assessment. On ash erupted during selected basaltic eruptions (at Stromboli, Etna,\nVesuvius, Gaua-Vanuatu), we have identified a set of characteristics that can be associated with the\noccurrence of intra-crater recycling processes, based also on the comparison with results of reheating\nexperiments performed on primary juvenile material, at variable temperature and under different redox\nconditions.","internal_url":"https://www.academia.edu/8899802/Identifying_recycled_ash_in_basaltic_eruptions","translated_internal_url":"","created_at":"2014-10-21T20:19:49.210-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":14420859,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":18172533,"work_id":8899802,"tagging_user_id":14420859,"tagged_user_id":1501609,"co_author_invite_id":null,"email":"p***o@pi.ingv.it","affiliation":"Istituto Nazionale di Geofisica e Vulcanologia","display_order":0,"name":"Massimo Pompilio","title":"Identifying recycled ash in basaltic eruptions"},{"id":18172541,"work_id":8899802,"tagging_user_id":14420859,"tagged_user_id":36210384,"co_author_invite_id":null,"email":"a***i@ingv.it","display_order":4194304,"name":"A. 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If fragments fall back within the crater area before being\nre-ejected during the ensuing activity, they are subject to thermally- and chemically-induced alterations.\nThese ‘recycled’ clasts can be considered as cognate lithic for the eruption/explosion they derive. Their exact\nidentification has consequences for a correct interpretation of eruption dynamics, with important\nimplications for hazard assessment. On ash erupted during selected basaltic eruptions (at Stromboli, Etna,\nVesuvius, Gaua-Vanuatu), we have identified a set of characteristics that can be associated with the\noccurrence of intra-crater recycling processes, based also on the comparison with results of reheating\nexperiments performed on primary juvenile material, at variable temperature and under different redox\nconditions.","impression_tracking_id":null,"owner":{"id":14420859,"first_name":"Claudia","middle_initials":null,"last_name":"D'Oriano","page_name":"CDOriano","domain_name":"ingv","created_at":"2014-07-27T18:56:54.386-07:00","display_name":"Claudia D'Oriano","url":"https://ingv.academia.edu/CDOriano"},"attachments":[{"id":35228958,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/35228958/thumbnails/1.jpg","file_name":"DOriano_et_al_SciRep_2014.pdf","download_url":"https://www.academia.edu/attachments/35228958/download_file","bulk_download_file_name":"Identifying_recycled_ash_in_basaltic_eru.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/35228958/DOriano_et_al_SciRep_2014-libre.pdf?1413947939=\u0026response-content-disposition=attachment%3B+filename%3DIdentifying_recycled_ash_in_basaltic_eru.pdf\u0026Expires=1743974710\u0026Signature=E0N3Zr1srxluAyD76EnYy4U9R0j96RQsTTjVFqzEHinWYIrAwI2apc5J01~UG0JP5mTfCm-fHwFEtslXS8Rjy8nkGo1rzmGjJEAse0wmjrgmjyvRjq3oDOxm4J7DhA4wN8QrjIbu0d1ByGGv46zXX1UmRUILi0KIv2Gf8ia7jA-vNv3sm1vjZpsJ~WpDsk62~8ie2pTdW~yp96iJc98z9RKx54uYw893uEViQDy6d2MUv59V8~v0uOihDIXAEFwZwArtZKVSi3U9n~pTR~ZWqD2acUPYcDIgysj-8HrcSqYhPq~LmZiPwymyrxTUd0PN5P-C0SQUyl-KwKguRDm5dA__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":1370,"name":"Volcanology","url":"https://www.academia.edu/Documents/in/Volcanology"},{"id":45291,"name":"Volcano monitoring","url":"https://www.academia.edu/Documents/in/Volcano_monitoring"},{"id":206238,"name":"Volcanic ash","url":"https://www.academia.edu/Documents/in/Volcanic_ash"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-8899802-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="7794657"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/7794657/Oxygen_isotope_geochemistry_of_mafic_magmas_at_Mt_Vesuvius"><img alt="Research paper thumbnail of Oxygen isotope geochemistry of mafic magmas at Mt. Vesuvius" class="work-thumbnail" src="https://attachments.academia-assets.com/48339158/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/7794657/Oxygen_isotope_geochemistry_of_mafic_magmas_at_Mt_Vesuvius">Oxygen isotope geochemistry of mafic magmas at Mt. Vesuvius</a></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Pumice and scoria from different eruptive layers of Mt. Vesuvius volcanic products contain mafic ...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Pumice and scoria from different eruptive layers of Mt. Vesuvius volcanic products contain mafic minerals consisting of High-Fo olivine and Diopsidic Pyroxene. These phases were crystallized in unerupted trachibasaltic to tephritic magmas, and were brought to surface by large phonolitic/tephri-phonolitic (e.g. Avellino and Pompei) and/or of tephritic and phono-tephritic (Pollena) eruptions. A large set of these mm-sized crystals was accurately separated from selected juvenile material and measured for their chemical compositions (EPMA, Laser Ablation ICP-MS) and 18O/16O ratios (conventional laser fluorination) to constrain the nature and evolution of the primary magmas at Mt. Vesuvius. Uncontaminated mantle δ18O values are hardly recovered in Italian Quaternary magmas, mostly due to the widespread occurrence of crustal contamination of the primary melts during their ascent to the surface (e.g. Alban Hills, Ernici Mts., and Aeolian Islands). At Mt. Vesuvius, measured olivine and clinopyroxene share quite homogeneous chemical compositions (Olivine Fo 85-90 ; Diopside En 45-48, respectively), and represent phases crystallized in near primary mafic magmas. Trace element composition constrains the near primary nature of the phases. Published data on volatile content of melt inclusions hosted in these crystals reveal the coexistence of dissolved water and carbon dioxide, and a minimum trapping pressure around 200-300 MPa, suggesting that crystal growth occurred in a reservoir at about 8-10 km depth. Recently, experimental data have suggested massive carbonate assimilation (up to about 20%) to derive potassic alkali magmas from trachybasaltic melts. Accordingly, the δ18O variability and the trace element content of the studied minerals suggest possible contamination of primary melts by an O-isotope enriched, REE-poor contaminant like the limestone of Vesuvius basement. Low, nearly primitive δ18O values are observed for olivine from Pompeii eruption, although still above the range of typical mantle minerals. The δ18Oolivine and δ18Ocpxof the minerals from all the studied eruptions define variable degrees of carbonate interaction and magma crystallization for the different eruptions, and possibly within the same eruption, and show evidence of oxygen isotope equilibrium at high temperature. However, energy-constrained AFC model suggest that carbonate assimilation was limited. On the basis of our data, we suggest that interaction between magma and a fluxing, decarbonation-derived CO2 fluid may be partly accounted for the measured O-isotope compositions.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="8f00255810159f42493cbcf82fd3fb3d" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":48339158,"asset_id":7794657,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/48339158/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="7794657"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="7794657"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 7794657; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=7794657]").text(description); $(".js-view-count[data-work-id=7794657]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 7794657; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='7794657']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "8f00255810159f42493cbcf82fd3fb3d" } } $('.js-work-strip[data-work-id=7794657]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":7794657,"title":"Oxygen isotope geochemistry of mafic magmas at Mt. Vesuvius","translated_title":"","metadata":{"abstract":"Pumice and scoria from different eruptive layers of Mt. Vesuvius volcanic products contain mafic minerals consisting of High-Fo olivine and Diopsidic Pyroxene. These phases were crystallized in unerupted trachibasaltic to tephritic magmas, and were brought to surface by large phonolitic/tephri-phonolitic (e.g. Avellino and Pompei) and/or of tephritic and phono-tephritic (Pollena) eruptions. A large set of these mm-sized crystals was accurately separated from selected juvenile material and measured for their chemical compositions (EPMA, Laser Ablation ICP-MS) and 18O/16O ratios (conventional laser fluorination) to constrain the nature and evolution of the primary magmas at Mt. Vesuvius. Uncontaminated mantle δ18O values are hardly recovered in Italian Quaternary magmas, mostly due to the widespread occurrence of crustal contamination of the primary melts during their ascent to the surface (e.g. Alban Hills, Ernici Mts., and Aeolian Islands). At Mt. Vesuvius, measured olivine and clinopyroxene share quite homogeneous chemical compositions (Olivine Fo 85-90 ; Diopside En 45-48, respectively), and represent phases crystallized in near primary mafic magmas. Trace element composition constrains the near primary nature of the phases. Published data on volatile content of melt inclusions hosted in these crystals reveal the coexistence of dissolved water and carbon dioxide, and a minimum trapping pressure around 200-300 MPa, suggesting that crystal growth occurred in a reservoir at about 8-10 km depth. Recently, experimental data have suggested massive carbonate assimilation (up to about 20%) to derive potassic alkali magmas from trachybasaltic melts. Accordingly, the δ18O variability and the trace element content of the studied minerals suggest possible contamination of primary melts by an O-isotope enriched, REE-poor contaminant like the limestone of Vesuvius basement. Low, nearly primitive δ18O values are observed for olivine from Pompeii eruption, although still above the range of typical mantle minerals. The δ18Oolivine and δ18Ocpxof the minerals from all the studied eruptions define variable degrees of carbonate interaction and magma crystallization for the different eruptions, and possibly within the same eruption, and show evidence of oxygen isotope equilibrium at high temperature. However, energy-constrained AFC model suggest that carbonate assimilation was limited. On the basis of our data, we suggest that interaction between magma and a fluxing, decarbonation-derived CO2 fluid may be partly accounted for the measured O-isotope compositions.","publication_date":{"day":null,"month":null,"year":2010,"errors":{}}},"translated_abstract":"Pumice and scoria from different eruptive layers of Mt. Vesuvius volcanic products contain mafic minerals consisting of High-Fo olivine and Diopsidic Pyroxene. These phases were crystallized in unerupted trachibasaltic to tephritic magmas, and were brought to surface by large phonolitic/tephri-phonolitic (e.g. Avellino and Pompei) and/or of tephritic and phono-tephritic (Pollena) eruptions. A large set of these mm-sized crystals was accurately separated from selected juvenile material and measured for their chemical compositions (EPMA, Laser Ablation ICP-MS) and 18O/16O ratios (conventional laser fluorination) to constrain the nature and evolution of the primary magmas at Mt. Vesuvius. Uncontaminated mantle δ18O values are hardly recovered in Italian Quaternary magmas, mostly due to the widespread occurrence of crustal contamination of the primary melts during their ascent to the surface (e.g. Alban Hills, Ernici Mts., and Aeolian Islands). At Mt. Vesuvius, measured olivine and clinopyroxene share quite homogeneous chemical compositions (Olivine Fo 85-90 ; Diopside En 45-48, respectively), and represent phases crystallized in near primary mafic magmas. Trace element composition constrains the near primary nature of the phases. Published data on volatile content of melt inclusions hosted in these crystals reveal the coexistence of dissolved water and carbon dioxide, and a minimum trapping pressure around 200-300 MPa, suggesting that crystal growth occurred in a reservoir at about 8-10 km depth. Recently, experimental data have suggested massive carbonate assimilation (up to about 20%) to derive potassic alkali magmas from trachybasaltic melts. Accordingly, the δ18O variability and the trace element content of the studied minerals suggest possible contamination of primary melts by an O-isotope enriched, REE-poor contaminant like the limestone of Vesuvius basement. Low, nearly primitive δ18O values are observed for olivine from Pompeii eruption, although still above the range of typical mantle minerals. The δ18Oolivine and δ18Ocpxof the minerals from all the studied eruptions define variable degrees of carbonate interaction and magma crystallization for the different eruptions, and possibly within the same eruption, and show evidence of oxygen isotope equilibrium at high temperature. However, energy-constrained AFC model suggest that carbonate assimilation was limited. On the basis of our data, we suggest that interaction between magma and a fluxing, decarbonation-derived CO2 fluid may be partly accounted for the measured O-isotope compositions.","internal_url":"https://www.academia.edu/7794657/Oxygen_isotope_geochemistry_of_mafic_magmas_at_Mt_Vesuvius","translated_internal_url":"","created_at":"2014-07-27T18:57:42.704-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":14420859,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":18172544,"work_id":7794657,"tagging_user_id":14420859,"tagged_user_id":null,"co_author_invite_id":298986,"email":"r***i@unica.it","display_order":0,"name":"Raffaello Cioni","title":"Oxygen isotope geochemistry of mafic magmas at Mt. 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Vesuvius volcanic products contain mafic minerals consisting of High-Fo olivine and Diopsidic Pyroxene. These phases were crystallized in unerupted trachibasaltic to tephritic magmas, and were brought to surface by large phonolitic/tephri-phonolitic (e.g. Avellino and Pompei) and/or of tephritic and phono-tephritic (Pollena) eruptions. A large set of these mm-sized crystals was accurately separated from selected juvenile material and measured for their chemical compositions (EPMA, Laser Ablation ICP-MS) and 18O/16O ratios (conventional laser fluorination) to constrain the nature and evolution of the primary magmas at Mt. Vesuvius. Uncontaminated mantle δ18O values are hardly recovered in Italian Quaternary magmas, mostly due to the widespread occurrence of crustal contamination of the primary melts during their ascent to the surface (e.g. Alban Hills, Ernici Mts., and Aeolian Islands). At Mt. Vesuvius, measured olivine and clinopyroxene share quite homogeneous chemical compositions (Olivine Fo 85-90 ; Diopside En 45-48, respectively), and represent phases crystallized in near primary mafic magmas. Trace element composition constrains the near primary nature of the phases. Published data on volatile content of melt inclusions hosted in these crystals reveal the coexistence of dissolved water and carbon dioxide, and a minimum trapping pressure around 200-300 MPa, suggesting that crystal growth occurred in a reservoir at about 8-10 km depth. Recently, experimental data have suggested massive carbonate assimilation (up to about 20%) to derive potassic alkali magmas from trachybasaltic melts. Accordingly, the δ18O variability and the trace element content of the studied minerals suggest possible contamination of primary melts by an O-isotope enriched, REE-poor contaminant like the limestone of Vesuvius basement. Low, nearly primitive δ18O values are observed for olivine from Pompeii eruption, although still above the range of typical mantle minerals. The δ18Oolivine and δ18Ocpxof the minerals from all the studied eruptions define variable degrees of carbonate interaction and magma crystallization for the different eruptions, and possibly within the same eruption, and show evidence of oxygen isotope equilibrium at high temperature. However, energy-constrained AFC model suggest that carbonate assimilation was limited. On the basis of our data, we suggest that interaction between magma and a fluxing, decarbonation-derived CO2 fluid may be partly accounted for the measured O-isotope compositions.","impression_tracking_id":null,"owner":{"id":14420859,"first_name":"Claudia","middle_initials":null,"last_name":"D'Oriano","page_name":"CDOriano","domain_name":"ingv","created_at":"2014-07-27T18:56:54.386-07:00","display_name":"Claudia D'Oriano","url":"https://ingv.academia.edu/CDOriano"},"attachments":[{"id":48339158,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/48339158/thumbnails/1.jpg","file_name":"Oxygen_isotope_geochemistry_of_mafic_mag20160826-2946-al5ixx.pdf","download_url":"https://www.academia.edu/attachments/48339158/download_file","bulk_download_file_name":"Oxygen_isotope_geochemistry_of_mafic_mag.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/48339158/Oxygen_isotope_geochemistry_of_mafic_mag20160826-2946-al5ixx-libre.pdf?1472233363=\u0026response-content-disposition=attachment%3B+filename%3DOxygen_isotope_geochemistry_of_mafic_mag.pdf\u0026Expires=1743974711\u0026Signature=ASUTIw7f0DBbBXMrLufDmHyrfkmCmLOCuWdWYcEFlwaAa0ofDhUhJAuQ~O~tDflNfhnd~owHmPsPIAFBFqYSNmvy4HqbPOQineNpdTl30saSpDR6hUMxx-tx22INmO6I5IcBTegGGsg6MFVHAaUNta9qjIhjPNXunHxALLMHvBARIqbz~sdRwzA8nhyRiFI7cYCOWdvbx9xIJljjmId2XysKKZn5FD2GobSGnXcCz2ePpMBjGtnlC3sppu~e3r1-VK0pg91wzfFO9n3u72nvL2F-tx2ezww-pxmwXyZOiTAEuFPtCfyR4jBZawcQbXONJaBvOw3gk~hCC2gc7FPnaA__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":30929,"name":"Eruption Mechanisms","url":"https://www.academia.edu/Documents/in/Eruption_Mechanisms"},{"id":78128,"name":"Vesuvius","url":"https://www.academia.edu/Documents/in/Vesuvius"},{"id":230706,"name":"Volcanic degassing","url":"https://www.academia.edu/Documents/in/Volcanic_degassing"}],"urls":[{"id":3249161,"url":"http://adsabs.harvard.edu/abs/2010EGUGA..1211515D"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-7794657-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="7794655"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/7794655/Carbonate_derived_CO2_purging_magma_at_depth_Influence_on_the_eruptive_activity_of_Somma_Vesuvius_Italy"><img alt="Research paper thumbnail of Carbonate-derived CO2 purging magma at depth: Influence on the eruptive activity of Somma-Vesuvius, Italy" class="work-thumbnail" src="https://attachments.academia-assets.com/48339149/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/7794655/Carbonate_derived_CO2_purging_magma_at_depth_Influence_on_the_eruptive_activity_of_Somma_Vesuvius_Italy">Carbonate-derived CO2 purging magma at depth: Influence on the eruptive activity of Somma-Vesuvius, Italy</a></div><div class="wp-workCard_item"><span>Earth and Planetary Science Letters</span><span>, 2011</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Mafic phenocrysts from selected products of the last 4 ka volcanic activity at Mt. Vesuvius were ...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Mafic phenocrysts from selected products of the last 4 ka volcanic activity at Mt. Vesuvius were investigated for their chemical and O-isotope composition, as a proxy for primary magmas feeding the system. 18O/ 16O ratios of studied Mg-rich olivines suggest that near-primary shoshonitic to tephritic melts experienced a flux of sedimentary carbonate-derived CO 2, representing the early process of magma contamination in the roots of the volcanic structure. Bulk carbonate assimilation (physical digestion) mainly occurred in the shallow crust, strongly influencing magma chamber evolution. On a petrological and geochemical basis the effects of bulk sedimentary carbonate digestion on the chemical composition of the near-primary melts are resolved from those of carbonate-released CO 2 fluxed into magma. An important outcome of this process lies in the effect of external CO 2 in changing the overall volatile solubility of the magma, enhancing the ability of Vesuvius mafic magmas to rapidly rise and explosively erupt at the surface.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="0ba8df901faeaf925b0a3c91f538412e" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":48339149,"asset_id":7794655,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/48339149/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="7794655"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="7794655"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 7794655; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=7794655]").text(description); $(".js-view-count[data-work-id=7794655]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 7794655; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='7794655']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "0ba8df901faeaf925b0a3c91f538412e" } } $('.js-work-strip[data-work-id=7794655]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":7794655,"title":"Carbonate-derived CO2 purging magma at depth: Influence on the eruptive activity of Somma-Vesuvius, Italy","translated_title":"","metadata":{"abstract":"Mafic phenocrysts from selected products of the last 4 ka volcanic activity at Mt. Vesuvius were investigated for their chemical and O-isotope composition, as a proxy for primary magmas feeding the system. 18O/ 16O ratios of studied Mg-rich olivines suggest that near-primary shoshonitic to tephritic melts experienced a flux of sedimentary carbonate-derived CO 2, representing the early process of magma contamination in the roots of the volcanic structure. Bulk carbonate assimilation (physical digestion) mainly occurred in the shallow crust, strongly influencing magma chamber evolution. On a petrological and geochemical basis the effects of bulk sedimentary carbonate digestion on the chemical composition of the near-primary melts are resolved from those of carbonate-released CO 2 fluxed into magma. An important outcome of this process lies in the effect of external CO 2 in changing the overall volatile solubility of the magma, enhancing the ability of Vesuvius mafic magmas to rapidly rise and explosively erupt at the surface.","ai_title_tag":"Influence of Carbonate-derived CO2 on Vesuvius Eruptions","publication_date":{"day":null,"month":null,"year":2011,"errors":{}},"publication_name":"Earth and Planetary Science Letters"},"translated_abstract":"Mafic phenocrysts from selected products of the last 4 ka volcanic activity at Mt. Vesuvius were investigated for their chemical and O-isotope composition, as a proxy for primary magmas feeding the system. 18O/ 16O ratios of studied Mg-rich olivines suggest that near-primary shoshonitic to tephritic melts experienced a flux of sedimentary carbonate-derived CO 2, representing the early process of magma contamination in the roots of the volcanic structure. Bulk carbonate assimilation (physical digestion) mainly occurred in the shallow crust, strongly influencing magma chamber evolution. On a petrological and geochemical basis the effects of bulk sedimentary carbonate digestion on the chemical composition of the near-primary melts are resolved from those of carbonate-released CO 2 fluxed into magma. An important outcome of this process lies in the effect of external CO 2 in changing the overall volatile solubility of the magma, enhancing the ability of Vesuvius mafic magmas to rapidly rise and explosively erupt at the surface.","internal_url":"https://www.academia.edu/7794655/Carbonate_derived_CO2_purging_magma_at_depth_Influence_on_the_eruptive_activity_of_Somma_Vesuvius_Italy","translated_internal_url":"","created_at":"2014-07-27T18:57:27.461-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":14420859,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":18172527,"work_id":7794655,"tagging_user_id":14420859,"tagged_user_id":null,"co_author_invite_id":2805600,"email":"c***i@igg.cnr.it","display_order":0,"name":"Chiara Boschi","title":"Carbonate-derived CO2 purging magma at depth: Influence on the eruptive activity of Somma-Vesuvius, Italy"},{"id":18172530,"work_id":7794655,"tagging_user_id":14420859,"tagged_user_id":null,"co_author_invite_id":1114070,"email":"d***i@igg.cnr.it","display_order":4194304,"name":"Luigi Dallai","title":"Carbonate-derived CO2 purging magma at depth: Influence on the eruptive activity of Somma-Vesuvius, Italy"},{"id":18172536,"work_id":7794655,"tagging_user_id":14420859,"tagged_user_id":32521915,"co_author_invite_id":null,"email":"r***i@unifi.it","display_order":6291456,"name":"R. 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Vesuvius were investigated for their chemical and O-isotope composition, as a proxy for primary magmas feeding the system. 18O/ 16O ratios of studied Mg-rich olivines suggest that near-primary shoshonitic to tephritic melts experienced a flux of sedimentary carbonate-derived CO 2, representing the early process of magma contamination in the roots of the volcanic structure. Bulk carbonate assimilation (physical digestion) mainly occurred in the shallow crust, strongly influencing magma chamber evolution. On a petrological and geochemical basis the effects of bulk sedimentary carbonate digestion on the chemical composition of the near-primary melts are resolved from those of carbonate-released CO 2 fluxed into magma. 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The recognition of juvenile vs. recycled fragments is not straightforward, and no unequivocal, widely accepted criteria exist to support this. The presence of recycled glassy fragments can hide primary magmatic information, introducing bias in the interpretations of the ongoing magmatic and volcanic activity. High temperature experiments were performed at atmospheric pressure on natural samples to investigate the effects of reheating on morphology, texture and composition of volcanic ash. Experiments simulate the transformation of juvenile glassy fragments that, falling into the crater or in the upper part of the conduit, are recycled by following explosions. Textural and compositional modifications obtained in laboratory are compared with similar features observed in natural samples in order to identify some main general criteria to be used for the discrimination of recycled material. Experiments were carried out on tephra produced during Strombolian activity, fire fountains and continuous ash emission at Etna, Stromboli and Vesuvius. Coarse glassy clasts were crushed in a nylon mortar in order to create an artificial ash, and then sieved to select the size interval of 1-0.71 mm. Ash shards were put in a sealed or open quartz tube, in order to prevent or to reproduce effects of air oxidation. The tube was suspended in a HT furnace at INGV-Pisa and kept at different temperatures (up to to 1110°C) for increasing time (0.5-12 hours). Preliminary experiments were also performed under gas flux conditions. Optical and electron microscope observations indicate that high temperature and exposure to the air induce large modifications on clast surface, ranging from change in color, to incipient plastic deformation till complete sintering. Significant change in color of clasts is strictly related to the presence of air, irrespective of temperature while sintering is favored by the high temperature and low fO2. Re-heating promotes nucleation and growth of crystals in the groundmass and associated change of glass composition, sometimes accompanied by growth and coalescence of vesicles in the size of 10-50 µm and cracking of the external surface.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="7794654"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="7794654"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 7794654; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=7794654]").text(description); $(".js-view-count[data-work-id=7794654]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 7794654; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='7794654']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=7794654]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":7794654,"title":"Simulating intracrater ash recycling during mid-intensity explosive activity: high temperature laboratory experiments on natural basaltic ash","translated_title":"","metadata":{"abstract":"Direct observations of mid-intensity eruptions, in which a huge amount of ash is generated, indicate that ash recycling is quite common. The recognition of juvenile vs. recycled fragments is not straightforward, and no unequivocal, widely accepted criteria exist to support this. The presence of recycled glassy fragments can hide primary magmatic information, introducing bias in the interpretations of the ongoing magmatic and volcanic activity. High temperature experiments were performed at atmospheric pressure on natural samples to investigate the effects of reheating on morphology, texture and composition of volcanic ash. Experiments simulate the transformation of juvenile glassy fragments that, falling into the crater or in the upper part of the conduit, are recycled by following explosions. Textural and compositional modifications obtained in laboratory are compared with similar features observed in natural samples in order to identify some main general criteria to be used for the discrimination of recycled material. Experiments were carried out on tephra produced during Strombolian activity, fire fountains and continuous ash emission at Etna, Stromboli and Vesuvius. Coarse glassy clasts were crushed in a nylon mortar in order to create an artificial ash, and then sieved to select the size interval of 1-0.71 mm. Ash shards were put in a sealed or open quartz tube, in order to prevent or to reproduce effects of air oxidation. The tube was suspended in a HT furnace at INGV-Pisa and kept at different temperatures (up to to 1110°C) for increasing time (0.5-12 hours). Preliminary experiments were also performed under gas flux conditions. Optical and electron microscope observations indicate that high temperature and exposure to the air induce large modifications on clast surface, ranging from change in color, to incipient plastic deformation till complete sintering. Significant change in color of clasts is strictly related to the presence of air, irrespective of temperature while sintering is favored by the high temperature and low fO2. Re-heating promotes nucleation and growth of crystals in the groundmass and associated change of glass composition, sometimes accompanied by growth and coalescence of vesicles in the size of 10-50 µm and cracking of the external surface.","publication_date":{"day":null,"month":null,"year":2010,"errors":{}}},"translated_abstract":"Direct observations of mid-intensity eruptions, in which a huge amount of ash is generated, indicate that ash recycling is quite common. The recognition of juvenile vs. recycled fragments is not straightforward, and no unequivocal, widely accepted criteria exist to support this. The presence of recycled glassy fragments can hide primary magmatic information, introducing bias in the interpretations of the ongoing magmatic and volcanic activity. High temperature experiments were performed at atmospheric pressure on natural samples to investigate the effects of reheating on morphology, texture and composition of volcanic ash. Experiments simulate the transformation of juvenile glassy fragments that, falling into the crater or in the upper part of the conduit, are recycled by following explosions. Textural and compositional modifications obtained in laboratory are compared with similar features observed in natural samples in order to identify some main general criteria to be used for the discrimination of recycled material. Experiments were carried out on tephra produced during Strombolian activity, fire fountains and continuous ash emission at Etna, Stromboli and Vesuvius. Coarse glassy clasts were crushed in a nylon mortar in order to create an artificial ash, and then sieved to select the size interval of 1-0.71 mm. Ash shards were put in a sealed or open quartz tube, in order to prevent or to reproduce effects of air oxidation. The tube was suspended in a HT furnace at INGV-Pisa and kept at different temperatures (up to to 1110°C) for increasing time (0.5-12 hours). Preliminary experiments were also performed under gas flux conditions. Optical and electron microscope observations indicate that high temperature and exposure to the air induce large modifications on clast surface, ranging from change in color, to incipient plastic deformation till complete sintering. Significant change in color of clasts is strictly related to the presence of air, irrespective of temperature while sintering is favored by the high temperature and low fO2. Re-heating promotes nucleation and growth of crystals in the groundmass and associated change of glass composition, sometimes accompanied by growth and coalescence of vesicles in the size of 10-50 µm and cracking of the external surface.","internal_url":"https://www.academia.edu/7794654/Simulating_intracrater_ash_recycling_during_mid_intensity_explosive_activity_high_temperature_laboratory_experiments_on_natural_basaltic_ash","translated_internal_url":"","created_at":"2014-07-27T18:57:27.341-07:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":14420859,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[{"id":18172532,"work_id":7794654,"tagging_user_id":14420859,"tagged_user_id":1501609,"co_author_invite_id":null,"email":"p***o@pi.ingv.it","affiliation":"Istituto Nazionale di Geofisica e Vulcanologia","display_order":0,"name":"Massimo Pompilio","title":"Simulating intracrater ash recycling during mid-intensity explosive activity: high temperature laboratory experiments on natural basaltic ash"},{"id":18172540,"work_id":7794654,"tagging_user_id":14420859,"tagged_user_id":36210384,"co_author_invite_id":null,"email":"a***i@ingv.it","display_order":4194304,"name":"A. Bertagnini","title":"Simulating intracrater ash recycling during mid-intensity explosive activity: high temperature laboratory experiments on natural basaltic ash"},{"id":18172543,"work_id":7794654,"tagging_user_id":14420859,"tagged_user_id":null,"co_author_invite_id":298986,"email":"r***i@unica.it","display_order":6291456,"name":"Raffaello Cioni","title":"Simulating intracrater ash recycling during mid-intensity explosive activity: high temperature laboratory experiments on natural basaltic ash"}],"downloadable_attachments":[],"slug":"Simulating_intracrater_ash_recycling_during_mid_intensity_explosive_activity_high_temperature_laboratory_experiments_on_natural_basaltic_ash","translated_slug":"","page_count":null,"language":"en","content_type":"Work","summary":"Direct observations of mid-intensity eruptions, in which a huge amount of ash is generated, indicate that ash recycling is quite common. The recognition of juvenile vs. recycled fragments is not straightforward, and no unequivocal, widely accepted criteria exist to support this. The presence of recycled glassy fragments can hide primary magmatic information, introducing bias in the interpretations of the ongoing magmatic and volcanic activity. High temperature experiments were performed at atmospheric pressure on natural samples to investigate the effects of reheating on morphology, texture and composition of volcanic ash. Experiments simulate the transformation of juvenile glassy fragments that, falling into the crater or in the upper part of the conduit, are recycled by following explosions. Textural and compositional modifications obtained in laboratory are compared with similar features observed in natural samples in order to identify some main general criteria to be used for the discrimination of recycled material. Experiments were carried out on tephra produced during Strombolian activity, fire fountains and continuous ash emission at Etna, Stromboli and Vesuvius. Coarse glassy clasts were crushed in a nylon mortar in order to create an artificial ash, and then sieved to select the size interval of 1-0.71 mm. Ash shards were put in a sealed or open quartz tube, in order to prevent or to reproduce effects of air oxidation. The tube was suspended in a HT furnace at INGV-Pisa and kept at different temperatures (up to to 1110°C) for increasing time (0.5-12 hours). Preliminary experiments were also performed under gas flux conditions. Optical and electron microscope observations indicate that high temperature and exposure to the air induce large modifications on clast surface, ranging from change in color, to incipient plastic deformation till complete sintering. Significant change in color of clasts is strictly related to the presence of air, irrespective of temperature while sintering is favored by the high temperature and low fO2. 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