<?xml version="1.0" encoding="ISO-8859-1"?><article xmlns:mml="http://www.w3.org/1998/Math/MathML" xmlns:xlink="http://www.w3.org/1999/xlink" xmlns:xsi="http://www.w3.org/2001/XMLSchema-instance">
<front>
<journal-meta>
<journal-id>0256-7024</journal-id>
<journal-title><![CDATA[Revista Geológica de América Central]]></journal-title>
<abbrev-journal-title><![CDATA[Rev. Geol. Amér. Central]]></abbrev-journal-title>
<issn>0256-7024</issn>
<publisher>
<publisher-name><![CDATA[Universidad de Costa Rica]]></publisher-name>
</publisher>
</journal-meta>
<article-meta>
<article-id>S0256-70242016000200007</article-id>
<article-id pub-id-type="doi">10.15517/rgac.v55i0.26965</article-id>
<title-group>
<article-title xml:lang="es"><![CDATA[La actividad explosiva del volcán Turrialba (Costa Rica) en el período 2010 - 2016]]></article-title>
<article-title xml:lang="en"><![CDATA[The explosive activity of Turrialba volcano (Costa Rica) in 2010 - 2016]]></article-title>
</title-group>
<contrib-group>
<contrib contrib-type="author">
<name>
<surname><![CDATA[Alvarado]]></surname>
<given-names><![CDATA[Guillermo E.]]></given-names>
</name>
<xref ref-type="aff" rid="Aff"/>
<xref ref-type="aff" rid="Aaf"/>
</contrib>
<contrib contrib-type="author">
<name>
<surname><![CDATA[Brenes-André]]></surname>
<given-names><![CDATA[José]]></given-names>
</name>
<xref ref-type="aff" rid="Aff"/>
</contrib>
<contrib contrib-type="author">
<name>
<surname><![CDATA[Barrantes]]></surname>
<given-names><![CDATA[Manuel]]></given-names>
</name>
<xref ref-type="aff" rid="Aff"/>
</contrib>
<contrib contrib-type="author">
<name>
<surname><![CDATA[Vega]]></surname>
<given-names><![CDATA[Eduardo]]></given-names>
</name>
<xref ref-type="aff" rid="Aff"/>
</contrib>
<contrib contrib-type="author">
<name>
<surname><![CDATA[de Moor]]></surname>
<given-names><![CDATA[J. Maarten]]></given-names>
</name>
<xref ref-type="aff" rid="Aff"/>
</contrib>
<contrib contrib-type="author">
<name>
<surname><![CDATA[Avard]]></surname>
<given-names><![CDATA[Geoffroy]]></given-names>
</name>
<xref ref-type="aff" rid="Aff"/>
</contrib>
<contrib contrib-type="author">
<name>
<surname><![CDATA[Dellino]]></surname>
<given-names><![CDATA[Pierfrancesco]]></given-names>
</name>
<xref ref-type="aff" rid="Aff"/>
</contrib>
<contrib contrib-type="author">
<name>
<surname><![CDATA[Mele]]></surname>
<given-names><![CDATA[Daniela]]></given-names>
</name>
<xref ref-type="aff" rid="Aff"/>
</contrib>
<contrib contrib-type="author">
<name>
<surname><![CDATA[DeVitre]]></surname>
<given-names><![CDATA[Charlotte]]></given-names>
</name>
<xref ref-type="aff" rid="Aff"/>
</contrib>
<contrib contrib-type="author">
<name>
<surname><![CDATA[Di Piazza]]></surname>
<given-names><![CDATA[Andrea]]></given-names>
</name>
<xref ref-type="aff" rid="Aff"/>
</contrib>
<contrib contrib-type="author">
<name>
<surname><![CDATA[Rizzo]]></surname>
<given-names><![CDATA[Andrea L.]]></given-names>
</name>
<xref ref-type="aff" rid="Aff"/>
</contrib>
<contrib contrib-type="author">
<name>
<surname><![CDATA[Carapezza]]></surname>
<given-names><![CDATA[Maria L.]]></given-names>
</name>
<xref ref-type="aff" rid="Aff"/>
</contrib>
</contrib-group>
<aff id="Af1">
<institution><![CDATA[,Instituto Costarricense de Electricidad  ]]></institution>
<addr-line><![CDATA[ ]]></addr-line>
<country>CR</country>
</aff>
<aff id="Af2">
<institution><![CDATA[,Red Ciudadana de Estaciones Meteorológicas  ]]></institution>
<addr-line><![CDATA[ ]]></addr-line>
<country>CR</country>
</aff>
<aff id="Af3">
<institution><![CDATA[,Universidad Nacional  ]]></institution>
<addr-line><![CDATA[ Heredia]]></addr-line>
<country>CR</country>
</aff>
<aff id="Af4">
<institution><![CDATA[,Università degli Studi di Bari  ]]></institution>
<addr-line><![CDATA[ Bari]]></addr-line>
<country>IT</country>
</aff>
<aff id="Af5">
<institution><![CDATA[,Red Sismológica Nacional  ]]></institution>
<addr-line><![CDATA[ ]]></addr-line>
<country>CR</country>
</aff>
<aff id="Af6">
<institution><![CDATA[,Istituto Nazionale di Geofisica e Vulcanologia  ]]></institution>
<addr-line><![CDATA[ Roma]]></addr-line>
<country>IT</country>
</aff>
<aff id="Af7">
<institution><![CDATA[,Istituto Nazionale di Geofisica e Vulcanologia  ]]></institution>
<addr-line><![CDATA[ Palermo]]></addr-line>
<country>IT</country>
</aff>
<pub-date pub-type="pub">
<day>00</day>
<month>12</month>
<year>2016</year>
</pub-date>
<pub-date pub-type="epub">
<day>00</day>
<month>12</month>
<year>2016</year>
</pub-date>
<numero>55</numero>
<fpage>7</fpage>
<lpage>60</lpage>
<copyright-statement/>
<copyright-year/>
<self-uri xlink:href="http://www.scielo.sa.cr/scielo.php?script=sci_arttext&amp;pid=S0256-70242016000200007&amp;lng=en&amp;nrm=iso"></self-uri><self-uri xlink:href="http://www.scielo.sa.cr/scielo.php?script=sci_abstract&amp;pid=S0256-70242016000200007&amp;lng=en&amp;nrm=iso"></self-uri><self-uri xlink:href="http://www.scielo.sa.cr/scielo.php?script=sci_pdf&amp;pid=S0256-70242016000200007&amp;lng=en&amp;nrm=iso"></self-uri><abstract abstract-type="short" xml:lang="es"><p><![CDATA[Resumen:La más reciente actividad eruptiva del volcán Turrialba se inició el 5 de enero de 2010, después de más de un siglo de estar dormido. El proceso de formación de cenizas emitidas (i.e., tipo de fragmentación) y el comportamiento aerodinámico de las mismas, se investigaron mediante la combinación de análisis granulométricos, petrografía óptica, análisis mineralógico, microscopía electrónica de barrido (SEM) y sistema de energía dispersiva (EDS). La ceniza estuvo compuesta por porcentajes variables de líticos accidentales, frescos (no necesariamente juveniles) a alterados hidrotermalmente (15 - 50 %), con minerales hidrotermales (1 - 8 % vol.: anhidrita, yeso, bassanita, alunita, hexahidrita, pirita, heulandita, azufre nativo), minerales de arcilla (8 - 17 %: montmorillonita, haloisita, alofana) y una menor cantidad de vidrio fresco (5 - 49 % vol.) como esquirlas y fragmentos (3 - 20% vol. taquilita y 2 - 26 % vol. sideromelana), fenocristales (3 - 13 % vol.), que pueden ser tanto juveniles como accesorios/reciclados (1 - 5 % vol. plagioclasa, 1 - 7 % vol. piroxeno, 0 - 1 % vol. olivino, 0 - 6 % vol. opacos, cristobalita y tridimita), y xenocristales (&#8804; 1 % vol.: riebeckita y biotita). Los minerales secundarios son el producto de la alteración hidrotermal profunda y de su expresión en el campo de fumarolas superficial. Las características texturales identificadas en partículas de ceniza finas (90 - 350 µm) sugieren que se formaron por la fragmentación debido a la interacción explosiva magma/agua. Las estructuras fundidas parecen estar relacionada con el comportamiento dúctil de las partículas sometidas a altas temperaturas (&gt; 600 ° C) en el sistema de fumarólico/magmático. El porcentaje del componente fresco fue bajo (1 - 2 % vol.) en la apertura del conducto eruptivo del 2010, incrementando paulatinamente hasta el presente (ca. 12 - 25 % vol. en 2013 - 2016). Las erupciones en el cráter Oeste, durante el 2014 al 2016, estuvieron relacionadas con una boca al inicio y después por dos o tres bocas simultáneamente activas. La alternancia de explosiones volcánicas (VEI: 0 - 2), desde conducto cerrado con la formación de nuevos cráteres, hasta un conducto abierto, y los intervalos de reposo (desgasificación exhalativa inter-eruptiva) fue controlado, posiblemente, por la velocidad a la que el magma poco vesiculado ascendió y se mantuvo en el edificio volcánico. Las tefras consisten en una sucesión compleja de capas generadas por corrientes de densidad piroclástica diluidas (principalmente oleadas húmedas), baja temperatura (&lt; 300 ºC), originadas por pulsos simples y cortos, por el colapso de columnas eruptivas freatomagmáticas, que viajaron cortas distancias (&lt; 1000 m) desde las bocas cratéricas, superando obstáculos, ocurridas simultáneamente con depósitos de caída piroclástica y emisión de proyectiles balísticos. El material fino en suspensión, en la parte superior de la columna convectiva, fue dispersado en la atmósfera y se sedimentó sobre el Valle Central. Los períodos de reposo podrían estar relacionados con un enfriamiento temporal del sistema de diques magmáticos o por una disminución de la actividad magmática en profundidad. La teoría de la fragmentación / transporte secuencial fue utilizada para deconvolucionar (desagregar) las granulometrías en 5 subpoblaciones, que fueron luego asociadas a mecanismos de fragmentación. Los casos en que se dio traslape de las modas fueron resueltos con una nueva manera de utilizar el coeficiente de fragmentación. Por primera vez se muestra que los resultados obtenidos, por el método mencionado, concuerdan con lo esperado de la erupciones freatomagmáticas, y con lo derivado a partir del modelo ab initio de fractura fractal.]]></p></abstract>
<abstract abstract-type="short" xml:lang="en"><p><![CDATA[Abstract:The most recent eruptive activity of Turrialba volcano began on the 5th of January 2010, after more than a century of dormancy. The fragmentation process and aerodynamic behavior of the ash from Turrialba's vulcanian eruptions were investigated by combining grain-size, petrography, mineralogy, Scanning Electron Microscopy (SEM) anhydrite, gypsum, bassanite, alunite, hexahydrite, pyrite, heulandite, native sulfur), clay minerals (8 - 17 % vol.: montmorillonite, halloysite, allophane), and a smaller quantity of fresh glassy ashes (5 - 49 % vol.) as fragments and shards (3 - 20 % vol. tackylite and 2 - 26 % vol. sideromelane), as well as primary and eroded/recycled phenocrysts (3 - 13 % vol.: 1 - 5% vol. plagioclase, 1 - 7 % vol. pyroxene, 0 - 1 % vol. olivine, 0 - 6 % vol. opaques, cristobalite and tridimite), and xenocrysts (&#8804; 1 % vol.: riebeckite and biotite). The secondary minerals were sourced from the deeper to surficial hydrothermal system. Textural features identified in ash particles (90 - 350 µm) suggest that they were formed by brittle fragmentation of vesicle-poor magma/water interaction; molten structures seems to be related to the ductile behavior of some fragments, probably due to the high temperature (&gt; 600 °C) of the fumarolic/magmatic system. The percentage of juvenile components was low (1 - 2 % vol.) at the first opening eruptive phase in January 2010, and it increased steadily until the end of 2016 (ca. 12 - 25 % vol.) . The ash eruptions in the Western Crater from 2014 to 2016 were related to one and later two or three simultaneously active vents fed by distinct conduit branches. The alternation of volcanic explosions (VEI: 0 - 2), from closed conduit and the formation of new craters, to open system with phreatomagmatic events, and the repose intervals (inter-eruptive exhalative degassing), were controlled by the rate at which magma ascended and remained in the volcanic edifice. The recent tephra sequence consists of a complex succession of layers generated by contrasting fragmentation and transportation dynamics. They resulted from fully diluted, low temperature (&lt; 300 °C), pyroclastic density currents (wet surge deposits), originated by short-lived, singlepulse, column collapse of phreatomagmatic columns, which traveled short distances (&lt; 1000 m) from the vent area and surmounted topographic obstacles, and simultaneous fallout and ballistic ejecta. The fine material, in continuous suspension within the uppermost part of the convective plume, was dispersed into the atmosphere and finally settled down on the Valle Central. The quiescent phases could be related to a temporal cooling of the magmatic dike system or to a waning of magmatic activity at depth. Sequential fragmentation/transport theory (SFT) was used to decompose grain-size distributions into five different sub-populations. A new way of using the resultant fragmentation coefficient to assign sub-populations to different fragmentation mechanisms, even in cases when modes overlapped, is presented. For the first time the corresponding results are consistent with the phreatomagmatic eruptions, as well as with those derived from ab initio fractal model.]]></p></abstract>
<kwd-group>
<kwd lng="en"><![CDATA[Volcanic ash]]></kwd>
<kwd lng="en"><![CDATA[vulcanian eruptions]]></kwd>
<kwd lng="en"><![CDATA[pheatomagmatism]]></kwd>
<kwd lng="en"><![CDATA[eruptive column collapse]]></kwd>
<kwd lng="en"><![CDATA[pyroclastic surges]]></kwd>
<kwd lng="en"><![CDATA[hydrothermal alteration]]></kwd>
<kwd lng="en"><![CDATA[granulometry]]></kwd>
<kwd lng="en"><![CDATA[SFT]]></kwd>
<kwd lng="en"><![CDATA[Turrialba volcano]]></kwd>
<kwd lng="en"><![CDATA[Costa Rica]]></kwd>
<kwd lng="es"><![CDATA[Ceniza volcánica]]></kwd>
<kwd lng="es"><![CDATA[erupciones vulcaniana]]></kwd>
<kwd lng="es"><![CDATA[freatomagmatismo]]></kwd>
<kwd lng="es"><![CDATA[colapso de columna eruptiva]]></kwd>
<kwd lng="es"><![CDATA[oleadas piroclásticas]]></kwd>
<kwd lng="es"><![CDATA[alteración hidrotermal]]></kwd>
<kwd lng="es"><![CDATA[granulometría]]></kwd>
<kwd lng="es"><![CDATA[SFT]]></kwd>
<kwd lng="es"><![CDATA[volcán Turrialba]]></kwd>
<kwd lng="es"><![CDATA[Costa Rica]]></kwd>
</kwd-group>
</article-meta>
</front><back>
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