<?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>1405-3322</journal-id>
<journal-title><![CDATA[Boletín de la Sociedad Geológica Mexicana]]></journal-title>
<abbrev-journal-title><![CDATA[Bol. Soc. Geol. Mex]]></abbrev-journal-title>
<issn>1405-3322</issn>
<publisher>
<publisher-name><![CDATA[Sociedad Geológica Mexicana A.C.]]></publisher-name>
</publisher>
</journal-meta>
<article-meta>
<article-id>S1405-33222019000100021</article-id>
<article-id pub-id-type="doi">10.18268/bsgm2019v71n1a3</article-id>
<title-group>
<article-title xml:lang="en"><![CDATA[Microscopic and tomographic studies for interpreting the genesis of desert varnish and the vesicular horizon of desert soils in Mongolia and the USA]]></article-title>
<article-title xml:lang="es"><![CDATA[Estudios microscópicos y tomográficos para interpretar la génesis de barniz del desierto y el horizonte vesicular de suelos desérticos en Mongolia y los EUA]]></article-title>
</title-group>
<contrib-group>
<contrib contrib-type="author">
<name>
<surname><![CDATA[Lebedeva]]></surname>
<given-names><![CDATA[Marina P.]]></given-names>
</name>
<xref ref-type="aff" rid="Aff"/>
<xref ref-type="aff" rid="Aaf"/>
</contrib>
<contrib contrib-type="author">
<name>
<surname><![CDATA[Golovanov]]></surname>
<given-names><![CDATA[Dmitry L.]]></given-names>
</name>
<xref ref-type="aff" rid="Aff"/>
<xref ref-type="aff" rid="Aaf"/>
</contrib>
<contrib contrib-type="author">
<name>
<surname><![CDATA[Shishkov]]></surname>
<given-names><![CDATA[Vasily A.]]></given-names>
</name>
<xref ref-type="aff" rid="Aff"/>
</contrib>
<contrib contrib-type="author">
<name>
<surname><![CDATA[Ivanov]]></surname>
<given-names><![CDATA[Andrey L.]]></given-names>
</name>
<xref ref-type="aff" rid="Aff"/>
</contrib>
<contrib contrib-type="author">
<name>
<surname><![CDATA[Abrosimov]]></surname>
<given-names><![CDATA[Konstantin N.]]></given-names>
</name>
<xref ref-type="aff" rid="Aff"/>
</contrib>
</contrib-group>
<aff id="Af1">
<institution><![CDATA[,Russian Academy of Sciences Dokuchaev Soil Science Institute ]]></institution>
<addr-line><![CDATA[Moscow ]]></addr-line>
<country>Russia</country>
</aff>
<aff id="Af2">
<institution><![CDATA[,Lomonosov Moscow State University  ]]></institution>
<addr-line><![CDATA[Moscow ]]></addr-line>
<country>Russia</country>
</aff>
<aff id="Af3">
<institution><![CDATA[,Russian Academy of Sciences Institute of Geography ]]></institution>
<addr-line><![CDATA[Moscow ]]></addr-line>
<country>Russia</country>
</aff>
<pub-date pub-type="pub">
<day>00</day>
<month>00</month>
<year>2019</year>
</pub-date>
<pub-date pub-type="epub">
<day>00</day>
<month>00</month>
<year>2019</year>
</pub-date>
<volume>71</volume>
<numero>1</numero>
<fpage>21</fpage>
<lpage>42</lpage>
<copyright-statement/>
<copyright-year/>
<self-uri xlink:href="http://www.scielo.org.mx/scielo.php?script=sci_arttext&amp;pid=S1405-33222019000100021&amp;lng=en&amp;nrm=iso"></self-uri><self-uri xlink:href="http://www.scielo.org.mx/scielo.php?script=sci_abstract&amp;pid=S1405-33222019000100021&amp;lng=en&amp;nrm=iso"></self-uri><self-uri xlink:href="http://www.scielo.org.mx/scielo.php?script=sci_pdf&amp;pid=S1405-33222019000100021&amp;lng=en&amp;nrm=iso"></self-uri><abstract abstract-type="short" xml:lang="en"><p><![CDATA[Abstract The composition and microfabric of the Av diagnostic surface horizon (crust) and desert varnish of soils formed on various parent materials covering ancient alluvial fans in extremely arid deserts of Central Asia (Trans-Altai Gobi, Mongolia) and North America (Mojave, USA) are analyzed. Application of a wide range of methods-morphological and micromorphological descriptions, scanning electron microscopy, electron microprobe analysis and microtomography, together with traditional physicochemical methods-has shown that desert varnish retains the same composition and relative contents of elements (Fe/Ti and Mn/Ba) independently from the initial composition of parent materials and geographical location of the studied regions. The absolute dominance of isolated closed (vesicular) pores, identified by micromorphology and confirmed by microtomography, can account for specific hydrophysical properties of the crust horizon; that is, low water-holding capacity and permeability. We explain both phenomena of desert pedogenesis-light-coloured crust horizon and dark-coloured desert varnish-the burst of microbiological activity and physicochemical processes after rare but heavy showers during the hot season. The development of iron-depleted zones around pores is considered the evidence of that phenomenon. Consequently, we propose that Mn2+undergoes mobilization within the crust horizon, followed by its upward migration with capillary and film moisture flows, against the gravity gradient to the surface of desert pavement with its subsequent fixation at the oxygen barrier. The processes of sulphate reduction are indirectly confirmed by the mobilization of Ba2+, which is immobile in the presence of sulphates. These elements (Mn and Ba) accumulate within the lower part of two-layer films. These films are located in microcavities on the upper sides of rock fragments of desert pavements in the studied regions. Films on lower sides of rock fragments and the upper part of those two-layered films are enriched in Fe and Ti, and therefore acquire reddish-brownish colours. Despite its transitory character, the process, which we suggest to call &#8216;cryptosolodization&#8217;, includes five stages: (1) Fe, Mn and sulphate reduction with mobilization of Ba2+from BaSO4, (2) precipitation of FeS and migration of Ba2+and Mn2+to the stone surface, (3) coprecipitation of Ba and Mn at a combined oxygen-sorption barrier, (4) oxidation of S2-to SO4 2-with mobilization of Ti2+from TiO2and (5) oxidation of Ti2+and Fe2+and their coprecipitation in the form of oxides/ hydroxides TiO2and Fe(OH)3.]]></p></abstract>
<abstract abstract-type="short" xml:lang="es"><p><![CDATA[Resumen El artículo analiza la composición y microestructura del Horizonte vesicular Av (Aye), que consiste en la corteza superficial diagnóstica y el barniz del desierto (laca) de suelos, formados sobre diferentes rocas madres y llanuras fanaluvial y antigua en condiciones extremadamente áridas de Asia Central (Transltai Gobi, Mongolia) y América del Norte (Mojave, Estados Unidos). Se aplicó una amplia gama de métodos. Entre ellos, descripciones morfológicas y micromorfológicas, microscopía electrónica de exploración, análisis electrónico de microsondas y microtomografía, y también los métodos físicos y químicos tradicionales. Los datos mostraron que laca del desierto (barniz del desierto) tiene la misma composición y la relación relativa de los elementos (Fe/Ti y Mn/Ba) independientemente de la composición inicial de las rocas madres y de la ubicación geográfica de las regiones estudiadas. Las propiedades hidrofísicas específicas del horizonte cortical superficial, sobre todo su baja permeabilidad al agua, pueden explicarse debido al dominio absoluto de los poros cerrados (vesiculares) aislados identificados por la micromorfología y confirmados por la microtomografía. Explicamos el proceso de formación de suelos -formación conjunta de la corteza ligera, superficial y vesicular y también la laca oscura del desierto (barniz del desierto)- como un mecanismo hidrofísico-biogeoquímico causante de un aumento de la actividad microbiológica y procesos físico-químicos después de las lluvias raras y fuertes en temporada calurosa. La evidencia de este fenómeno radica en la evolución de las zonas empobrecidas de hierro alrededor de los poros. Al mismo tiempo, Mn2+está sujeto a la movilización en el horizonte de la corteza y luego se mueve hacia arriba a la superficie con flujos de humedad capilar y de película contra el gradiente gravitacional seguido de la fijación en la barrera de oxígeno. La recuperación de sulfatos (sulfatreducción) se confirma indirectamente mediante la movilización de Ba2+, que se encuentra inmóvil en la presencia de sulfatos. Estos elementos (Mn y Ba) se acumulan en la parte inferior de las películas de doble capa, las cuales están en los microcavidades sobre los lados superiores de los fragmentos de roca del puente desértico en las áreas investigadas. Las películas sobre los lados inferiores y la parte superior de los fragmentos de roca están enriquecidas con Fe y Ti y, por lo tanto, adquieren colores rojizos. Sugerimos llamar a este proceso &#8216;criptosolodización&#8217;, a pesar de su carácter a corto plazo(explosivo). Incluye 5 etapas: (1) recuperación de Fe, Mn y sulfatos con la movilización de Ba2+de BaSO4, (2) deposición de FeS y migración de Ba2+y Mn2+a la superficie de la roca, (3) coprecipitación de Ba y Mn en la barrera combinada de oxígeno-sorción, (4) oxidación S2-a SO4 2-con la movilización de Ti2+de TiO2y (5) la oxidación Ti2+y Fe2+y su coprecipitación en forma de óxidos/hidróxidos TiO2y Fe(OH)3.]]></p></abstract>
<kwd-group>
<kwd lng="en"><![CDATA[desert soils]]></kwd>
<kwd lng="en"><![CDATA[micromorphology]]></kwd>
<kwd lng="en"><![CDATA[pedogenesis]]></kwd>
<kwd lng="en"><![CDATA[mechanisms of development of desert varnish]]></kwd>
<kwd lng="es"><![CDATA[suelos desérticos]]></kwd>
<kwd lng="es"><![CDATA[micromorfología]]></kwd>
<kwd lng="es"><![CDATA[formación del suelo]]></kwd>
<kwd lng="es"><![CDATA[mecanismos del desarrollo de barniz desértico y el horizonte vesicular (cortical)]]></kwd>
</kwd-group>
</article-meta>
</front><back>
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