<?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>S1405-33222023000300108</article-id>
<article-id pub-id-type="doi">10.18268/bsgm2023v75n3a061023</article-id>
<title-group>
<article-title xml:lang="en"><![CDATA[Depositional environment and sequence stratigraphy of the Qom Formation (Miocene) from the Ghalibaf section, Central Iran]]></article-title>
<article-title xml:lang="es"><![CDATA[Ambiente deposicional y estratigrafía secuencial de la Formación Qom (Mioceno) de la sección Ghalifab, Irán Central]]></article-title>
</title-group>
<contrib-group>
<contrib contrib-type="author">
<name>
<surname><![CDATA[Sharifi]]></surname>
<given-names><![CDATA[Jafar]]></given-names>
</name>
<xref ref-type="aff" rid="Aff"/>
</contrib>
<contrib contrib-type="author">
<name>
<surname><![CDATA[Nasiri]]></surname>
<given-names><![CDATA[Yaghub]]></given-names>
</name>
<xref ref-type="aff" rid="Aff"/>
</contrib>
<contrib contrib-type="author">
<name>
<surname><![CDATA[Badpa]]></surname>
<given-names><![CDATA[Mahdi]]></given-names>
</name>
<xref ref-type="aff" rid="Aff"/>
</contrib>
<contrib contrib-type="author">
<name>
<surname><![CDATA[Taghdisi Nikbakht]]></surname>
<given-names><![CDATA[Samira]]></given-names>
</name>
<xref ref-type="aff" rid="Aff"/>
</contrib>
<contrib contrib-type="author">
<name>
<surname><![CDATA[Sarkar]]></surname>
<given-names><![CDATA[Suman]]></given-names>
</name>
<xref ref-type="aff" rid="Aff"/>
</contrib>
<contrib contrib-type="author">
<name>
<surname><![CDATA[Hadi]]></surname>
<given-names><![CDATA[Mehdi]]></given-names>
</name>
<xref ref-type="aff" rid="Aff"/>
</contrib>
</contrib-group>
<aff id="Af1">
<institution><![CDATA[,Payame Noor University Department of Geology ]]></institution>
<addr-line><![CDATA[Tehran ]]></addr-line>
<country>Iran</country>
</aff>
<aff id="Af2">
<institution><![CDATA[,University of Gonabad Faculty of Science Geology Department]]></institution>
<addr-line><![CDATA[Gonabad ]]></addr-line>
<country>Iran</country>
</aff>
<aff id="Af3">
<institution><![CDATA[,Tehran  ]]></institution>
<addr-line><![CDATA[Tehran ]]></addr-line>
<country>Iran</country>
</aff>
<aff id="Af4">
<institution><![CDATA[,Birbal Sahni Institute of Palaeosciences  ]]></institution>
<addr-line><![CDATA[Lucknow ]]></addr-line>
<country>India</country>
</aff>
<aff id="Af5">
<institution><![CDATA[,Mashhad  ]]></institution>
<addr-line><![CDATA[Mashhad ]]></addr-line>
<country>Iran</country>
</aff>
<pub-date pub-type="pub">
<day>00</day>
<month>00</month>
<year>2023</year>
</pub-date>
<pub-date pub-type="epub">
<day>00</day>
<month>00</month>
<year>2023</year>
</pub-date>
<volume>75</volume>
<numero>3</numero>
<copyright-statement/>
<copyright-year/>
<self-uri xlink:href="http://www.scielo.org.mx/scielo.php?script=sci_arttext&amp;pid=S1405-33222023000300108&amp;lng=en&amp;nrm=iso"></self-uri><self-uri xlink:href="http://www.scielo.org.mx/scielo.php?script=sci_abstract&amp;pid=S1405-33222023000300108&amp;lng=en&amp;nrm=iso"></self-uri><self-uri xlink:href="http://www.scielo.org.mx/scielo.php?script=sci_pdf&amp;pid=S1405-33222023000300108&amp;lng=en&amp;nrm=iso"></self-uri><abstract abstract-type="short" xml:lang="en"><p><![CDATA[ABSTRACT The Miocene strata of the Qom Formation from the Ghalibaf section, Central Iran (NW Semnan) documented a high diversity of shallow-marine microfacies. These deposits in the Ghalibaf section, with a total thickness of 445 m, are characterized by twenty-one microfacies. The carbonate microfacies are deposited into five facies belts, including a lagoon, upper slope, lower slope, platform-margin sand shoals and margin facies. The presence of barrier reefs, intraclasts, oncoids, and grainstone aggregates, along with the absence of vast tidal flat areas, are distinguished. According to the aforementioned evidences, these sediments were deposited on a rimmed carbonate platform. In addition, the heterolithic calciturbidite deposits also show that the carbonate sequences were sedimented on a rimmed carbonate platform. Based on the available data of sequence stratigraphy analysis, seven third-order depositional sequences are bounded by type-1 and type-2 sequence boundaries. The relative sea-level changes between the upper and lower sequence boundaries in accord with the global sea-level curves reveal a reasonable correlation. However, some differences in other sequence boundaries might be due to local tectonic activities in the Qom Formation sedimentary basin, thereby leading to local sea-level changes. Moreover, biostratigraphic data based on the larger foraminifera index markers, including Praebullalveolina curdica, Borelis melo, Dendritina rangi, Meandropsina iranica, Elphidium sp. 14, Neorotalia viennoti, and Miogypsina sp. suggests the Miocene Shallow Benthic Zones, SBZ24-SBZ25 equivalent to the late Aquitanian-Burdigalian timespan.]]></p></abstract>
<abstract abstract-type="short" xml:lang="es"><p><![CDATA[RESUMEN Los estratos del Mioceno de la Formación Qom Formation en la sección Ghalibaf, Irán Central (NO Semnan), documentan una alta diversidad de microfacies marinas someras. Estos depósitos, en la sección Ghalibaf, con un espesor total de 445 m, se caracterizan por veitiún microfacies. Las microfacies de carbonatosfueron depositadas en cinco cinturones de facies, incluyendo laguna, pendiente superior, pendiente inferior, bancos de arena de margen de plataforma y facies marginales en una plataforma carbonatada bordeada. La presencia de barreras de arrecifes, intraclastos, oncoides, The presence of barrier reefs, intraclasts, oncoids, y calizas granulares de carga agregada, junto con la ausencia de vastas areas de planicie de mareas, logran distinguirse. De acuerdo a las evidencias antes mencionadas, estos sedimentos fueron depositados en una plataforma carbonatada marginada. Adicionalmente, el carácter heterolítico de depósitos de calcirrudita muestran que las secuencias fueron despositadas en el tipo de plataforma citado. Con base en los datos disponibles de análisis de estratigrafía secuencial, setentaytres órdenes de secuencias deposicionales se caracterizan por límites de secuencia topoe-1 y tipo. Los cambios de nivel del mar relativos entre los límites de secuencia superior e inferior, de acuerdo a las curvas del nivel global del mar, revelan una correlación razonable. Sin embargo, algunas diferencias en otros límites de secuencia pueden deberse a actividad tectónica local en la cuenca sedimentaria de la Formación Qom, lo que produciría cambios locales del nivel del mar. Adicionalmente, datos bioestratigráficos basados en grandes foraminíferos, marcadores índice, que incluyen Praebullalveolina curdica, Borelis melo, Dendritina rangi, Meandropsina iranica, Elphidium sp. 14, Neorotalia viennoti y Miogypsina sp., sugieren las Zonas Bénticas Someras del Mioceno SBZ24-SBZ25, las cuales son equivalentes al lapso temporal del Aquitanian tardío-Burdigalian.]]></p></abstract>
<kwd-group>
<kwd lng="en"><![CDATA[Qom Formation]]></kwd>
<kwd lng="en"><![CDATA[Miocene]]></kwd>
<kwd lng="en"><![CDATA[Sequence Stratigraphy]]></kwd>
<kwd lng="en"><![CDATA[Central Iran]]></kwd>
<kwd lng="en"><![CDATA[Microfacies]]></kwd>
<kwd lng="es"><![CDATA[Formación Qom]]></kwd>
<kwd lng="es"><![CDATA[Mioceno]]></kwd>
<kwd lng="es"><![CDATA[Estratigrafía secuencial]]></kwd>
<kwd lng="es"><![CDATA[Irán Central]]></kwd>
<kwd lng="es"><![CDATA[Microfacies]]></kwd>
</kwd-group>
</article-meta>
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