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<article language="en">
	<journal>
		<journal_title>Atmospheric Chemistry and Physics Discussions</journal_title>
		<journal_url>www.atmos-chem-phys-discuss.net</journal_url>
		<issn>1680-7367</issn>
		<eissn>1680-7375</eissn>
		<volume_number>9</volume_number>
		<issue_number>3</issue_number>
		<publication_year>2009</publication_year>
	</journal>
	<doi>10.5194/acpd-9-12559-2009</doi>
	<article_url>http://www.atmos-chem-phys-discuss.net/9/12559/2009/</article_url>
	<abstract_html>http://www.atmos-chem-phys-discuss.net/9/12559/2009/acpd-9-12559-2009.html</abstract_html>
	<fulltext_pdf>http://www.atmos-chem-phys-discuss.net/9/12559/2009/acpd-9-12559-2009.pdf</fulltext_pdf>
	<start_page>12559</start_page>
	<end_page>12596</end_page>
	<publication_date>2009-05-27</publication_date>
	<article_title content_type="html">Photolytic control of the nitrate stable isotope signal in snow and atmosphere of East Antarctica and implications for reactive nitrogen cycling</article_title>
	<authors>
		<author numeration="1" affiliations="1,2,4">
			<name>M. M. Frey</name>
			<email>maey@bas.ac.uk</email>
		</author>
		<author numeration="2" affiliations="1,2">
			<name>J. Savarino</name>
		</author>
		<author numeration="3" affiliations="1,2">
			<name>S. Morin</name>
		</author>
		<author numeration="4" affiliations="1,2">
			<name>J. Erbland</name>
		</author>
		<author numeration="5" affiliations="1,3">
			<name>J. M. F. Martins</name>
		</author>
	</authors>
	<affiliations>
		<affiliation numeration="1" content_type="html">CNRS – Institut National des Sciences de l&apos;Univers (INSU), France</affiliation>
		<affiliation numeration="2" content_type="html">Laboratoire de Glaciologie et Géophysique de l&apos;Environnement, Université Joseph Fourier-Grenoble, St Martin d&apos;Hères, France</affiliation>
		<affiliation numeration="3" content_type="html">Laboratoire d&apos;Etude de Transferts en Hydrologie et Environnement, Université Joseph Fourier-Grenoble, St Martin d&apos;Hères, France</affiliation>
		<affiliation numeration="4" content_type="html">now at: British Antarctic Survey, Natural Environment Research Council, Cambridge, United Kingdom</affiliation>
	</affiliations>
	<abstract content_type="html">The nitrogen (&amp;delta;&lt;sup&gt;15&lt;/sup&gt;N) and triple oxygen (&amp;delta;&lt;sup&gt;17/18&lt;/sup&gt;O)
isotopic composition of nitrate (NO&lt;sub&gt;3&lt;/sub&gt;&lt;sup&gt;&amp;minus;&lt;/sup&gt;) was measured year-round in
the atmosphere and snow pits at Dome C (DC, 75.1&amp;deg; S,
123.3&amp;deg; E), and in surface snow on a transect between DC
and the coast. Snow pit profiles of &amp;delta;&lt;sup&gt;15&lt;/sup&gt;N (&amp;delta;&lt;sup&gt;18&lt;/sup&gt;O)
in NO&lt;sub&gt;3&lt;/sub&gt;&lt;sup&gt;&amp;minus;&lt;/sup&gt; show significant enrichment (depletion) of &amp;gt;200 (&amp;lt;40)
&amp;permil; compared to the isotopic signal in atmospheric NO&lt;sub&gt;3&lt;/sub&gt;&lt;sup&gt;&amp;minus;&lt;/sup&gt;,
whereas post-depositional fractionation in &amp;Delta;&lt;sup&gt;17&lt;/sup&gt;O(NO&lt;sub&gt;3&lt;/sub&gt;&lt;sup&gt;&amp;minus;&lt;/sup&gt;)
is small, allowing reconstruction of past shifts in tropospheric oxidation
pathways from ice cores. Assuming a Rayleigh-type process we find in the
DC04 (DC07) pit fractionation factors ε of &amp;minus;50&amp;plusmn;10 (&amp;minus;71&amp;plusmn;12)
&amp;permil;, 6&amp;plusmn;3 (9&amp;plusmn;2) &amp;permil; and 1&amp;plusmn;0.2 (2&amp;plusmn;0.6) &amp;permil;, for
&amp;delta;&lt;sup&gt;15&lt;/sup&gt;N, &amp;delta;&lt;sup&gt;18&lt;/sup&gt;O and &amp;Delta;&lt;sup&gt;17&lt;/sup&gt;O,
respectively. A photolysis model reproduces ε for
&amp;delta;&lt;sup&gt;15&lt;/sup&gt;N within the range of uncertainty at DC and for
lab experiments reported by Blunier et al. (2005), suggesting that the current
literature value for photolytic isotopic fractionation in snow is significantly
underestimated. Depletion of oxygen stable isotopes is attributed to photolysis
followed by isotopic exchange with water and hydroxyl radicals.
Conversely, &lt;sup&gt;15&lt;/sup&gt;N enrichment of the NO&lt;sub&gt;3&lt;/sub&gt;&lt;sup&gt;&amp;minus;&lt;/sup&gt; fraction in the snow
implies &lt;sup&gt;15&lt;/sup&gt;N depletion of
emissions. Indeed, &amp;delta;&lt;sup&gt;15&lt;/sup&gt;N in atmospheric NO&lt;sub&gt;3&lt;/sub&gt;&lt;sup&gt;&amp;minus;&lt;/sup&gt;
shows a strong decrease from background levels (4.4&amp;plusmn;6.8&amp;permil;) to &amp;minus;35.1&amp;permil;
in spring followed by recovery during summer, consistent with
significant snow pack emissions of reactive nitrogen. Field and
lab evidence therefore suggest that photolysis dominates fractionation
and associated NO&lt;sub&gt;3&lt;/sub&gt;&lt;sup&gt;&amp;minus;&lt;/sup&gt; loss from snow in the low-accumulation
regions of the East Antarctic Ice Sheet (EAIS). The &amp;Delta;&lt;sup&gt;17&lt;/sup&gt;O
signature confirms previous coastal measurements that the peak of
atmospheric NO&lt;sub&gt;3&lt;/sub&gt;&lt;sup&gt;&amp;minus;&lt;/sup&gt; in spring is of stratospheric origin. After sunrise
photolysis drives then redistribution of NO&lt;sub&gt;3&lt;/sub&gt;&lt;sup&gt;&amp;minus;&lt;/sup&gt; from the snowpack
photic zone to the atmosphere and a snow surface skin layer, thereby
concentrating NO&lt;sub&gt;3&lt;/sub&gt;&lt;sup&gt;&amp;minus;&lt;/sup&gt; at the surface. Little NO&lt;sub&gt;3&lt;/sub&gt;&lt;sup&gt;&amp;minus;&lt;/sup&gt; is
exported off the EAIS plateau, still snow emissions from as far as 600 km
inland can contribute to the coastal NO&lt;sub&gt;3&lt;/sub&gt;&lt;sup&gt;&amp;minus;&lt;/sup&gt; budget.</abstract>
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</article>

