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<oai_dc:dc xmlns:dc="http://purl.org/dc/elements/1.1/" xmlns:oai_dc="http://www.openarchives.org/OAI/2.0/oai_dc/" xmlns:xsi="http://www.w3.org/2001/XMLSchema-instance" xsi:schemaLocation="http://www.openarchives.org/OAI/2.0/oai_dc/ http://www.openarchives.org/OAI/2.0/oai_dc.xsd">
  <dc:contributor>Michael J. Kunk</dc:contributor>
  <dc:contributor>John Aleinikoff</dc:contributor>
  <dc:contributor>John F. Sutter</dc:contributor>
  <dc:creator>Craig Dietsch</dc:creator>
  <dc:date>2010</dc:date>
  <dc:description>&lt;p class="p1"&gt;&lt;span class="s1"&gt;The Waterbury dome, located in the Rowe-Hawley zone in western Connecticut, is a triple window exposing three terranes: parautochthonous or allochthonous peri-Laurentian rocks in its lowest level 1, allochthonous rocks of the Rowe-Hawley zone in its middle level 2, and allochthonous cover rocks, including Silurian-Devonian rocks of the Connecticut Valley Gasp&amp;eacute; trough, in its highest level 3. Levels 1 and 2 are separated by the Waterbury thrust, a fault equivalent to Cameron's Line, the Taconic suture in southwestern New England. Relict mesoscopic folds and foliation in levels 1 and 2 are truncated by a dominant D&lt;/span&gt;&lt;span class="s2"&gt;&lt;sub&gt;2&lt;/sub&gt;&lt;/span&gt;&lt;span class="s1"&gt; migmatitic layering and are likely Taconic. U-Pb zircon crystallization ages of felsic orthogneiss and tonalite, syntectonic with respect to the formation of S&lt;/span&gt;&lt;span class="s2"&gt;&lt;sub&gt;2&lt;/sub&gt;&lt;/span&gt;&lt;span class="s1"&gt;, and a biotite quartz diorite that crosscuts level 2 paragneiss are 437 &amp;plusmn; 4 Ma, 434 &amp;plusmn; 4 Ma, and 437 &amp;plusmn; 4 Ma, respectively.&lt;/span&gt;&lt;/p&gt;
&lt;p class="p1"&gt;&lt;span class="s1"&gt;Level 3 nappes were emplaced over the Waterbury dome along an Acadian d&amp;eacute;collement synchronous with the formation of a D&lt;/span&gt;&lt;span class="s2"&gt;&lt;sub&gt;3&lt;/sub&gt;&lt;/span&gt;&lt;span class="s1"&gt; thrust duplex in the dome. The d&amp;eacute;collement truncates the Ky + Kfs-in (migmatite) isograd in the dome core and a St-in isograd in level 3 nappes, indicating that peak metamorphic conditions in the dome core and nappe cover rocks formed in different places at different times. Metamorphic overgrowths on zircon from the felsic orthogneiss in the Waterbury dome have an age of 387 &amp;plusmn; 5 Ma. Rocks of all levels and the d&amp;eacute;collement are folded by D&lt;/span&gt;&lt;span class="s2"&gt;&lt;sub&gt;4&lt;/sub&gt;&lt;/span&gt;&lt;span class="s1"&gt; folds that have a strongly developed, regional crenulation cleavage and D&lt;/span&gt;&lt;span class="s2"&gt;&lt;sub&gt;5&lt;/sub&gt;&lt;/span&gt;&lt;span class="s1"&gt; folds. The Waterbury dome was formed by thrust duplexing followed by fold interference during the Acadian orogeny. The &lt;/span&gt;&lt;span class="s2"&gt;&lt;sup&gt;40&lt;/sup&gt;&lt;/span&gt;&lt;span class="s1"&gt;Ar/&lt;/span&gt;&lt;span class="s2"&gt;&lt;sup&gt;39&lt;/sup&gt;&lt;/span&gt;&lt;span class="s1"&gt;Ar ages of amphibole, muscovite, biotite, and K-feldspar from above and below the d&amp;eacute;collement are ca. 378 Ma, 355 Ma, 360 Ma (above) and 340 (below), and 288 Ma, respectively. Any kilometer-scale vertical movements between dome and nappe rocks were over by ca. 378 Ma. Core and cover rocks of the Waterbury dome record synchronous, post-Acadian cooling.&lt;/span&gt;&lt;/p&gt;</dc:description>
  <dc:format>application/pdf</dc:format>
  <dc:identifier>10.1130/2010.1206(08)</dc:identifier>
  <dc:language>en</dc:language>
  <dc:publisher>The Geological Society of America</dc:publisher>
  <dc:title>The tectono-thermal evolution of the Waterbury dome, western Connecticut, based on U-Pb and &lt;sup&gt;40&lt;/sup&gt;Ar/&lt;sup&gt;39&lt;/sup&gt;Ar ages</dc:title>
  <dc:type>article</dc:type>
</oai_dc:dc>