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                  <text>&lt;p&gt;&lt;strong&gt;Start here:&lt;br /&gt;&lt;/strong&gt;Ernst, W.G., 2015, Franciscan geologic history constrained by tectonic/olistostromal high-grade metamafic blocks in the iconic California Mesozoic-Cenozoic accretionary complex: American Mineralogist, v. 100, p. 6-13.Â &lt;a href="http://dx.doi.org/10.2138/am-2015-4850" target="_blank"&gt;&lt;span&gt;doi:Â &lt;/span&gt;&lt;span class="slug-doi"&gt;10.2138/am-2015-4850&lt;/span&gt;&lt;/a&gt;&lt;/p&gt;
&lt;ul&gt;&lt;li&gt;This source supplies useful information on the low temperature, high pressure environment in which these rocks formed.Â &lt;/li&gt;
&lt;/ul&gt;&lt;strong&gt;Additional resources:&lt;br /&gt;&lt;/strong&gt;Barnes, J., Eldam, R., Lee, C.T., Errico, J., Loewy, S., and Cisneros, M., 2013, Petrogenesis of serpentinites from the Franciscan Complex, western California, USA: Lithos, v. 178, p. 143-157.Â &lt;a class="S_C_ddDoi" href="http://dx.doi.org/10.1016/j.lithos.2012.12.018" target="_blank"&gt;doi:10.1016/j.lithos.2012.12.018&lt;/a&gt;&lt;br /&gt;&lt;ul&gt;&lt;li&gt;Describes the petrogenesis of serpentine as seen in one of the items in the collection (Fr-4).&lt;/li&gt;
&lt;/ul&gt;&lt;p&gt;Cooper, F., Platt, J., and Anczkiewicz, R., 2011, Constraints on early Franciscan subduction rates from 2-D thermal modeling: Earth and Planetary Science Letters, v. 312, p. 69-79. doi:&lt;a href="http://dx.doi.org/10.1016/j.epsl.2011.09.051"&gt;10.1016/j.epsl.2011.09.051&lt;/a&gt;&lt;/p&gt;
&lt;ul&gt;&lt;li&gt;This paper suggests that the rate of subduction in this area may have been five times lower than previous studies have found.&lt;/li&gt;
&lt;/ul&gt;&lt;p&gt;Ghatak, A., Basu, A., and Wakabayashi, J., 2013, Implications of Franciscan Complex graywacke geochemistry for sediment transport, provenance determination, burial-exposure duration, and fluid exchange with cosubducted metabasites: Tectonics, v. 32, p. 1480-1492. doi:Â &lt;a href="http://dx.doi.org/10.1002/tect.20078"&gt;10.1002/tect.20078&lt;/a&gt;&lt;/p&gt;
&lt;ul&gt;&lt;li&gt;This article states that the europium anomalies of the greywacke samples suggest provenance from the Sierra Nevada batholith.&lt;/li&gt;
&lt;/ul&gt;&lt;p&gt;Langenheim, V., Jachens, R., Wentworth, C., and McLaughlin, R., 2013, Previously unrecognized regional structure of the Coastal Belt of the Franciscan Complex, northern California, revealed by magnetic data: Geosphere, v. 9, p. 1514-1529. doi:Â &lt;a href="http://dx.doi.org/10.1130/GES00942.1"&gt;10.1130/GES00942.1&lt;/a&gt;&lt;/p&gt;
&lt;ul&gt;&lt;li&gt;&lt;span&gt;Using magnetic data, this article provides an overview of the regional structure of the Franciscan Complex.&lt;/span&gt;&lt;/li&gt;
&lt;/ul&gt;</text>
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                <text>Angular, silty size gains, composed of equal parts quatz, feldspars and rock fragments. Prominent orange and brown surface oxydation on all samples. Some samples contain evidence of bedding planes.  Calicte is found along bedding planes, as well as on some surfaces perpendicular to bedding. Some samples include very fine calcite veins (&lt;0.5mm) intersecting through the bedding planes. (FOV: 1.28)</text>
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                <text>Roadcut on south side of Petaluma Pt.&#13;
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                <text>Purchased from Western Minerals, Inc.</text>
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                  <text>Western Minerals, Inc.</text>
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                  <text>Purchased from Western Minerals, Inc.</text>
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              <description>An account of the resource</description>
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                  <text>A classic example of Barrovian-type metamorphism in Dutchess County, NY associated with the Taconic orogeny. A Barrovian metamorphic sequence displays gradual pressure and temperature increase along the metamorphic gradient, and occurs during regional metamorphism. These zones of pressure and temperature increase are recognizable by the characteristic minerals that accompany them. Dutchess County, NY contains an unusually complete sequence.&#13;
&#13;
This collection contains metamorphic rocks from chlorite grade to sillimanite grade in a tight spatial window which records the regional metamorphic gradient increasing  from WNW to ESE. This collection also contains some rocks that mirror the protoliths of the schists and quartzites of the sequence (shales and graywacke). </text>
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                  <text>1970</text>
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                  <text>450-430 Ma</text>
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                  <text>&lt;strong&gt;Start Here:&lt;/strong&gt; &lt;br /&gt;Vollmer, F. W., and Walker, J., 2009, The classic Barrovian metamorphic sequence of Dutchess County and its structural and stratigraphic context in the Taconic Orogeny. In Guidebookâ€”New York State Geological Association Meeting, v. 81, p. 11-1.Â &lt;br /&gt;&lt;a href="http://www2.newpaltz.edu/~vollmerf/papers/Vollmer_and_Walker_2009_NYSGA.pdf"&gt;http://www2.newpaltz.edu/~vollmerf/papers/Vollmer_and_Walker_2009_NYSGA.pdf&lt;/a&gt;Â (accessed March 15th, 2015)&lt;br /&gt;&lt;br /&gt;&lt;ul&gt;&lt;li&gt;A useful field trip guide across the Barrovian metamorphic sequence of Dutchess county. Good general introduction to the geology of the area.&lt;/li&gt;
&lt;/ul&gt;&lt;strong&gt;Additional Resources:&lt;/strong&gt;&lt;br /&gt;Whitney, D.L., Mechum, T.A., Keuhner, S.M., and Dilek, Y.R., 1996, Progressive metamorphism of pelitic rocks from protolith to granulite facies, Dutchess County, New York, USA: constraints on the timing of fluid infiltration during regional metamorphism, Journal of Metamorphic Geology, v. 14, p. 163-181. &lt;a href="http://dx.doi.org/"&gt;http://dx.doi.org/&lt;span&gt;10.1046/j.1525-1314.1996.05836.x&lt;/span&gt;&lt;/a&gt;&lt;br /&gt;&lt;br /&gt;&lt;ul&gt;&lt;li&gt;A fairly general look at the progressive metamorphism in Dutchess County by one of the foremost workers in the area.&lt;/li&gt;
&lt;/ul&gt;&lt;br /&gt;Knopf, E.B., 1927, Some recent work in the Taconic area: American Journal of Science, v. 41, p. 42-458. &lt;a href="http://dx.doi.org/"&gt;http://dx.doi.org/&lt;span&gt;10.2475/ajs.s5-14.84.429&lt;/span&gt;&lt;/a&gt;&lt;br /&gt;&lt;br /&gt;&lt;ul&gt;&lt;li&gt;One of the first articles to describle the Dutchess County rocks as a "classic" Barrovian sequence.Â &lt;/li&gt;
&lt;/ul&gt;&lt;br /&gt;Ghent, E.D., Stout, M.Z., 1981, Geobarometry and geothermometry of plagioclase-biotite-garnet-muscovite assemblages, Contributions to Mineralogy and Petrology, v. 76, p. 92-97. &lt;a href="http://dx.doi.org/"&gt;http://dx.doi.org/&lt;span&gt;10.1007/BF00373688&lt;/span&gt;&lt;/a&gt;&lt;br /&gt;&lt;br /&gt;&lt;br /&gt;&lt;ul&gt;&lt;li&gt;Work constraining the pressure and temperature paths of metamorphism in the sequence through equilibrium assemblages. This work was found to be in agreement with other equilibrium assemblage PT paths.&lt;/li&gt;
&lt;/ul&gt;&lt;br /&gt;Whitney, D.L., Mechum, T.A., Dilek, Y.R., and Keuhner, S.M., 1996, Modification of garnet during regional metamorphism in garnet through sillimanite-zone rocks, Dutchess County, New York, American Mineralogist, v. 81, p. 696-705. &lt;a href="http://www.minsocam.org/MSA/AmMin/TOC/Articles_Free/1996/Whitney_p696-705_96.pdf"&gt; http://www.minsocam.org/MSA/AmMin/TOC/Articles_Free/1996/Whitney_p696-705_96.pdf&lt;/a&gt;&lt;br /&gt;&lt;br /&gt;&lt;ul&gt;&lt;li&gt;Work by Whitney on changes in PTX conditions leading to modification of garnet in the metamorphic sequence. Garnet is widely distributed through the sequence, which makes it a useful marker for tracking these changes.&lt;/li&gt;
&lt;/ul&gt;</text>
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                <text>&lt;a href="http://geosciencecollections.milne-library.org/collections/show/18"&gt;Barrovian Metamorphic Sequence--Dutchess County, New York&lt;/a&gt;</text>
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                <text>Green shale of the Indian River member of the Normanskill formation. This shale contains muscovite, chlorite, plagioclase, and quartz.&#13;
&#13;
The thin section shows quartz and biotite with some minor opaques.&#13;
&#13;
This rock is from the chlorite zone of the Barrovian metamorphic sequence (low metamorphism).&#13;
&#13;
This rock was collected from the east end of a large road cut where samples 1 and 3 were also collected from.</text>
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                <text>Purchased from Western Minerals Inc.</text>
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            <element elementId="50">
              <name>Title</name>
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                  <text>(TMJ) Quartz-rich Metamorphic Suite -- Tanzawa Mountains, Kanto, Japan</text>
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                  <text>The Tanzawa Mountains in Japan were created in an arc-arc collision, when the Izu-Bonin-Mariana Arc was subducted beneath the Honshu Arc. This eventually  accreted into the Tanzawa Mountains.  The samples in this collection were found in and around the Tanzawa Mountains.  The suite includes hornfels, amphibolites, quartz diorite, granophyres, and other basaltic rocks.  The samples range from fine to coarse grained.  An interesting feature found on many of the samples was a flow-like swirl of minerals in the thin section, visible in XPL.  The quartz diorite  samples had crystalline, powdery substances on them, which were analyzed using a Scanning Electron Microscope (SEM). The chemical compositions of the mentioned powdery substances were calcium, aluminum, silicon, and oxygen. </text>
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              <name>Contributor</name>
              <description>An entity responsible for making contributions to the resource</description>
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                <elementText elementTextId="17776">
                  <text>Western Minerals, Inc.</text>
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              <name>References</name>
              <description>A related resource that is referenced, cited, or otherwise pointed to by the described resource.</description>
              <elementTextContainer>
                <elementText elementTextId="17996">
                  <text>&lt;p&gt;&lt;strong&gt;Start here:&lt;br /&gt;&lt;/strong&gt;Kawate, S., and Makoto, A., 1998, Petrogenesis of the Tanzawa plutonic complex, central Japan; exposed felsic middle crust of the Izu-Bonin-Mariana Arc: Island Arc, v. 7, p. 342-358, &lt;br /&gt;link: http://dx.doi.org/10.1111/j.1440-1738.1998.00194.x.&lt;/p&gt;
&lt;ul&gt;&lt;li&gt;This paper explains the chemical variation and high SiO&lt;sub&gt;2Â &lt;/sub&gt;percentage of rocks within Tanzawa region, and describes in some depth the tectonic events that uplifted the Tanzawa Mountains. Â &lt;/li&gt;
&lt;/ul&gt;&lt;p&gt;&lt;strong&gt;Additional resources:&lt;br /&gt;&lt;/strong&gt;&lt;/p&gt;
&lt;p&gt;Kitamura, K., Ishikawa, M., and Arima, M., 2003, Petrological model of the northern Izu-Bonin-Mariana Arc crust; constraints from high-pressure measurements of elastic wave velocities of the Tanzawa plutonic rocks, central Japan: Tectonophysics, v. 371, p.213-221,Â &lt;br /&gt;link:Â http://dx.doi.org/10.1016/S0040-1951(03)00229-4&lt;/p&gt;
&lt;ul&gt;&lt;li&gt;
&lt;p&gt;This paper researchs the variations in acoustic impedance between different hornblende-gabbroic rocks from Tanzawa, Japan.Â &lt;/p&gt;
&lt;/li&gt;
&lt;/ul&gt;&lt;p&gt;Mikami, K., 1953, Metamorphic rocks in the southeastern margin of the Tanzawa quartz-diorite mass: Science Reports of Yokohama National University, v. 2, p. 34-49&lt;/p&gt;
&lt;ul&gt;&lt;li&gt;This paper studies the chemical analysis of amphibolites resulting from contact metamorphism of the quartz-diorite mass in the Tanzawa Mountains.&lt;/li&gt;
&lt;/ul&gt;&lt;p&gt;Tani, K., Dunkley, D. J., Kimura, J., Wysoczanski, R.J., Yamada, K., and Tatsumi, Y.,2010,Â Syncollisional rapid granitic magma formation in an arc-arc collision zone: Evidence from the Tanzawa plutonic complex, Japan:Â Geology [Boulder], v. 38, p.215-218,Â &lt;br /&gt;link:Â http://dx.doi.org/10.1130/G30526.1&lt;/p&gt;
&lt;ul&gt;&lt;li&gt;
&lt;p&gt;This paper discusses the collison that exposed the gabbroic rocks of the Tanzawa plutonic complex, and overall gives the reader an in-depth sturctural history of the Tanzawa Mountains.Â &lt;/p&gt;
&lt;/li&gt;
&lt;/ul&gt;&lt;p&gt;Yoshimura, T., 1997, Ca-Al silicates in low-grade metavolcanic rocks from southern Tanzawa Mountains, Central Japan: Journal of Mineralogy Petrology and Economic Geology, Â v. 92, p. 363-378, &lt;br /&gt;link: http://dx.doi.org/10.2465/ganko.92.363.&lt;/p&gt;
&lt;ul&gt;&lt;li&gt;
&lt;p&gt;This paper explains prevalence of greenschist facies within the Tanzawa Mountain region, and gives the mineral composition of rocks from southern region of Tanzawa Mountains.&lt;/p&gt;
&lt;/li&gt;
&lt;/ul&gt;&lt;p&gt;Â &lt;/p&gt;
&lt;p&gt;Â &lt;/p&gt;
&lt;p&gt;Â &lt;/p&gt;
&lt;p&gt;&lt;br /&gt;&lt;br /&gt;&lt;/p&gt;</text>
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              <description>Spatial characteristics of the resource.</description>
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                  <text>The samples were found in the Tanzawa Mountains of Kanto, Japan. &#13;
</text>
                </elementText>
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            <element elementId="116">
              <name>Temporal Coverage</name>
              <description>Temporal characteristics of the resource.</description>
              <elementTextContainer>
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                  <text>The Tanzawa Mountains were formed during the late Pliocene. </text>
                </elementText>
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          <description>Formation or other descriptive rock category</description>
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              <text>Greenschist Facies Volcanic (Zone IV)</text>
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            <description>An account of the resource</description>
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                <text>Rock Sample:&#13;
The sample color is light brown to dark brown in color with white residue through out the surface. The rock has a light green tint. There is a greasy luster to the sample.  There are large white veins and planes of cleavage that follow a foliation pattern.  The large white veins react with acid.  There is a petal-like residue of white and brown minerals.  The sample experienced chemical weathering.  The rock has a silty texture.&#13;
&#13;
Thin Section:&#13;
There are some small veins.  The matrix is too small to identify with a microscope but it is dark in color while under PPL and a very light yellow color under XPL.  Some of the plagioclase is curved.  The matrix intergrown in many of the quartz crystals.  The sample is holocrystalline.  &#13;
-Quartz (75%)&#13;
-Unknown Matrix (~15-25%)&#13;
-Plagioclase (~7%)&#13;
-Magnification at 4x/0.10</text>
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