Finishing updates
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@@ -21,7 +21,7 @@
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<li><a href="{% url 'three_d_viewer:erb101_theory_structure' %}"><span>Structure of Earth</span></a></li>
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<li><a href="{% url 'three_d_viewer:erb101_theory_pt' %}"><span>Pressure and temperature</span></a></li>
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<li><a href="{% url 'three_d_viewer:erb101_theory_bowen' %}"><span>Bowen's reaction series</span></a></li>
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<li><a href="{% url 'three_d_viewer:theory_classification' %}"><span>Classification of minerals</span></a></li>
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<li><a href="{% url 'three_d_viewer:erb101_theory_classification' %}"><span>Classification of minerals</span></a></li>
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<li><a href="{% url 'three_d_viewer:erb101_theory_silicates' %}"><span>Silicates</span></a></li>
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<li class='last'><a href="{% url 'three_d_viewer:erb101_theory_crystals' %}"><span>Crystals</span></a></li>
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{% endblock %}
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@@ -0,0 +1,32 @@
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{% extends "three_d_viewer/base.html" %}
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{% load static %}
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{% block content %}
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<div id="pushDownTwo"></div>
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<div id="mainText">
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<h1 class="subHeadings">Theory</h1>
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<h2 class="theoryHeadings" id="classification">Classification of Minerals</h2>
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<p>
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The classification of minerals is based on their chemistry. The following mineral classes are based on the character of their common anions:</p>
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<li><p>Silicates (SiO<sub>4</sub><sup>4-</sup>)</p></li>
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<li><p>Oxides (O<sup>2-</sup>)</p></li>
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<li><p>Sulfides (S<sup>2-</sup>)</p></li>
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<li><p>Sulfates (SO<sub>4</sub><sup>2-</sup>)</p></li>
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<li><p>Halides (Cl<sup>-</sup>)</p></li>
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<li><p>Fluorites (F<sup>-</sup>)</p></li>
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<li><p>Phosphates (PO<sub>4</sub><sup>3-</sup>)</p></li>
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<li><p>Carbonates (CO<sub>3</sub><sup>2-</sup>)</p></li>
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<li><p>Native elements, e.g. Au.</p></li>
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<p><br />
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The relative abundance of elements in the Earth’s crust (? Composition and structure of Earth) determines which minerals form.
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As we can see in table x, oxygen is the most abundant anion in the Earth’s crust.
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Thus, the crust can be seen as a tight package of oxygen anions (O<sup>2-</sup>), which are bonded by larger cations,
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such as Si<sup>4+</sup>, Mg<sup>2+</sup>, or Al<sup>3+</sup>.
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The way atoms are packed together depends on the cation to anion radius ratio (Rx/Rz).
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With oxygen as the major anion, specific coordination and coordination polyhedra can be expected for different cations.
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<br /><br /><br />
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<a href="{% url 'three_d_viewer:theory_silicates' %}"><span>Silicate minerals</span></a>
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</p>
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<div id="pushDownThree"></div>
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</div>
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{% endblock %}
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@@ -13,7 +13,7 @@
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continental environments. Ocean crust is young mafic crust dominated by basalts and gabbros that is recycled regularly(~300Ma) due to subduction processes.
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Continental crust is much more varied in structure and composition than oceanic, but has an overall average composition of granodiorite.
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<br /><br />
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The boundary of the crust and mantle is defined by the Mohorovi?i? discontinuity, commonly referred to as the Moho.
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The boundary of the crust and mantle is defined by the Mohorovičić discontinuity, commonly referred to as the Moho.
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It is defined by a sharp increase in seismic wave velocity, due to a change in material properties between crustal rocks and mantle rocks. The mantle is dominated by
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silicate minerals that are rich in iron and magnesium, chiefly pyroxenes and polymorphs of olivine, forming peridotite. The mantle, while solid, behaves plastically,
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allowing to flow at very slow rates.
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@@ -7,25 +7,25 @@
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<h1 class="subHeadings">Theory</h1>
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<h2 class="theoryHeadings" id="bowensreactionseries">Bowen's Reaction Series</h2>
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<p>
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Bowen's Reaction Series arranges the silicate minerals (? Silicate minerals) in the order that they crystallize from magma. The minerals at the
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Bowen's Reaction Series arranges the <a href="{% url 'three_d_viewer:theory_silicates' %}"><span>silicate minerals</span></a> in the order that they crystallize from magma. The minerals at the
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top of the series crystallize from the melt at higher temperature than those lower down. It contains a continuous series, (right hand limb), a
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discontinuous series (left hand limb), and the residual phases, which are listed in their relative sequence of crystallization. The discontinuous
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series describes the sequence of minerals that crystallize as the temperature of the magma decreases. The discontinuity of each of the
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crystallization sequences reflects the different melting/crystallization temperatures of the minerals, and the change in composition of the
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residual magma, as the early crystallizing phases are being fractionated from the melt. The continuous series always crystallizes plagioclase,
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residual magma, as the early crystallizing phases are being fractionated from the melt. The continuous series always crystallizes <a href={% url 'three_d_viewer:'|add:plag.url plag.id %}>plagioclase</a>,
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but the composition of the plagioclase changes from more calcic (i.e. anorthite) at higher temperatures to more sodic (i.e. albite) as the
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temperature decreases. The compositional change during mineral growth can be recorded in compositional zoning of plagioclase
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crystals (see ? Solid-solution series). The minerals at the bottom of Bowen’s reaction series crystallize last and are more stable,
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and less susceptible to weathering. Thus, Bowen's reaction series also predicts the stability of minerals (? Stability of minerals) in the
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crystals. The minerals at the bottom of Bowen’s reaction series crystallize last and are more stable,
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and less susceptible to weathering. Thus, Bowen's reaction series also predicts the stability of minerals in the
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low pressure conditions at the Earth's surface.
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<br /><br />
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It should be noted that all reactions do not start crystallizing olivine/anorthite-rich plagioclase and continue through until they
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crystallize quartz (? Quartz). Which minerals actually form, depend on many factors, such as the chemical composition of the melt, temperature,
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pressure, and amount of fractional crystallization. For example, basalts form from the crystallization of olivine, pyroxene and
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crystallize <a href={% url url_extender|add:quartz.url quartz.id %}>quartz</a>. Which minerals actually form, depend on many factors, such as the chemical composition of the melt, temperature,
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pressure, and amount of fractional crystallization. For example, basalts form from the crystallization of
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<a href={% url url_extender|add:olivine.url olivine.id %}>olivine</a>,
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<a href={% url url_extenderadd:diopside.url diopside.id %}>pyroxene</a> and
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calcic plagioclase, meaning that crystallization stopped without the series progressing. If more fractional crystallization
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(? Fractional crystallization) were to occur, more intermediate and felsic minerals can crystallize. Such a differentiation path is
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illustrated in the TAS diagram, where primitive igneous rocks (i.e. basaltic) evolve to more felsic
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(SiO2-rich; i.e. rhyolite) ones (? TAS diagram).
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were to occur, more intermediate and felsic minerals can crystallize.
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<br/>
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<img src="{% static "three_d_viewer/images/bowen.jpg" %}" style="padding-top:20px; text-align: left;" width="600px" height="auto">
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</p>
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@@ -8,7 +8,7 @@
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<h2 class="theoryHeadings" id="classification">Classification of Minerals</h2>
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<p>
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The classification of minerals is based on their chemistry. The following mineral classes are based on the character of their common anions:</p>
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<li><p>Silicates (SiO<sub>4</sub><sup>4-</sup>)</p></li>
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<li><p><a href="{% url 'three_d_viewer:theory_silicates' %}"><span>Silicates</span></a> (SiO<sub>4</sub><sup>4-</sup>)</p></li>
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<li><p>Oxides (O<sup>2-</sup>)</p></li>
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<li><p>Sulfides (S<sup>2-</sup>)</p></li>
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<li><p>Sulfates (SO<sub>4</sub><sup>2-</sup>)</p></li>
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@@ -18,14 +18,13 @@
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<li><p>Carbonates (CO<sub>3</sub><sup>2-</sup>)</p></li>
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<li><p>Native elements, e.g. Au.</p></li>
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<p><br />
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The relative abundance of elements in the Earth’s crust (? Composition and structure of Earth) determines which minerals form.
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As we can see in table x, oxygen is the most abundant anion in the Earth’s crust.
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<img src="{% static "three_d_viewer/images/element abundance.png" %}" align="right" width="412" height="324">
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The relative abundance of elements in the Earth’s crust (see <a href="{% url 'three_d_viewer:theory_structure' %}"><span>Structure of Earth</span></a>) determines which minerals form.
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Oxygen is the most abundant anion in the Earth’s crust.
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Thus, the crust can be seen as a tight package of oxygen anions (O<sup>2-</sup>), which are bonded by larger cations,
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such as Si<sup>4+</sup>, Mg<sup>2+</sup>, or Al<sup>3+</sup>.
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The way atoms are packed together depends on the cation to anion radius ratio (Rx/Rz).
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With oxygen as the major anion, specific coordination and coordination polyhedra can be expected for different cations.
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<br /><br /><br />
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<a href="{% url 'three_d_viewer:theory_silicates' %}"><span>Silicate minerals</span></a>
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</p>
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<div id="pushDownThree"></div>
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</div>
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@@ -12,7 +12,9 @@
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gravitational collapse emerged the proto-Sun and a surrounding disk of dust and gas. Attraction forces within this rotating
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protoplanetary disk that fed the young Sun, led to the accretion of progressively growing objects and planetesimals.
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Increasing mass and gravitational forces of the growing planetary bodies resulted in interactions and disturbance in their orbits,
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ultimately giving rise to larger collisions. Earth, as a terrestrial inner planet formed relatively close to the Sun through the
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ultimately giving rise to larger collisions.
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<br /><br />
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Earth, as a terrestrial inner planet formed relatively close to the Sun through the
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accumulation of rather heavier matter, whereas the outer planets formed from gas that had been blown away in more distal
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regions of the solar system (solar wind). Continuous bombardment and larger impacts – including one that led to the
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formation of the Moon -, and the radioactive decay within the Earth heated the planet resulting in partial melting.
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@@ -20,6 +22,7 @@
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silicate mantle. Further chemical differentiation by partial melting of the mantle led to the formation of Earth’s proto-crust.
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The Earth’s layering into core, mantle and crust due to this early differentiation remains an essential
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feature of the Earth’s structure.
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<br /><br />
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</p>
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<figure>
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<a href="{% static "three_d_viewer/images/earth differentiation.png" %}"><img width=600 height=350 src="{% static "three_d_viewer/images/earth differentiation.png" %}">
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@@ -30,7 +30,7 @@
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The method of heat transfer changes throughout the Earth. There are three main mechanisms for heat transfer in the Earth:
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conduction, convection, and radiation. Starting in the inner core, the main method of heat transfer is by conduction through the
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solid material. In the liquid, outer core heat transfer is by both conduction and convection. The mantle is dominated by convection,
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which is the driver of plate tectonics (? Plate tectonics). The crust is again dominated by conduction, and finally energy escapes the
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which is the driver of plate tectonics. The crust is again dominated by conduction, and finally energy escapes the
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Earth to the atmosphere by radiation.
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<br /><br />
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Pressure in the Earth continually increases with depth, according to the formula P = gρz, where g is the gravitation field strength,
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@@ -39,7 +39,7 @@
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and increases to about 3.3 g/cm<sup>3</sup> in the mantle. The increase of pressure with depth in the Earth affects the dominant mineralogy,
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as well as the increase of the melting point of different minerals.
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<br /><br />
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The structure of minerals, such as <a href={% url 'three_d_viewer:'|add:olivine.url olivine.id %}>olivine</a> becomes unstable as pressure increases (? Stability of minerals).
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The structure of minerals, such as <a href={% url url_extender|add:olivine.url olivine.id %}>olivine</a> becomes unstable as pressure increases.
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Below about 410 km olivine (Mg<sub>2</sub>SiO<sub>4</sub>) becomes unstable and transforms into wadsleyite (Mg<sub>2</sub>SiO<sub>4</sub>),
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which has the same chemical composition as olivine, but has a different crystal structure. As depth increases,
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wadsleyite transforms to ringwoodite (Mg<sub>2</sub>SiO<sub>4</sub>) at ~520 km, which subsequently transforms into silicate perovskite
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@@ -26,9 +26,10 @@
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<img src="{% static "three_d_viewer/images/inosilicates.png" %}" align="right">
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In the inosilicates, [SiO<sub>4</sub>]<sup>4-</sup> tedrahedra are linked as chains, which in turn are linked together by cations.
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Single-chain inosilicates form [Si<sub>2</sub>O<sub>6</sub>]<sup>4-</sup> groups, and double-chain inosilicates
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form [Si<sub>4</sub>O<sub>11</sub>]<sup>6-</sup> groups. Pyroxenes, e.g. diopside with the chemical formula
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form [Si<sub>4</sub>O<sub>11</sub>]<sup>6-</sup> groups. Pyroxenes, e.g. <a href={% url url_extender|add:diopside.url diopside.id %}>diopside</a> with the chemical formula
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CaMgSi<sub>2</sub>O<sub>6</sub>, are single-chain, and amphiboles, e.g. hornblende
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(Ca<sub>2</sub>(Mg,Fe,Al)<sub>5</sub>(Al,Si)<sub>8</sub>O<sub>22</sub>(OH)), are double-chain inosilicates.
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(Ca<sub>2</sub>(Mg,Fe,Al)<sub>5</sub>(Al,Si)<sub>8</sub>O<sub>22</sub>(OH)) or <a href={% url url_extender|add:actinolite.url actinolite.id %}>actinolite</a>
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(Ca<sub>2</sub>(Fe,Mg)<sub>5</sub>Si<sub>8</sub>O<sub>22</sub>(OH)<sub>2</sub>) are double-chain inosilicates.
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</p>
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</tr></td>
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<tr><td>
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@@ -38,7 +39,7 @@
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In the nesosilicate group, [SiO<sub>4</sub>]<sup>4-</sup> tedrahedra are isolated from each other and share their oxygens
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with octahedral groups, which contain cations, such as Mg<sup>2+</sup>, Fe<sup>2+</sup>, or Ca<sup>2+</sup>. A common
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rock-forming mineral of the nesosilicate group is
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<a href={% url 'three_d_viewer:'|add:olivine.url olivine.id %}>olivine</a> with the chemical formula
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<a href={% url url_extender|add:olivine.url olivine.id %}>olivine</a> with the chemical formula
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(Mg,Fe)<sub>2</sub>SiO<sub>4</sub>.
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</p>
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</tr></td>
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@@ -65,9 +66,9 @@
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<p>
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<img src="{% static "three_d_viewer/images/tectosilicates.png" %}" align="right">
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Complete linkage of [SiO<sub>4</sub>]<sup>4-</sup> tedrahedra results in the 3-dimensional framework of the tectosilicates.
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<a href={% url 'three_d_viewer:'|add:quartz.url quartz.id %}>Quartz</a> (SiO<sub>2</sub>) and the feldspars
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(<a href={% url 'three_d_viewer:'|add:plag.url plag.id %}>plagioclase</a>,
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<a href={% url 'three_d_viewer:'|add:microcline.url microcline.id %}>microcline</a>)
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<a href={% url url_extender|add:quartz.url quartz.id %}>Quartz</a> (SiO<sub>2</sub>) and the feldspars
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(<a href={% url url_extender|add:plag.url plag.id %}>plagioclase</a>,
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<a href={% url url_extender|add:microcline.url microcline.id %}>microcline</a>)
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(e.g. anorthite, CaAl<sub>2</sub>Si<sub>2</sub>O<sub>8</sub>) are tectosilicates.
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</p>
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</tr></td>
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@@ -6,19 +6,30 @@
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<div id="mainText">
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<h1 class="subHeadings">Theory</h1>
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<h2 class="theoryHeadings" id="structureofearth">Structure of Earth</h2>
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<p>
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The Earth's structure is differentiated in three distinct layers: the core, mantle, and crust (? Earth profile). The layers are distinguished
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by a change in the velocity of seismic waves at their boundaries (? Seismic profile). The crust is the upper most part of the earth, with
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<figure align="left">
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<img src="{% static "three_d_viewer/images/structure - usgs.gif" %}" >
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<figcaption align="left"><p>Image sourced from <a href="http://pubs.usgs.gov/gip/dynamic/graphics/FigS1-1.gif">USGS</a>.</p></figcaption>
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</figure>
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<br />
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<p>The Earth's structure is differentiated in three distinct layers: the core, mantle, and crust. The layers are distinguished
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by a change in the velocity of seismic waves at their boundaries (? Seismic profile).
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The crust is the upper most part of the earth, with
|
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depths ranging from an average of 7 km in the oceans, to an average of 38 km in continental crust. The crust thickens underneath mountain
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ranges, and can reach depths of 90 km underneath the Himalayas. The composition of the crust also differs between oceanic and continental
|
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environments. Ocean crust is young mafic crust dominated by basalts and gabbros that is recycled regularly (~300 Ma) due to subduction
|
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processes (? Subduction). Continental crust is much more varied in structure and composition than oceanic, but has an overall average
|
||||
processes. Continental crust is much more varied in structure and composition than oceanic, but has an overall average
|
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composition of granodiorite.
|
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<br /><br />
|
||||
</p>
|
||||
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<p>
|
||||
<br /><br />
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<img src="{% static "three_d_viewer/images/element abundance.png" %}" align="right" width="412" height="324">
|
||||
The boundary of the crust and mantle is defined by the Mohorovicic discontinuity, commonly referred to as the Moho. It is defined by a
|
||||
sharp increase in seismic wave velocity, due to a change in material properties between crustal rocks and mantle rocks (? Seismic profile).
|
||||
The mantle is dominated by silicate minerals that are rich in iron and magnesium, chiefly pyroxenes and polymorphs (? Polymorphs) of olivine,
|
||||
sharp increase in seismic wave velocity, due to a change in material properties between crustal rocks and mantle rocks.
|
||||
The mantle is dominated by silicate minerals that are rich in iron and magnesium, chiefly
|
||||
<a href={% url url_extender|add:diopside.url diopside.id %}>pyroxenes</a> and polymorphs of
|
||||
<a href={% url url_extender|add:olivine.url olivine.id %}>olivine</a>,
|
||||
forming peridotite. The mantle, while solid, behaves plastically, allowing to flow at very slow rates.
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<br /><br />
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The core is distinguished by the absence of S waves, leading to the inference that the core is liquid.
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@@ -27,15 +38,15 @@
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crystallizing minerals from the liquid part of the core as the Earth cools.
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<br /><br />
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The crust and mantle are also further distinguished by material properties into the lithosphere, asthenosphere, and
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mesosphere (? Earth profile). The chemical composition is uniform throughout the mantle though, but changes in pressure and temperature
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mesosphere. The chemical composition is uniform throughout the mantle though, but changes in pressure and temperature
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determine which polymorphs will exist at different depths. The lithosphere contains the crust, and the upper part of the mantle down
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to ~100 km under oceanic crust, and 200-300 km under continental crust (Twiss & Moores, 2007). The lithosphere-asthenosphere boundary
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is defined by the 1300 K isotherm, which is the temperature where olivine starts to behave viscously. The rocks in the mesosphere are
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under more pressure than those in the asthenosphere, so no longer behave viscously.
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||||
</p>
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<figure>
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<img src="{% static "three_d_viewer/images/structure - usgs.gif" %}" style="padding-top:20px;">
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<figcaption><p>Image sourced from <a href="http://pubs.usgs.gov/gip/dynamic/graphics/FigS1-1.gif">USGS</a>.</p></figcaption>
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<figure align="left" >
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<a href='{% static "three_d_viewer/images/depth profile.png" %}' align="right"><img height=494 width=412 src='{% static "three_d_viewer/images/depth profile.png" %}'></a>
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<figcaption>The seismic profile of the Earth.</figcaption>
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||||
</figure>
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||||
</div>
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<div id="pushDownThree"></div>
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@@ -284,15 +284,25 @@ class TheoryTemplateView(generic.TemplateView):
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def get_context_data(self, **kwargs):
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context = super(TheoryTemplateView, self).get_context_data(**kwargs)
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context['base_template'] = 'three_d_viewer/base.html'
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context['url_extender'] = 'three_d_viewer:'
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context['olivine'] = Mineral.objects.filter(name='Olivine')[0]
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context['quartz'] = Mineral.objects.filter(name='Quartz')[0]
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context['microcline'] = Mineral.objects.filter(name='Microcline')[0]
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context['plag'] = Mineral.objects.filter(name='Plagioclase')[0]
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context['diopside'] = Mineral.objects.filter(name='Diopside')[0]
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context['actinolite'] = Mineral.objects.filter(name='Actinolite')[0]
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return context
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class ERB101TheoryTemplateView(generic.TemplateView):
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||||
def get_context_data(self, **kwargs):
|
||||
context = super(ERB101TheoryTemplateView, self).get_context_data(**kwargs)
|
||||
context['base_template'] = 'three_d_viewer/erb101/base.html'
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context['url_extender'] = 'three_d_viewer:erb101_'
|
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context['olivine'] = Mineral.objects.filter(name='Olivine')[0]
|
||||
context['quartz'] = Mineral.objects.filter(name='Quartz')[0]
|
||||
context['microcline'] = Mineral.objects.filter(name='Microcline')[0]
|
||||
context['plag'] = Mineral.objects.filter(name='Plagioclase')[0]
|
||||
context['diopside'] = Mineral.objects.filter(name='Diopside')[0]
|
||||
context['actinolite'] = Mineral.objects.filter(name='Actinolite')[0]
|
||||
return context
|
||||
|
||||
|
||||
Reference in New Issue
Block a user