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Sillimanite is an index mineral for high temperature and variable pressure metamorphism.

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Graphite is a form of carbon, while sillimanite is a type of aluminum silicate mineral. Graphite is known for its excellent conductivity and lubricating properties, while sillimanite is valued for its high heat resistance and hardness.

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kyanite and sillimanite

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John Thomas Cheney has written:

'Mineralogy and petrology of lower sillimanite through sillimanite + K-feldspar zone pelitic schists, Puzzle Mountain area, N.W. Maine' -- subject(s): Petrology, Sillimanite, Mineralogy

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Sillimanite is the Official State Mineral.

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Sillimanite, nickel, petroleum

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Sillimanite, nickel, petroleum

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Yes, zircon, ilmenite, and sillimanite are commonly found in the beach sands of Kerala. However, tungsten is not typically present in significant quantities in these sands. These minerals are important sources of valuable elements and are often extracted through beach sand mining operations.

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Delaware's state gem is the sillimanite, which is a rare polymorph of andalusite and kyanite. It was designated as the state gem in 1977.

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Delaware does not have a state rock, or a state gemstone, but the state mineral is sillimanite.

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D. H. de Jager has written:

'Sillimanite in Namaqualand'

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Nephrite is an ornamental gemstone. It begins with the letter N.

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No, andalusite, sillimanite, and kyanite are not sedimentary rocks. They are metamorphic minerals that form under high-pressure and high-temperature conditions from the metamorphism of aluminum-rich rocks like schist or pelitic rocks.

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Kyanite and its two related minerals, andalusite and sillimanite, are used primarily in the glass-making, metallurgy, refractory, and ceramic industries.

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Two examples of index minerals are kyanite and staurolite. These minerals are used by geologists to determine the metamorphic grade of a rock based on their presence and abundance.

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David Joseph Hall has written:

'Compositional variations in biotites and garnets from kyanite and sillimanite zone mica schists, Orange area, Massachusetts and New Hampshire' -- subject(s): Biotite, Garnet

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Some minerals found in Delaware include quartz, feldspar, mica, kaolinite, and garnet. The state also has deposits of sand, gravel, and clay minerals. Mining activities in Delaware primarily focus on industrial minerals used in construction and manufacturing.

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There are many types of refractory bricks available. Those are Andalusite Bricks, Dense Silica Brick for Glass Furnace, Corundum Mullite Brick, Corundum Brick, Fireclay Brick for Coke Oven, Fireclay Brick for Blast Furnace, Low Creep High Alumina Brick for Hot Stoves, High Alumina Bricks for Blast Furnaces, General Refractory Fireclay Brick, General High alumina refractory brick, Insulating firebrick, Silica bricks-coke oven refractories, Magnesia brick, Magnesia Bricks for Cement Industry, High Alumina Bricks For Cement Industry, Fused cast Bricks, Sillimanite Bottom Blocks, Low Porosity Fireclay Bricks, Zirconia Bricks, General fireclay brick for steel industry, Refractory insulating fire brick B&C series, Insulating bricks etc.

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Metamorphic rocks do not have a single chemical formula as they are composed of minerals that vary depending on the parent rock and the conditions of metamorphism. Common minerals found in metamorphic rocks include quartz, feldspar, mica, and calcite, among others. The chemical composition of metamorphic rocks can be complex and vary widely.

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The three main rock types are igneous, sedimentary, and metamorphic. Igneous rocks are formed from the solidification of molten material, sedimentary rocks are formed from the accumulation and lithification of sediments, and metamorphic rocks are formed when existing rocks are subjected to high heat and pressure, causing them to recrystallize. Each type has unique characteristics such as texture, mineral composition, and origin that differentiate them from one another.

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Metamorphic rocks are igneous, sedimentary, and metamorphic rocks that have been altered by heat, pressure, or ion exchange. Therefore, there is a wide range of metamorphic rock component material.

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Metamorphic rocks have undergone changes in temperature and pressure, causing them to recrystallize. Look for distinct mineral layers, banding, or foliation in the rock, which are common features of metamorphic rocks. Additionally, metamorphic rocks often have a shiny or glassy appearance due to the rearrangement of minerals during metamorphism.

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Linear change on reheating means that the size of refractory products is irreversible changed when the refractory products are heated to high temperature. A positive value indicates expansion which is called expansion of linear change on reheating; negative value indicates contraction which is called contraction of linear change on reheating.

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Introduction:

Lead-Zinc deposits in India are localized mainly in the Precambrian formations of the Peninsular Shield and to a smaller extent in the lesser Himalayas. The important economically viable deposits are located in two main regions of India viz., Western Region and Southern Region with some scattered deposits in other parts such as North and Eastern Regions.

Western Deposits:

The Western Region comprises Rajasthan and Gujarat States. Copper-lead-zinc mineralization occurs as bi-and multi-metal deposits and 95% of National Ore Resource is confined to this region. There are two distinct metallogenic provinces; the north-eastern parts characterized by predominantly copper rich province, confined to the rocks of Delhi Super group, whereas in South Rajasthan and North Gujarat, the mineralization is chiefly lead-zinc ores with subordinate copper in the rocks of Pre- Aravalli, Aravalli and Delhi Super group (Table 1).

Bhilwara Super group:

Rajpura-Dariba-Bethumni Belt:

The Rajpura-Dariba-Bethumani belt is considered to form the western limb of Banera-Bhinder synform extending from Bhinder in the south to Banera in the north over a distance of about 130km.

The Dariba-Bethumani belt, extending from Bethumani in the north and Dariba in the south is composed of a group of folded met sedimentary rocks belonging to the Bhilwara Super group of pre-Aravalli age. Numerous old workings, gossans and ferruginous breccias have been recorded in the southern part of the belt in the Rajpura-Dariba area. The ore deposit is strata bound and is enclosed in a sequence comprising metamorphic equivalents of ortho-quartzite, carbonates and carbonaceous faces which are flanked by a thick monotonous sequence of meta-argillites. Rajpura-Dariba ore body owes its importance to its multi-metal sulphide-sulphosalt associations within the ores.

Zinc is dominant metal followed by lead and copper. The important trace metals are cadmium and silver. The sulphide ores at Dariba mine show conspicuous mineralogical zoning. Copper, lead-zinc and iron rich zones appear successively from the footwall to hanging wall. Two important lodes viz., Main and East lode, separated by a parting of 150 m, occur at Rajpura-Dariba. The main lode is further divided into South lode and North lode.

Rajpura-Dariba has been developed as a 3000 TPD underground mine with matching beneficiation facilities. The other less significant deposits are Mokhanpura North and South, Sindesar Kalan (East) and Malikhera block which are low in metal content and hosted by graphitic schist.

HZL is also exploring at Bamnia Kalan, which is 14 km north of Rajpura-Dariba mine, where the lead-zinc mineralization occurs in calc-silicate/dolomite and garnet bearing carbonaceous schist. Two distinct zones of mineralization viz., Main Zone and West Zone occur in this area. In the Main Zone, ore lenses are of variable dimensions, disposed in encephalon pattern with dextral overlap in sympathy with complicated fold pattern.

Rampura Agucha Lead-Zinc Deposit:

Introduction

The Rampura Agucha lead-zinc deposit is located 15 km southeast of Gulabpura in the Bhilwara district, Rajasthan. The village Rampura, originally located adjoining the western flank of the deposit was rehabilitated in 1990, prior to the commencement of open pit operation and Agucha village is about 1.5 km southwest of the deposit. The proximity of these two village led to the naming of it's as" Rampura-Agucha deposit". Since its discovery in 1977, the deposit has attained significance because of its large potential and geological setting not known to be conducive for mineralization. The deposits forms a part of pre-Aravalli Banded Gneissic Complex consisting of gneisses, schist and intrusive of acidic and basic igneous rocks that occupy, predominantly, the southeastern plains of Ajmer and Bhilwara.

Discovery and History of Exploration:

Garnet is found in almost all rock types around Rampura-Agucha deposit. In connection with an assessment of the potential of semi-precious and abrasive varieties of garnet of the area, T.C. Rampuria of Directorate of Mines and Geology, Government of Rajasthan (DMG), observed multicolored gossan bands, slag dumps and a linear shallow depression in the vicinity, in August, 1977. Preliminary geological, geophysical and geochemical surveys were made by DMG Rajasthan in 1978 and 1979, which resulted in indications of good potential and surface drilling in May, 1979.

Such indications attracted the attention of Hindustan Zinc Limited (HZL), which proposed detailed exploration through 15,500 m of surface drilling and 500 m of underground development, which was approved in February 1980, at estimated expenditure of Rs. 12.5 million.

Geology of the Deposit

Since a greater part of the area is capped with soil cover and fresh rock exposures are scanty, much of the information for detailed geology was gathered from the drill cores. The rock units show NE-SW strike with steep dips in hanging wall (75°-80°) and moderate dips in footwall (60°-65°) towards south-eats and plunges towards NNE. The sequence of rocks, from hanging wall to footwall, can be broadly grouped as under:

1. Garnet-biotite-sillimanite gneiss with intermittent bands of calc-granulites, amphibolites and aplites/ pegmatite's

2. Garnet-mica-sillimanite gneiss/ schist

3. Garnet-biotite-sillimanite gneiss with lenses of quartzo-felsphathic bands, amphibolites, pegmatite's and aplites

4. Granite gneiss, and

5. Mylonitic rocks.

Ore Zone

Economic mineralization is predominantly in graphite-mica-sillimanite gneiss / schist over a strike length of 1550m. The ore zone has a sharp contact with the hanging wall and footwall. The hanging wall side of the lode is the richest and also wide, followed by comparatively lean grade in the middle and a narrow, rich, footwall zone. Coarse-grained crystalline galena, associated with pyrite and pyrrohitite are seen in the hanging wall rocks. The mineralization's in hanging wall and footwall contacts is invariably fine to coarse-grained, and is made up of sphalerite and galena with numerous inclusions or rounded to sub-rounded discrete grains of feldspar, quartz, hornblende, sillimanite and dark green chlorite.

Attitude of the ore zone:

The general strike of the ore zone is parallel to the enclosing rocks, which is roughly NE-SW. The dip of the ore zone varies along the strike and depth. Near the surface, the dip of the hanging wall contact is steeper (75° to 80°SE) as compared to footwall contact (about 60° SE). In depth, dips of both the hanging and footwall contacts show a tendency to flatten. In general, the dip varies from 50° to 80°. The ore zone shows a variation in width, both along the strike and dip. The width of the ore zone gradually widens to about 95 to 100m between latitudes S-200 and S-400.

Mineralogy of the Ore Body

The graphite-mica-sillimanite schist hosts the economic mineralizations in Rampura-Agucha deposit. The economic minerals in the order of decreasing abundance along with their ranges of modal percentages are: sphalerite (15-20%), pyrite (15-18%), pyrrhotite (12-14%), galena (1-2%) and sulphosalts (0.1-0.2%). Graphite is ubiquitous in the ore body (7-10%). The gangue minerals that amount up to 45% to 50% of the ore zone constitute quartz, feldspar (orthoclase, plagioclase), various micaceous minerals (sericite, chlorite, and biotite), sillimanite with significant amount of garnets, amphibole, pyroxene, rutile, apatite etc.

Mining

The Rampura Agucha deposit at comparatively shallow depth is ideally suited for open pit mining using conventional equipment. The ore body is comparatively narrower and richer in grade in the northern part and wider in the southern. Thus open pit operation can go deeper only in the southern part.

Aravalli Super group

Zawar Lead-Zinc Belt

The Archaean basement comprising of gneiss, schist, amphibolite, quartzite and granite dating back to 3.2 to 2.5 by. showing unconformable relationship with the Aravalli cover rocks, is clearly marked in and around Udaipur. Stratigraphic succession, established by Roy et.al., (1984,b) for the Aravalli Super group of the type area around Udaipur and Zawar show two major groups separated by an unconformity. The Upper Aravalli Group consists of greywacke-slate-phyllite, quartzite, dolomite and silty arenite (host for sulphides of zinc and lead) while carbonaceous and pelitic phyllites, dolomite, quartzite, stromatolyte, phosphorite, chlorite schist, amphibolites, quartz arenite and local conglomerate belong to Lower Aravalli Group.

In general, Aravalli rocks in Udaipur-Zawar region show a low-grade metamorphism. The recrystallisation of the silicate minerals suggests the grade of metamorphism to be of greenschist facies. A few dyke-like bodies, intrusive in Aravalli rocks of Zawar, occur as totally unreformed.

The present structural disposition of Zawar area is the manifestation of two distinct major periods of tectonic cycles, each of which was characterized by intense folding and faulting. In Zawar area, the north and south limb of cross fold is represented by Mochia, Balaria and Bowa, whereas Baroi and Zawarmala represent the north-south trending and northerly plunging first generation fold system.

The mineralization occurs as sheated zones, veins stringers and disseminations, forming lenticular bodies arranged in overlapping enechelon pattern. The individual ore shoots persist along strike between 50 and 500 m, dip between 50° and vertical and plunge between 30° and 60° west or north. The ore body varies in width between 1 and 40 meters.

The mineralization is restricted solely within dolomitic horizon along with the structural control, but regional stratigraphic and litho logical control is also evident. The main sulphide minerals are sphalerite, pyrite and galena. Chalcopyrite, pyrrhotite and arsenopyrite are the associated minerals. Appreciable amount of silver and cadmium occur within the ore minerals.

Zawar belt has been the oldest centre of lead-zinc production in the world. The producing deposits are- Mochia, Balaria, Zawarmala and Baroi. Zawar group of mines has a capacity of 4000 TPD from underground mines with matching beneficiation facility and infrastructure.

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The three rock types are sedimentary, igneous, and metamorphic. At one time, early in Earth's history, all rocks were igneous, having solidified from molten rock. From a textural point of view the differences are as follows: Sedimentary: grains of similar or differing sizes showing variable sphericity and roundness either grain or matrix supported. Igneous: crystalline grains interlocking but not showing any preferred orientation. Metamorphic: crystalline grains (for the most part except low grade metamorphic rocks) interlocking, showing preferred orientation (alignment) and associated metamorphic minerals such as garnet, kyanite and sillimanite for example. Formation:Igneous rocks, which are formed from magma cooling underground, or lava above ground are formed from previous igneous, metamorphic, or sedimentary rocks which have become melted, usually as a result of plate collision and subduction. When these igneous rocks are exposed to weathering and erosion, they break down into smaller particles that are transported by wind and water to a place of deposition, where they can form into sedimentaryrock strata, through a process of lithification, where excess water is squeezed out by overburden pressures and the particles are cemented together by various minerals precipitating out of solution. Igneous and metamorphic rocks can both be turned into sedimentary rocks in this way. Igneous and sedimentary rocks can also be changed by heat and/or pressure into metamorphic rocks, by transforming their existing mineral structures into new minerals or realigning the existing minerals. There are different degrees of metamorphism, so even an existing metamorphic rock can become a different metamorphic rock.

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Earl Victor Shannon has written:

'Notes on anglesite, anthrophyllite, calcite, datolite, sillimanite, stilpnomelane, tetrahedrite and triplite' -- subject(s): Mineralogy

'Tschermigite, ammoniojarosite, epsomite, celestite, and paligorskite from southern Utah' -- subject(s): Mineralogy

'Miargyrite silver ore from the Randsburg district, California' -- subject(s): Miargyrite, Mineralogy, Silver ores

'The mineralogy and petrology of intrusive Triassic diabase at Goose Creek, Loudon County, Virginia' -- subject(s): Diabase, Mineralogy, Petrology

'Notes on an andorite-bearing silver ore from Nevada' -- subject(s): Andorite, Silver ores

'The oxidation of meteoric irons with comparative descriptions of two new examples of magnetic iron oxides from terrestrial sources' -- subject(s): Iron oxides, Meteorites

'Boulangerite, bismutoplagionite, naumannite and a silver-bearing variety of jamesonite' -- subject(s): Mineralogy

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Igneous rocks are formed from the solidification of molten material, such as lava or magma. Sedimentary rocks are formed from the accumulation and compaction of sediment over time. Metamorphic rocks are formed from the alteration of existing rocks through heat, pressure, or chemical processes. Igneous rocks have a crystalline structure, sedimentary rocks often contain fossils, and metamorphic rocks exhibit foliation.

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Metamorphism can be defined as the solid state recrystallisation of pre-existing rocks due to changes in heat and/or pressure and/or introduction of fluids i.e without melting. There will be mineralogical, chemical and crystallographic changes. Metamorphism produced with increasing pressure and temperature conditions is known as prograde metamorphism. Conversely, decreasing temperatures and pressure characterize retrograde metamorphism. Kinds of metamorphism Regional or Barrovian metamorphism covers large areas of continental crust typically associated with mountain ranges, particularly subduction zones or the roots of previously eroded mountains. Conditions producing widespread regionally metamorphosed rocks occur during an orogenic event. The collision of two continental plates or island arcs with continental plates produce the extreme compressional forces required for the metamorphic changes typical of regional metamorphism. These orogenic mountains are later eroded, exposing the intensely deformed rocks typical of their cores. The conditions within the subducting slab as it plunges toward the mantle in a subduction zone also produce regional metamorphic effects. The techniques of structural geology are used to unravel the collisional history and determine the forces involved. Regional metamorphism can be described and classified into metamorphic facies or zones of temperature/pressure conditions throughout the orogenic terrane. Metamorphic facies

Metamorphic facies are recognizable terranes or zones with an equilibrium assemblage of key minerals that were in equilibrium under specific range of temperature and pressure during a metamorphic event. The facies are named after the metamorphic rock formed under those facies conditions from basalt. Facies relationships were first described by Eskola (1920). Facies: * Low T - low P : Zeolite * Mod - high T - low P : Prehnite-Pumpellyite * High-P low T : Blueschist * Mod P - Mod to high T: Greenschist - Amphibolite - Granulite * High P - Mod - high T : Eclogite

In the Barrovian sequence (described by George Barrow in zones of progressive metamorphism in Scotland), metamorphic grades are also classified by mineral assemblage based on the appearance of key minerals in rocks of pelitic (shaly, aluminous) origin: Low grade ------------------- Intermediate --------------------- High grade : Greenschist ------------- Amphibolite ----------------------- Granulite : Slate --- Phyllite ---- Schist --------- Gneiss -----------------------Migmatite(partial metling) >>>melt : Chlorite zone :: ::: :::: Biotite zone ::::: :::::: ::::::: Garnet zone :::::::: ::::::::: :::::::::: Staurolite zone ::::::::::: :::::::::::: ::::::::::::: Kyanite zone :::::::::::::: ::::::::::::::: :::::::::::::::: Sillimanite zone Contact metamorphism occurs typically around intrusive igneous rocks as a result of the temperature increase caused by the intrusion of magma into cooler country rock. The area surrounding the intrusion (called aureoles) where the contact metamorphism effects are present is called the metamorphic aureole. Contact metamorphic rocks are usually known as hornfels. Rocks formed by contact metamorphism may not present signs of strong deformation and are often fine-grained. Contact metamorphism is greater adjacent to the intrusion and dissipates with distance from the contact. The size of the aureole depends on the heat of the intrusive, its size, and the temperature difference with the wall rocks. Dikes generally have small aureoles with minimal metamorphism whereas large ultramafic intrusions can have significantly thick and well-developed contact metamorphism. The metamorphic grade of an aureole is measured by the peak metamorphic mineral which forms in the aureole. This is usually related to the metamorphic temperatures of pelitic or alumonisilicate rocks and the minerals they form. The metamorphic grades of aureoles are andalusite hornfels, sillimanite hornfels, pyroxene hornfels. Magmatic fluids coming from the intrusive rock may also take part in the metamorphic reactions. Extensive addition of magmatic fluids can significantly modify the chemistry of the affected rocks. In this case the metamorphism grades into metasomatism. If the intruded rock is rich in carbonate the result is a skarn. Fluorine-rich magmatic waters which leave a cooling granite may often form greisens within and adjacent to the contact of the granite. Metasomatic altered aureoles can localize the deposition of metallic ore minerals and thus are of economic interest. Hydrothermal metamorphism is the result of the interaction of a rock with a high-temperature fluid of variable composition. The difference in composition between existing rock and the invading fluid triggers a set of metamorphic and metasomatic reactions. The hydrothermal fluid may be magmatic (originate in an intruding magma), circulating groundwater, or ocean water. Convective circulation of water in the ocean floor basalts produces extensive hydrothermal metamorphism adjacent to spreading centers and other submarine volcanic areas. The patterns of this hydrothermal alteration is used as a guide in the search for deposits of valuable metal ores. This kind of metamorphism occurs when either an extraterrestrial object (a meteorite for instance) collides with the Earth's surface or during an extremely violent volcanic eruption. Impact metamorphism is, therefore, characterized by ultrahigh pressure conditions and low temperature. The resulting minerals (such as SiO2 polymorphs coesite and stishovite) and textures are characteristic of these conditions. Dynamic metamorphism is associated with major fault planes. Metamorphism is localised adjacent to the fault plane and is caused by frictional heat generated by the fault movement. Cataclasis, crushing and grinding of rocks into angular fragments, occurs in dynamic metamorphic zones, giving cataclastic texture. The textures of dynamic metamorphic zones are dependent on the depth at which they were formed, as the confining pressure determines the deformation mechanisms which predominate. Within depths less than 5km, dynamic metamorphism is not often produced because the confining pressure is too low to produce frictional heat. Instead, a zone of breccia or cataclasite is formed, with the rock milled and broken into random fragments. This generally forms a mélange. At depth, the angular breccias transit into a ductile shear texture and into mylonite zones. Within the depth range of 5-10km pseudotachylite is formed, as the confining pressure is enough to prevent brecciation and milling and thus energy is focused into discrete fault planes. The frictional heating in this case may melt the rock to form pseudotachylite glass or mylonite, and adjacent to these zones, result in growth of new mineral assemblages. Within the depth range of 10-20km, deformation is governed by ductile deformation conditions and hence frictional heating is dispersed throughout shear zones, resulting in a weaker thermal imprint and distributed deformation. Here, deformation forms mylonite, with dynamothermal metamorphism observed rarely as the growth of porphyroblasts in mylonite zones. Overthrusting may juxtapose hot lower crustal rocks against cooler mid and upper crust blocks, resulting in conductive heat transfer and localised contact metamorphism of the cooler blocks adjacent to the hotter blocks, and often retrograde metamorphism in the hotter blocks. The metamorphic assemblages in this case are diagnostic of the depth and temperature and the throw of the fault and can also be dated to give an age of the thrusting. Metamorphism is further divided into prograde and retrograde metamorphism. Prograde metamorphism involves the change of mineral assemblages (paragenesis) with increasing temperature and (usually) pressure conditions. These are solid state dehydration reactions, and involve the loss of volatiles such as water or carbon dioxide. Prograde metamorphism results in a rock representing the maximum pressure and temperature experienced. These rocks often return to the surface without undergoing retrograde metamorphism , where the mineral assemblages would become more stable under lower pressures and temperatures. Retrograde metamorphism involves the reconstitution of a rock under decreasing temperatures (and usually pressures) where revolatisation occurs; allowing the mineral assemblages formed in prograde metamorphism to return to more stable minerals at the lower pressures. This is a relatively uncommon process, because volatiles must be present for retrograde metamorphism to occur. Most metamorphic rocks return to the surface as a representation of the maximum pressures and temperatures they have undergone. == ==

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== == Rocks that have undergone a change in mineral structure or composition, without melting, through heat and/or pressure are metamorphic rocks. Examples are slate, anthracite, and gneiss.

How does contact (prograde) occur? the changes in mineral assemblage and mineral composition that occur during burial and heating are referred to as prograde metamorphism.

Where does contact (prograde) occur? Contact metamorphism occurs typically around intrusive igneous rocks as a result of the temperature increase caused by the intrusion of magma into cooler country rock. The area surrounding the intrusion where the contact metamorphism effects are present is called the metamorphic aureole. Contact metamorphic rocks are usually known ashornfels. Rocks formed by contact metamorphism may not present signs of strong deformation and are often fine-grained.

Why does contact (prograde) occur? Contact metamorphism occurs typically around intrusive igneous rocks as a result of the temperature increase caused by the intrusion of magma into cooler country rock. The area surrounding the intrusion where the contact metamorphism effects are present is called the metamorphic aureole.[5] Contact metamorphic rocks are usually known ashornfels. Rocks formed by contact metamorphism may not present signs of strong deformation and are often fine-grained.

Contact metamorphism is greater adjacent to the intrusion and dissipates with distance from the contact. The size of the aureole depends on the heat of the intrusion, its size, and the temperature difference with the wall rocks. Dikes generally have small aureoles with minimal metamorphism whereas large ultramafic intrusions can have significantly thick and well-developed contact metamorphism.

The metamorphic grade of an aureole is measured by the peak metamorphic mineral which forms in the aureole. This is usually related to the metamorphic temperatures ofpelitic or alumonisilicate rocks and the minerals they form.The metamorphic grades of aureoles are andalusite hornfels, sillimanite hornfels, pyroxene hornfels.

Magmatic fluids coming from the intrusive rock may also take part in the metamorphic reactions. Extensive addition of magmatic fluids can significantly modify the chemistry of the affected rocks. In this case the metamorphism grades into metasomatism. If the intruded rock is rich in carbonate the result is a skarn. Fluorine-rich magmatic waters which leave a cooling granite may often form greisens within and adjacent to the contact of the granite. Metasomatic altered aureoles can localize the deposition of metallic oreminerals and thus are of economic interest.

Prograde and retrograde metamorphism[edit]

Metamorphism is further divided into prograde and retrograde metamorphism. Prograde metamorphism involves the change of mineral assemblages (paragenesis) with increasing temperature and (usually) pressure conditions. These are solid state dehydration reactions, and involve the loss of volatiles such as water or carbon dioxide. Prograde metamorphism results in rock characteristic of the maximum pressure and temperature experienced. Metamorphic rocks usually do not undergo further change when they are brought back to the surface.

Retrograde metamorphism involves the reconstitution of a rock via revolatisation under decreasing temperatures (and usually pressures), allowing the mineral assemblages formed in prograde metamorphism to revert to those more stable at less extreme conditions. This is a relatively uncommon process, because volatiles must be present.

Garnets with Mn-rich cores and Mn-poorer rims record growth zoning that represents the change from the lower-T conditions at which the garnet core grew to the higher-T conditions at which the garnet rim grew (i.e., prograde metamorphism involving increasing temperature and pressure). Mn is preferentially partitioned into garnet relative to most other common minerals, so Mn is sequestered in early-formed garnet, depleting the local environment of the growing garnet in Mn.

(b) Minerals that show major element growth zoning probably did not experience very high metamorphic temperatures. At high temperature (> 700 C) and sufficient duration, zoning may be homogenized as intracrystalline diffusion becomes more effective at eliminating compositional variation. An unzoned mineral that is typically zoned at low-medium metamorphic grades has either experienced high temperature conditions or was never zoned (owing to a simple reaction history at limited P-T or to growth entirely at high-T).

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== == Rocks that have undergone a change in mineral structure or composition, without melting, through heat and/or pressure are metamorphic rocks. Examples are slate, anthracite, and gneiss.

How does contact (prograde) occur? the changes in mineral assemblage and mineral composition that occur during burial and heating are referred to as prograde metamorphism.

Where does contact (prograde) occur? Contact metamorphism occurs typically around intrusive igneous rocks as a result of the temperature increase caused by the intrusion of magma into cooler country rock. The area surrounding the intrusion where the contact metamorphism effects are present is called the metamorphic aureole. Contact metamorphic rocks are usually known ashornfels. Rocks formed by contact metamorphism may not present signs of strong deformation and are often fine-grained.

Why does contact (prograde) occur? Contact metamorphism occurs typically around intrusive igneous rocks as a result of the temperature increase caused by the intrusion of magma into cooler country rock. The area surrounding the intrusion where the contact metamorphism effects are present is called the metamorphic aureole.[5] Contact metamorphic rocks are usually known ashornfels. Rocks formed by contact metamorphism may not present signs of strong deformation and are often fine-grained.

Contact metamorphism is greater adjacent to the intrusion and dissipates with distance from the contact. The size of the aureole depends on the heat of the intrusion, its size, and the temperature difference with the wall rocks. Dikes generally have small aureoles with minimal metamorphism whereas large ultramafic intrusions can have significantly thick and well-developed contact metamorphism.

The metamorphic grade of an aureole is measured by the peak metamorphic mineral which forms in the aureole. This is usually related to the metamorphic temperatures ofpelitic or alumonisilicate rocks and the minerals they form.The metamorphic grades of aureoles are andalusite hornfels, sillimanite hornfels, pyroxene hornfels.

Magmatic fluids coming from the intrusive rock may also take part in the metamorphic reactions. Extensive addition of magmatic fluids can significantly modify the chemistry of the affected rocks. In this case the metamorphism grades into metasomatism. If the intruded rock is rich in carbonate the result is a skarn. Fluorine-rich magmatic waters which leave a cooling granite may often form greisens within and adjacent to the contact of the granite. Metasomatic altered aureoles can localize the deposition of metallic oreminerals and thus are of economic interest.

Prograde and retrograde metamorphism[edit]

Metamorphism is further divided into prograde and retrograde metamorphism. Prograde metamorphism involves the change of mineral assemblages (paragenesis) with increasing temperature and (usually) pressure conditions. These are solid state dehydration reactions, and involve the loss of volatiles such as water or carbon dioxide. Prograde metamorphism results in rock characteristic of the maximum pressure and temperature experienced. Metamorphic rocks usually do not undergo further change when they are brought back to the surface.

Retrograde metamorphism involves the reconstitution of a rock via revolatisation under decreasing temperatures (and usually pressures), allowing the mineral assemblages formed in prograde metamorphism to revert to those more stable at less extreme conditions. This is a relatively uncommon process, because volatiles must be present.

Garnets with Mn-rich cores and Mn-poorer rims record growth zoning that represents the change from the lower-T conditions at which the garnet core grew to the higher-T conditions at which the garnet rim grew (i.e., prograde metamorphism involving increasing temperature and pressure). Mn is preferentially partitioned into garnet relative to most other common minerals, so Mn is sequestered in early-formed garnet, depleting the local environment of the growing garnet in Mn.

(b) Minerals that show major element growth zoning probably did not experience very high metamorphic temperatures. At high temperature (> 700 C) and sufficient duration, zoning may be homogenized as intracrystalline diffusion becomes more effective at eliminating compositional variation. An unzoned mineral that is typically zoned at low-medium metamorphic grades has either experienced high temperature conditions or was never zoned (owing to a simple reaction history at limited P-T or to growth entirely at high-T).

3 answers


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2089 words found.

4 answers