A Survey On The Creek Geological History

A Survey On The Creek Geological History
Kevin Wright
GEOL 204
Dr. Miller
June 8th, 2015
Caliente Creek Geological History
1.At the beginning of the Tertiary, there is a layer of andesite breccia–a fast cooling extrusive rock that has not traveled far from its original deposition.
This indicates a volcanic depositional environment. This formation was then intruded by intrusive slower cooling rocks that create a noncomformity
between it and the Walker formation. The tuff breccia in the Walker formation is consistent with the same depositional environment as the andesite
breccia formation as they are both extrusive rocks. It is possible that there was an eruption from a volcano that deposited the highly viscous andesite
rocks followed by slower falling ash, which was then ... Show more content on Helpwriting.net ...
The Freeman–Jewett shale formation is a strong indicator of a low–energy/quiet depositional environment. It is likely this layer was originally
deposited offshore in a marine environment. This is further supported by the following Bena Gravel formation, which is emblematic of a transitional
beach–type environment with pebble size sand and gravel. This coarser layer of sand and gravel overlying the silty and sandy shale could be
evidence for a regressive cycle and receding sea levels. The Bena Gravel formation is eroded by Kern River Gravel which creates a disconformity in
the stratigraphy. The Kern River Gravel has stream like deposits but since it cuts through the Bena Gravel Formation it is suggestive the Kern River
Gravel formation has a delta depositional environment. The Terrace formation suggests a stream depositional environment. If terracing is present, it
indicates a decrease in discharge over time. The next formation, Alluvium, is evidence of an alluvial fan deposition, a glacial deposition that has been
reworked by meltwater, or of a dried lake bed. (Levin p.86). Regardless of which, the Alluvium formation gives away easily to mass wasting to from
the landslide formation.
Most alluvial fan deposits occur near the margins of the depositional basin because they occur in low areas at the base of the Temblor formation or
Sierra Nevada's. The marine deposits, beach
... Get more on HelpWriting.net ...

Rainy Lake Wrench Zone ( Rlwz )
Rainy Lake Wrench Zone (RLWZ)
Most known mineral occurrences in the RRB are in the RLWZ, as it is the best exposed and most explored part of the block. Modest gold and silver
production occurred here in the past (25,000 oz Au; 3,000 oz Ag) and magmatic sulfide deposits have been outlined in the Grassy Portageintrusion
(two separate mineralized zones: 300,000 t @ 1.89% Cu and 300,000 t @ 0.8% Cu; Poulsen 2000). The RLWZ also hosts VMS–style prospects in a
bi–modal volcanic pile that is underlain by a composite trondhjemite–tonalite–gabbro–anorthosite intrusion. Zn is predominant in this volcanic
complex, with lesser Cu, indicating shallow water and (or) low temperature mineralization process affected the rocks. Au has been documented in the
volcanic pile, but may represent orogenic style mineralization. These metal assemblages and the geometry of the volcanic pile are similar to Sturgeon
lake VMS camp (e.g. Hudak 2003), indicating it has potential for hosting economic Zn–Cu deposits. However, the atypical lithologic make–up of the
composite subvolcanic intrusion (i.e. anorthosite–dominated) does not match well–endowed VMS camps (Galley 2003) and the proximal high–grade
metamorphism (amphibolite facies) and strong deformation (shearing) may have compromised the preservation of hypogene mineralized zones. If
mineralized zones are preserved, they could be Au–rich, as the structural setting (bounded by crustal–scale faults) and inferred paleotectonic setting
(rifted arc or

Case Study: Don Valley Brickyard
Sarah Hall, 1000680872September 23, 2014
Lab 1: Don Valley Brickyard Short Pre–Lab Report
1. The geology of Ontario is divided into three layers of rock. The first layer, Precambrian Canadian Shield rocks, is composed of mainly igneous and
metamorphic rocks from the Precambrian Eon. This layer is the eldest at approximately 3–0.8x109 years old and is therefore the bottom–most layer
(L). Although this layer is largely found in the Canadian Shield region of Ontario, glacial erratics from the Precambrian layer can be found at the Don
Valley Brickyard (L). In the GTA, younger sediments and rocks cover the Precambrianrock layer (L). The second layer is Paleozoic rock, composed of
sedimentary rocksвЂЁ. It was deposited 600–400 million years ... Show more content on Helpwriting.net ...
The 440 million year old Georgian Bay Formation is largely composed of fossiliferous grey–black shale (L1R). It also consists grey fine–grained
limestone, sandstone and green/grey siltstone interbedded with green/grey and blue/grey shales (Bond et. al. 1976). The frequency of hard rock units
increases toward the top of the formation. Recurrent tropical storms across the Ordovician seas caused the formation of shady, thin limestone with
wave ripples on top. Numerous fossils can be found in the siltstones and limestone including molluscs, crinoids and gastropods

Hot Springs Observation Paper
In Midway, Utah, there is distinct geologic activity. The area features a collection of rocks spanning through multiple time periods. Also, the
hydrothermal activity in the region is extensive. The hot springs in the area are relatively young, and distinct because of their location and formation. A
closer examination of the hot springs shows that the springs are mineral rich, and form a chemical sedimentary rock.
The ages of the rocks in the area vary greatly. The oldest rock in the area, according to Bromfield, Baker, and Crittenden, is tillite from the Mineral
fork formation, dated back to the Precambrian era (1967). There are Paleozoic and Mesozoic sedimentary rocks in the Wasatch Mountains (Kohler,
1979). The majority of the rock in the ... Show more content on Helpwriting.net ...
The former of the two look like hills, with large openings in the top (Baker, 1968; Kohler, 1979). I captured the top of the mound I was in; it stood
at about 55 feet tall (Willis and Willis, 2000). The spring that I went to is called a Hot Pot. I wasn't able to capture the process of CO2 gas being
released. Regardless, I included a picture of the deep water. The tufa made up all of the walls (and despite being made up of calcite, they were
very stable without reinforcement). In a picture, I captured to solid limestone inside the spring. Also, the tufa deposits in layers (Baker, 1968). I
captured a picture of the layered rock and included it. The spring that I went to, because it was so large, was also a good example of the soil
makeup of the other springs (the soil was fairly stable). The assortment was similar to what Kohler examined, and was mostly sand and gravel (1979).
However, the spring I went to had larger pieces of tufa. The tufa not only made up the natural composition of the mound, but also the entrance; large
pieces of the limestone were lined up against the outside. I captured a picture of this as well. The For the above reasons, the Midway thermal springs
are a hydrothermal anomaly. The history, the location, and the physical makeup of the springs make them extremely

Slave Carton Analysis
The Slave Structural Province is a unique and distinctive Archean craton in the northwest Canadian Shied, which is indicated by its rock types,
deposits and structures (Padgham,1992). The Slave province covers much smaller than (1/10) that of Superior Province, which is about 213 000 km2.
The supracrustals (33% of Slave province) consist of 70–80% of greywacke– mudstone and approximately 20% of volcanic rocks, which is high in
SiO2 (felsic to intermediate) (Padgham,1992). There are abundant mineral deposits in the Slave Province: gold deposits, rare–element–rich pegmatite
and zinc–lead–silver–concentrated volcanogenic massive sulfides (VMS), which differ from the high contents of copper–zinc–gold in the Superior
Province (Padgham & Fyson, 1992).... Show more content on Helpwriting.net ...
All of the volcanic and metasedimentary rocks are metamorphosed, whose grades are extending from greenschist to upper amphibolite, characterized by
low–pressure but high–temperature (Isachsen & Bowring, 1994). The influence of basement fracture zone is reflected in the homoclinal and abruptly
alternated trends of the volcanic belts, which is more frequently found in the southwestern domain of the province, while north belts show angular
patterns (Fyson & Helmstaedt, 1988; Padgham,1992; Padgham & Fyson, 1992). Except for the sharp dips of the volcanics, regional–scale folds,
foliations and cleavages over several successions shown in the metasedimentary rocks are studied to understand the deformation and metamorphism
(Isachsen & Bowring, 1994). Fyson & Helmstaedt (1988) compare three major types of folds which are ranked by their ages and sizes from oldest,
most extensive F0 to minor–sized, cleavage–foliation–associated S3 folds with intermediate type F1 between them and they suggest that the parallel
trend and they suggest both foliation and folds are results of syntectonic

Permin Land Formation Essay
Cape Lieper and Cape Ingersoll formations: They are part of Ryder Gletscher Group. They are mainly composed of dolomites and other carbonates
rocks and they overlie Dallas Bugt Formation with thicknesses of up to 40m (Higgins et al, 1991). Other smaller formations within the Ryder Gletscher
Group include Lower–Middle Cambrian wulff River and Cape Wood formations and they are mainly dominated by irregular bedded micritic limestone
with thickness of up to 150m (Higgins et al, 1991). Cape Kent Formation of Lower Cambrian which was probably formed in a high–energy
depositional environment in shallow water contains oolitic limestone with thickness of up to 10m(Higgins et al, 1991). Permin Land Formation: It is
dominated by medium–to fine–grained well–sorted and rounded sandstone (Higgins et al, 1991). There are also dolomite and siltstone interbed and
features like wave–ripple lamination, flat and low–angle lamination as well as shallow trough & tabular crossbedding are also present indicating a
shallow marine depositional environment. The thickness of Permin Land Formation is up to 50m (Higgins et al, 1991). Johansen Land Formation: It
overlies Permin Land Formation and it is believed to have been formed in an... Show more content on Helpwriting.net ...
The evaporates of Nygaard Bay Formation are probably subaqueous sediments that were formed in a shallow broad saline basin and they contain
irregular & ripple laminations with shaly dolomites interbeds of up to 10m (Higgins et al, 1991). Limestone of probably shallow subtidal to intertidal
origin dominates the lower part of the Nygaard Bay Formation and the combined thickness of the upper and lower parts is up to 40m and it has been
mapped in Washington Land (Higgins et al, 1991). Permin land, Nygaard Bay and Johansen land formations are part of Ryder Gletscher

The Iron Mask Project Is Located At An Elevation Of M 425...
The Iron Mask project is located at an elevation of ~425 m above mean sea level and within the Canadian Shield that is characterized by subdued
topography with rolling hills and numerous lakes and rivers. Vegetation in the area composes a Boreal forest, and includes both coniferous and
mixed–wood forests. Conifer tree species include white and black spruce, balsam, jack pine fir, eastern white cedar, and tamarack, while the deciduous
(hardwood) species are mainly white birch and poplar (https://www.ontario.ca/page/forest–regions). Preliminary access can be made from the town of
Cartier (population ~300 people) via HWY 144, from which the Fox Lake road and the Old Cartier Hwy provide access to within 5 km of the
center of claim area. From the Old Cartier Hwy, forest and lake access roads provide light vehicle access to the center and southern parts of the
property. The northern parts of the area are more remote, requiring access via boat on Clear Lake or a forest road near the northern extent of the
property (Champion Bear, 2003 ). The project area is located in a moderately humid continental climate, with short to moderate length, warm to hot
summers and long, cold winters. Precipitation in Ontario averages 600–1000 mm per year, including ample snowfall in the winter months. Ranges of
temperatures and precipitation in the area are shown in Table 1. The Iron Mask project occurs near the Sudbury Ni–Cu camp, which is part of the
broader Abitibi granite–greenstone terrane

Geology Of The Oaks Belt
Geology of the Oaks Belt The Oaks Belt is composed of mafic to felsic volcanic and volcaniclastic rocks, clastic sedimentary rocks, iron formation
and several generations of intrusive rocks. Mafic volcanic rocks constitute the bulk of the stratigraphy in the OB and occur as both pillowed basalts
and massive flows. They are aphanitic to fine–grained and dark green to black (Frey and Venzke, 1991). Mafic volcaniclastic rocks are more common
lower in stratigraphy. Intermediate volcanic rocks occur almost exclusively as tuffs, are feldspar–phyric and contain 20–30% mica and amphibole. A
package of felsic volcaniclastic rocks tentatively defined as fragmental rhyolites to dacites occur near the stratigraphic top of the volcanic pile and
directly underlie massive sulfide and iron–oxide exhalative horizons. These highly siliceous rocks are mica and amphibole–poor, and occur as both
quartzphyric fragments and tuffs. Felsic agglomerate rocks are common and sometimes show a dacite to rhyolite transition down stratigraphy.
Fragments in agglomerates are sometimes set in a tonalite matrix (Frey and Venzke, 1991). Clastic rocks are most common in the central part of the
study area and sometimes display graded bedding as well as slumping and soft–sediment deformation (Frey and Venzke, 1991).Chemical sedimentary
rocks in the OB include iron formation and chert. Given the tendency of massive sulfide deposits to occur in brecciated piles of tuff fragments with
associated footwall

San Pedro Pellado Volcanic Complex by Davidson, Ferguson,...
Subsequent research focusing more solely on the San Pedro Pellado Volcanic Complex by Davidson, Ferguson, Colucci, and Dungan (1988) provides
evidence that some degree of crustal assimilation has had an impact on the evolution of magmas in the volcanic complex. The evidence for this is the
high Оґ^18O observed in fresh non–glassy rock units. Taylor and Sheppard (1986) argue that the differences in characteristics among rock units of the
complex cannot be explained by the closed system fractionalization of an unaltered mantle melt. The concentrations of the oxygen isotopes suggest that
the magmas that formed these igneous rocks have undergone some contamination with a crustal component containing a higher concentration of 18O
(Davidson et al., 1988). The occasional presence of granitic xenoliths in the lavas and tuffs, such as the Pellado unit, are also indicative of some level
of crustal contamination. These xenoliths are enriched in large ion lithophiles and have similar concentrations of REE as the underlying basement
material and are therefore believed to be pieces of the underlying basement of the volcanic complex (Davidson et al., 1988). For the granites to be
included into the melts as they rise through the crustal material indicates there is some degree of interaction between melts and crustal material. In
addition to alteration by crustal contamination, the magmas of the San Pedro Pellado Complex were also likely subject to alteration by magma mixing
(Davidson et

Teaching Is More Than Simple Worksheets And Powerpoint
Teaching is like a draft, each time you teach you can improve your teaching. This saying my sound silly, but walk into a classroom and teach a lesson
and this saying will become very relevant. Many people overestimate how easy teaching can be. Teaching is more than simple worksheets and
powerpoint that provide the information. Students have variety of needs and have a variety of learning styles and as teachers we need to make
accommodations for each child. There are around twenty–four students and one teacher, these twenty–four students are all unique and different. As a
future teacher, walking into a classroom I needed to think about my objectives, language, assessments, feedback, how successful and unsuccessful my
lesson was, and what I can work on to become a more successful teacher. All of these thoughts are going about a lesson, which can be a ten minute
lesson or a sixty minute lesson. Through this practicum experience my understanding about teaching and learning has deepened and has taught me so
much about what I need to work on to become a more successful teacher. As teacher we expect our students to be always working to better
themselves and as teachers we need to be leading by example, if anything the experience has deepened my intrinsic motivation for becoming a better
teacher. Realization that students come in a variety of different shapes and sizes, and have a variety of diversity. This experience in the classroom and
depended my personal philosophy and guided

Plaster Of Paris
I.Purpose:
The purpose of the experiment is to determine how a mold and cast constructs fossils. The hypothesis is a fossil mold will form after the plaster of
paris is set and dried out. The justification for the hypothesis is a cast will form when an animal or plant is covered in sediments. Once the sediments
start to harden into a rock state the fossil will become captured and preserved. (Wile, 159–162)
II.Materials:
1.Modeling clay or Play–Doh
2.Plaster of paris
3.A paper plate
4.A shell or something with a distinctive design
5.Vaseline or another kind of petroleum jelly
6.Eye protection
III.Procedure:
The shell was covered in petroleum jelly then set on the counter while the modeling clay was being stretched out on plate. Once the modeling clay
was stretched out so it was two times bigger then the shell, the shell was firmly pushed into the clay. Before the shell was removed the plaster of
paris was mixed together using the direction on the package. When the shell was removed it formed the mold, the plaster of paris was poured over the
mold until the mold was filled. The plate was ... Show more content on Helpwriting.net ...
A mold is formed when an animal or plant are captured in sediments later hardening into sedimentary rock. Fossils are typically found in sedimentary
rock because igneous rock is created with magma at a temperature too high for an organic remains to survive. Metaphoric rock is created when
sedimentary or igneous rock has a high temperature and has high pressure. A fossil is able to form in metaphoric rock but the pressure and heat the
fossil is disconfirmed and useless. (Reference, "Why Are Fossils Only Found in Sedimentary Rock?") Weathering will start to affect the rocks form
and mainly the fossil captured inside. Weathering normally has more affect on the fossil causing the fossil inside to disintegrate. Sometimes the rock
will break open and then the only fossil remaining is a mold. (Wile,

Waucoba Wash Quadrangle
Geologic History of Waucoba Wash Quadrangle, California
The Waucoba Wash Quadrangle, California cross section begins with the deposition of the Cambrian layers such as the Campito Formation, Poleta
Formation (upper and middle members and undivided), Harkless Formation, Saline Valley Formation (lower and upper members), Mule Spring
Limestone, Monola Formation (lower and upper members), and the Bonanaza King dolomite (dominantly limestone and undivided). These Cambrian
rocks are followed by rock layers from the Devonian period, thus meaning that an unconformity occurred between the layers. The Devonian dolomite
rock layers include the Hidden Valley dolomite and the Lost Burro Formation (cherty dolomite). These are followed by the Mississippian... Show more
content on Helpwriting.net ...
One of the major things noticeable from the cross section is that quite a few of the rock layers are over turned, where the older rock layers are above
the newer rock layers. This is seen in the contact between the Quartz Monzonite of Papoose Flat and the Campito Formation which is also a
disconformity. Next there is some fault zones separating the Camptio, Poleta, and Harkless formations. We then see some more overturned layers
with the contacts between Saline Spring Valley Formation (lower and upper members) above the Mule Spring Formation along with some inferred
folding. With a normal fault separating the inferred folding event, we see where the overturning occurs. In between the Cambrian layers we see
Tertiary Basalt nonconformities also being folded, thus with that we know that the folding event was more recent than the formation of the Basalt.
Next there is a large Basalt field with a spot of the Harkless formation. Again we see over tuning as the Basalt field ends there are the Devonian and
Mississippian rock Layers on top of the basalt. Separating these overturned layers from the Harkless Formation and the Saline valley Formation (upper
member), which are not overturned, is a thrust fault. From this information, there was a major stress event sometime after the Tertiary period causing
the rock layers to fold and overturn. And from this stress event and from the folding, normal and thrust faults are formed. Finally we see that there were
alluvial and landslide deposits from the Quaternary after the folding, faulting, and over

What Is Petrogenetic Evolution And Magma Genesis?
Petrogenetic Evolution and Magma Genesis
The petrographic and chemical data suggest that the potential source region of the studied volcanic suite is the subcontinental lithosphere mantle. The
analytical data suggest that the composition of primary magma was largely controlled by partial melting which is the critical factor in distinguishing
these continental volcanic rocks. Regarding to mineralogy of silicic rocks, the common presence of irregular and rounded margins which are observed
for a large number of plagioclase crystals that engulf K–feldspar exhibiting rapakivi texture, beside combination with sieve textures point to marginal
melting of these crystals and consequently a process of disequilibrium (in this case thermal) (e.g. ... Show more content on Helpwriting.net ...
Depletion in Nb, Ti, and P is considered to be associated with fractionation of Ti–bearing phases such as ilmenite and titanite, and apatite. Low CaO
(1.4–3.15 %) contents and moderately to strongly negative anomalies of Ba indicate an extensive fractionation of plagioclase and/or K–feldspar (Wu et
al., 2003). This latter type of fractionation coupled with K–feldspar rich composition especially in rhyolite (Table 1, Fig.6A) point to final fractionation
at low pressures (see discussion of liquid–feldspar relations in Carmichael et al., 1974, p231–235). This is also favored by their high Or/Ab ratios
(Table 2, Blundy and Cashman, 2001). This could also be a viable explanation for the exclusively felsic composition of products of the IsbilVolcano.
Thermodynamic modeling on major elements using the MELTS program (Ghiorso and Sack, 1995) has been made in order to evaluate potential
fractional crystallization processes in the felsic magmatism. The evolution of Al2O3 and MgO contents closely matches the whole rock data, when
modeled with a pressure of 2 kbar, a water content of 2 wt.% and fO2 at QFM + 1, in which crystallizations of amphibole, biotite, muscovite, feldspar
and quartz are considered. However, CaO, FeO, and TiO2 deviate from the observed rock compositions. These discrepancies could be due to the
limitations of the MELTS program when applied to

Major Rock Units And Deformation Events
Figure 1: (A) North America with the location of Figure B outlined by the black box. (B) Simplified map of the tectonostratigraphic terranes
comprising the Superior Province with locations of mineral deposits. (C) Tectonostratigraphic terranes of Minnesota. The location of Figure 3a is
denoted by the black box. Terrane boundaries are denoted by thick black lines and iron formation is shown by thin red lines. Table 1: Major
lithologic units of the Wabigoon subprovince in Canada that are on strike with the rocks in the study area. Modified from Davis et al. (1989), Fralick
and Davis (1999), and Czek and Poulsen (2010). Figure 2: Lithostratigraphc correlation of major rock units and deformation events in the Neoarchean
terranes of Minnesota.... Show more content on Helpwriting.net ...
Most drilled massive sulfide deposits and iron formation layers occur near the top of the volcanic pile and overly the flanks of the LLIC. Felsic
rocks underlying massive sulfide deposits in the top of the volcanic pile are FI and FII types. Rocks with a magnetic signature similar to known
massive sulfide deposits occur down section and over the center of the LLIC. These rocks are interpreted as having the highest potential for hosting
Au–rich VMS deposits. Mafic rocks of the Oaks Intrusion (OI) occur in the eastern part of the belt and have been dated at 2671В±8 Ma (Keatts et al,
2003). Likely time correlative to the OI, a magnetic mafic sill (Oaks Intrusion sill; OIS) intruded and inflated the volcanic pile after or
contemporaneously with the main deformation event (D2). Table 2: Magnetic susceptibility of common igneous rocks used for interpretation and
modeling. From Ford (2008) and Anderson et al. (2013). Figure 4: Profiles of magnetic data on cross sections A–A', B–B', and C–C'. The location of
these cross section lines is shown on Figure 3b and Figure 6. Location of massive sulfides (MS), the Lost Lake Intrusive Complex (LLIC), magnetic
halos (MH) surrounding the LLIC, the Oaks Intrusion sill (OIS), and faults (FLT) are labeled on residual field magnetic data plots. Vertical and
horizontal derivative techniques outline shallow, highly magnetic causative anomalies

The Grand Canyon By John Wesley Powell
Introduction
On May 24, 1869, Major John Wesley Powell set off to explore the Grand Canyon and discovered its beauty to educate the world about this vast
landscape. Before his discovery, it had been known as Big Canyon, neither are appropriate titles. Grand is an understatement to describe this canyon.
Majestic would be a better description as it is defined as lofty dignity as well as sublime beauty, which greatness can't be measured or imitated. The
extraordinary splendor of its landscape can't be compared and its history is just as impressive. It is considered one of the seven wonders of the world
with reason.
The Grand Canyon was named such in 1871 and in 1919 the Grand Canyon became a National Park. Before becoming a National Park Grand
Canyon was given Federal protection in 1893 as a Forest Reserve. A few years later, Grand Canyon became a National Monument. The mission was
to preserve the park and its features. It was to leave the canyon pristine for the future while providing a way visitors could enjoy the park.
The Grand Canyon is located in Northern Arizona and is part of the Colorado Plateau that was uplifted during tectonic activity. It is said to be more
than 1.7 billion years old and filled with many mysteries still about its formation. This immense canyon was cut by the Colorado River that exposed its
horizontal layers of rock history. These layers have mostly a red hue but each group of strata has a distinctive color often giving us a sign of its origin.

Geological Structure And Lithology Of Platforms Rocks
Geological structure and lithology of platforms rocks are considered as crucial importance in determining both the process of formation and
development of shore platforms (Edwards 1941; Trenhaile 1987; Sunamura 1992; Kennedy 2010; Dickson et al 2004; Naylor and Stephenson 2010;
Thornton and Stephenson 2006).
Trenhaile (1987) defined three areas that geology will be affectively controlled the process of formation and development of shore platforms: 1) erosion
process; 2) platform profiles; and 3) degree of inheritance of shore platforms.
Rock lithology, structure and mineralogy could be determined the erosion processed operated upon the shore platforms. Rocks that is thinly bedded
and well jointed will be eroded dominantly be wave quarrying. Rocks that absorb large quantity of water are probably more susceptible to erode by
chemical solution. Accumulated debris size at the cliff foot is determined geological factors which in turn determine the amount of erosion rate of cliff.
Rock dip affects the surface morphology shape. Washboard relief develops in steeply dipping, thinly bedded strata. Smooth surface of platforms occurs
when dip is shallow or horizontal.
Rocks strength is controlled either platforms are completely or partially inheritance from previous sea level rising. If the platforms developed in softer
rocks sediments will be probably completely eroded by rising sea level but if the rocks is harder it may be inherent by past sea level.
Edwards (1941) is the

Anne Sexton Metaphor
Daniel Jung
English 1114: 003
01 October 2014
Poetry is a Code; The Key Often is Metaphor:
Anne Sexton's "You All Know the Story of the Other Woman Poetry is an art form that is rich in notional and semantic content. In a few stanzas,
poems are so capable of painting an idea or event so vividly that it seems alive. However poetry, by itself, cannot exhibit qualities of life: they require
a willingness to understand unfamiliar ways of describing a phenomenon. Thus poetry has been likened to a scrambled code that is impossible to
decipher in its literal context. Thus, poetry requires a key to decipher it and the code, often, is metaphor.
In "You All Know the Story of the Other Woman", Sexton first introduces the setting claiming that "It's a little Walden" (Sexton, 1). The "little Walden"
(1) is the first key that assists in decoding the Sexton's poem – it is a metaphor that refers to an isolated and tranquil residence. However the following
lines depict a scene of action, not peace, resulting in an ... Show more content on Helpwriting.net ...
By likening the man's actions as a body that "takes off and flies, / flies straight as an arrow" (3–4), it is evident that there is a sexual interaction
between a man and woman; however their relationship is unclear. Analysing Sexton's choice of "arrow" (4) suggests that the woman is a one–time
attraction for the man because an arrow flies straight and is physically incapable of returning to the bow from which it was strung. However, the
metaphor does not reveal the relationship between the two, it can only be assumed and thus, according to Sexton, it is "a bad translation" (5) which
suggests that although the metaphor is capable of describing the physicality of their relationship, it is ineffective at describing the esoteric qualities.
Thus it becomes glaringly apparent that a single metaphor is incapable of completely unlocking the code of poetry – although it does, in part, decode
some aspect of the

The Geology Of The Peninsular Terrane
out along a ~400–km–long, NE–striking belt within the Kahiltna basin (Fig. 1). They are mainly flysch deposits inter–preted to have been derived
primarily from the igneous rocks of the Peninsular terrane to the southeast, with local contri–butions from the Triassic Chilikadrotna Greenstones to the
northwest (Wallace et al., 1989; Wilson et al., 2006).
The Peninsular terrane is a Triassic to Jurassic island–arc complex that was accreted to the North American craton by the Early Cretaceous (Detterman
and Reed, 1980; Jones et al., 1987; Ridgway et al., 2002; Trop et al., 2002, 2005; Clift et al., 2005). The terrane includes mafic to andesitic flows
and volcaniclastic rocks, limestone, and mudstone. These rocks structurally overlie and are intruded by Jurassic plutonic rocks of the Talkeetna arc
(Reed and Lanphere, 1973; Reed et al., 1983; Rioux et al., 2010). The plutonic rocks include gabbroic to granitic compositions, but are dominated by
quartz diorite and tonalite rocks (Detterman and Reed, 1980; Reed et al., 1983).
The Togiak terrane, located west of the Peninsular terrane, is an island–arc complex that contains Late Triassic to Early Cretaceous basaltic to dacitic
volcanic and volcaniclastic rocks and graywacke (Decker et al., 1994). These rocks were ac–creted to the North American craton during the middle to
late Early Cretaceous (Box, 1985).
The Peninsular and Togiak terranes are separated by the Farewell terrane (Fig. 1) that contains a Lower Paleozoic through Lower

Pebble Day Narrative
Pebble had just arrived at her grandmother Boulder's house who was seated in her rock–ing chair. Pebble had always wondered how her grandmother
had ended up as an Igneous rock and decided that today she would ask. "Grandmother, how is it you became a igneous rock?"
"Oh, twas a long long long time ago. One billion years, I believe, when I underwent my first change that lead me to what I am today." she reminisced
with a faraway look in her eye.
"Wow one billion! You sure are old grandma." Pebble blurted.
"Hmph, kids these days have no respect for their elder," Grandmother scolded, eyeing her granddaughter. "Tell me, is it that rowdyrock music that
influenced your rude behavior? When I was a whippersnapper ..."
"Sorry grandma, what happened ... Show more content on Helpwriting.net ...
"Years later, I was at an amusement park on a school field trip on one of the hottest days of the year. In fact, it was so hot that I guess a lot of rocks
had the same idea. It was so crowded that I could barely roll a centimeter. At that moment, I realized that I had gotten separated from my class! I
hurried to look around, but I could barely move past the packed crowd of rocks in front of the most popular ride. Stones pushed and pressed against
one another trying to get on the ride. I soon forgot about my class and pressed against the crowd in my effort to get in line. I waited in the packed
crowd in an unbearable heat for thousands of years. By the time it was my turn, I had become a Metamorphic rock to my surprise."
"If you became a Metamorphic rock again, then how are you an Igneous right now?" asked Pebble.
"Well I have changed hundreds of times over the years, it's called the rock cycle. This is just my current form but it can change when you least expect
it. "
" Do you think I'm going to change too!?" demanded Pebble.
"Of course you will, it all depends on the conditions you're under." replied grandma
"Well, when it happens at least now I know that it's okay." said

The Geology Of Ontario Through Its Rocks
Minerals are what make–up Rocks and rocks are what make up the geology of an area. In this report, we will focus on the geology of Ontario through
its rocks. We will look at ten difference rocks samples that have been collected from several different places here in Windsor Ontario including the
beach, the river, gravel pits, along highways and roadways as well in parks and campsites. The rocks that were collected are all rocks that have formed
right here in Ontario.
Canada and especially Ontario have very interesting and much filled geologic pasts. Ontario has many types of rocks and minerals that have formed
and are still forming due to the geology. Ontario has sedimentary rocks; igneous rock, and metamorphic rock as well as minerals such as gold, silver,
quartz, and many more. In this paper, we will begin by talking about ten rocks that were collected right here in Windsor Ontario. The rocks were
examined from the outside which tended to be weathered and the inside which were fresh.
Description of rock types:
The collection of the rocks was based on just picking up the most amount of difference looking rocks that was possible and bringing them home to
analyze. This was done for about two months from many difference locations including campgrounds, beaches, rivers, highways as well as construction
sites. After about two months there were many rocks so I started to analyze and take out the rocks that were of the same kind. I found many granite,
basalt and conglomerate rocks.

Bedrocks In The Handcart Gulch
The bedrocks in the Handcart Gulch consist of Proterozoic meta–sediment and meta–igneous rocks and Tertiary porphyry intrusive rocks (Bove et al
2012, Lovering 1935). Bove et al., (2002) measured rock properties including mineralogy, alteration, and bulk chemistry from recovered cores. Four
deep wells (WP1–WP4) were located in the upper portions of the watershed, and nine shallow wells were along the main channels (HC wells). The
WP1 was located on ridge top of Webster Pass at 3687 m, and drilled to a depth of 610 m, and WP2 was located in the upper portions of the
watershed, and dilled to a depth of 460 m. The felsic rocks in WP1 and 2 were hydrothermally altered due to the intrusion, and the degree of alteration
varied with depth. In upper sections, the rocks were altered to quartz–sericite–pyrite mineral assemblages, whose depths extended to 300 m in WP1 and
200m in WP2. In deeper sections, the rocks were weakly altered to propylitic assemblages that contain calcite, chlorite, and primary feldspars.

Statement Of Purpose In Mining Engineering
Statement of Purpose
To whom it may concern,
"In the mountains the shortest way is from pick to pick." Friedrich Nietzsche (1844–1900) I have always believed that various branches of sciences are
separated from a stout unique body that its roots are made from basic sciences of physics, mathematics and chemistry. Similar to three main colors of
Green, Blue and Red, their combination creates other majors.
It was perhaps my acquaintance with mathematics in high school that later shaped the rest of my life. I still vividly remember the day my mathematics
teacher approached me to encourage me to participate in a mathematics contest at the provincial level in 2004. There were almost three hundred
contestants to compete in different fields of mathematics, ranging from Algebra, Probability, Numeric theories and Geometry to Differential. When the
results came out, I realized I had outstripped all the candidates ... Show more content on Helpwriting.net ...
Furthermore, I strongly believe that an American academic environment is the best place for me to achieve this, because not only it would provide me
with a magnificent atmosphere to broaden my horizons, but also it has the reputation for being the best place to experience practical team work. I am
very excited about the prospect of studying Mining Engineering at this university, as I believe it will open the doors to a wealth of opportunities In
the future. The program is intensive and covers all topics of my interest in detail. So I corresponded with Dr. Elizabeth Holley, who works in the areas
of my interest such as Mineral Exploration especially for porphyry and epithermal deposits and her supportive response encouraged me to apply to
your university. I am confident that my solid background, creativity, communication skills and passion for learning will allow me to succeed in the

and several generations of intrusive rocks. Mafic volcanic rocks constitute the bulk of the stratigraphy in the OB and occur as both pillowed basalts
and massive flows. They are aphanitic to fine–grained and dark green to black (Frey and Venzke, 1991). Mafic volcaniclastic rocks are more common
lower in stratigraphy. Intermediate volcanic rocks occur almost exclusively as tuffs, are feldspar–phyric and contain 20–30% mica and amphibole.
Felsic volcaniclastic rocks vary from rhyolites to dacites and occur mainly near the stratigraphic top of the volcanic pile where they directly underlie
massive sulfide and iron formation deposits. These highly siliceous rocks are mica and amphibole–poor, and occur as both quartzphyric fragments and
tuffs. Felsic agglomerate rocks transition from dacite to rhyolite down stratigraphy (Frey and Venzke, 1991). Clastic rocks are most common in the
central part of the study area and display graded bedding as well as slumping and soft–sediment deformation (Frey and Venzke, 1991).Chemical
sedimentary rocks in the OB include iron formation and chert. The tendency of massive sulfide deposits to occur in brecciated piles of tuff fragments
with associated footwall alteration indicates they are not seawater precipitates. Chert is typically sulfidic, with pyrite and pyrrhotite as the main sulfide
minerals.

Essay on The Science of Rocks
1.According to Thompson and Turk (2011), there are two types of igneous rocks–extrusive and intrusive–and the primary difference between the two
types of igneous rocks is that the rocks are formed in two separate locations: within the Earth's crust and on the Earth's surface (35). Extrusive igneous
rocks form when "magma rises all the way through the crust to erupt onto Earth's surface" (35). Since the crystals do not have much time to grow,
extrusive sedimentary rocks, also commonly known as volcanic rocks, have "fine–grained textures, with crystals too small to be seen with the naked
eye" (Thompson & Turk, 2011, 36). For example, basalt is a common very fine–grained volcanic rock. On the other hand, intrusive igneous rocks form
when ... Show more content on Helpwriting.net ...
The difference in the mineral composition is apparent in the rocks' color and grain texture. Since basalt is a mafic rock, it tends to have a dark green
to black, dark color, while granite tends to have a clear, white, and pink light color (Thompson & Turk, 2011, 37). Additionally, because basalt is an
extrusive igneous rock, it has a very fine–grained texture, meaning that the crystals are nearly impossible to see (Thompson & Turk, 2011, 36). On the
other hand, granite is an intrusive igneous rock, meaning that it has a medium– or coarse–grained texture, where the mineral grains and crystals are
easily visible (Thompson & Turk, 2011, 36).
3.According to Thompson and Turk (2011), sedimentary rocks are broadly divided into four categories: clastic, organic, chemical, and bioclastic rocks.
Clastic sedimentary rock is "composed of particles of weathered rocks, such as sand grains and pebbles (also known as clasts), which have been
transported, deposited, and lithified" (38). Clastic rocks, such as shale, siltstone, and sandstone, are composed of fragments of older rocks: clay, silt,
and sand (38). Moreover, organic sedimentary rocks consist of "lithified remains of plants or animals," and the most common examples are coal, which
is made up of decomposed and compacted plant remains and

Magma Contamination And Sulfide Immiscibility Of The...
MAGMA CONTAMINATION AND SULFIDE IMMISCIBILITY OF THE METEORIC IMPACT ZONE IN THE SUDBURY NI
–CU DEPOSITS:
ONTARIO, CANADA
WILLIAMS, Jane B. (University of Wisconsin–Eau Claire, willijan@uwec.edu)
Sudbury, Canada is the location of a world class Ni–Cu deposit phenomena. Numerous studies have produced an explanation for the complex evolution
of its deposition and enrichment thanks to the impaction of a meteorite 1.85 million years ago. The impact of the meteorite is thought to have caused
fracturing that led to the generation of magma from deep in the crust that helped in later filling the crater and producing the igneous complex (Faggart
et. al., 1985). The igneous complex (Figure 1a) has an elongated shape (60 km long and 27 km wide) with circular deposits surrounding it similar to a
bulls–eye. Evidence of the meteoric impact includes brecciation located in the center of the basin (Onaping Formation), deformation of the margin of
the intrusive complex (Huronian Group), shatter cones, and pseudotachylite. The meteor is thought to have flash melted the crust which proceeded to
differentiate into a granophyre and a leuconorite to norite composition. The granophyre makes up 60% of the complex and the leuconorite and norite
make up the remaining 40% (Figure 1b)(Barnes et. al., 2005). About 50% of the ore is found in the sublayer norite and the breccia that is associated
with the norite. This ore is mainly disseminated sulphides. The massive sulphides are located in the center

Rocks
Rock Report Exercise
Due Date: 4/1/2014Name: Rianne Richter Class: 1121k Grade: /35
After you have finished Lab Exercises 4, 5, and 7, complete the following questions. You may have to refer to the exercises for assistance to locate
specific answers.
1. Match the rock type with the correct statement describing its formation. (3 point).
вќ– Found where the atmosphere or liquid water causes erosion and movement of rock pieces. Metamorphic Formation
вќ– Found mostly near convergent tectonic plate boundaries where the P/T condition can be very high. ... Show more content on Helpwriting.net ...
|Planet |Water |Atmosphere |Molten interior |Plate tectonics |
|Mercury |No |No |Early on |No |
|Venus |No |Thick |Yes |No |
|Earth |Liquid, ice |Medium |Yes |Yes |
|Moon |No |No |Early on |No |
|Mars |Ice |Thin |For a while, no more |No |
10. Where in our solar system might we find igneous rocks? (Hint: what factors are necessary for igneous rocks to form?) (2 point)
11. Where is our solar system might we find metamorphic rocks? (Hint: what factors are necessary for metamorphic rocks to form?) (2 point)
Earth only, need plate tectonics for changing of rocks.
12. Where is our solar system might we find sedimentary rocks? (Hint: what factors are necessary for sedimentary rocks to form?) (2 point)

13. What is

Wilberns Formation Essay
The Wilberns formation has never been studied in the subsurface. Barnes & Bell performed the last encompassing study of the Wilberns in 1977 and
the analysis was all performed on outcropping surface rocks. Modern techniques and understanding of carbonate and clastic petrology and sub–surface
mineral core will help to shed new light on the very complex Wilberns Formation. Information garnered from this new study could help to better
understand Cambrian aged hydrocarbon reservoirs and source rocks, as well as mixed lithofacies aquifers. The goals of this study are as follows: 1)
Find and describe the member contacts within the Wilberns in the subsurface. 2) Determine stratigraphic facies and lithofacies along with
corresponding depositional environments.... Show more content on Helpwriting.net ...
From the core analysis and description, precise boundaries between the four members of the Wilberns Formation were described, allowing for further
study of the Wilberns in the subsurface. Other than the member boundaries, various flooding surfaces and cycle sets were identified and described.
From the core description and analysis areas of interest marked for further analysis by using thin sections. Thirty thin sections will be taken from the
Harold – Johanson MC – 1 core. The thin sections were picked at random areas that were deemed interesting. Six or more spots per member were
chosen. The thin sections will be analyzed with a petrographic microscope to determine mineral content, cementing, hydrocarbon staining, porosity and
permeability, as well as any microfossils present. The Harold – Johanson MC – 1 core was continuously slabbed throughout the entire Wilberns
interval. This allowed a rare opportunity to differentiate the members of the Wilberns formation despite their gradational nature. Core analysis and
description of lithofacies aided the interpretation of depositional environments and paleoenvironmental

Rocks and Dates Geology Analysis
The Grand Canyon is a wonderful place to gain a sense of how old the earth really is because of the ability to date the layers of rock in the canyon.
The Rocks exposed in Grand Canyon are truly ancient, ranging from 1840 million years old or 1.84 billion years old (to 270 million years of age.
(Beus, and Morales, 2003). While the Grand Canyon is not old in comparison to much of the earth, it is considered young earth because it was
slivered by an ie in the last six million years. This gives the rocks in the Canyon Ice age fossils and new deposits, in the grand scheme of things.
Some of the younger deposits in the Canyon are only a thousand years old and are the result of lava that began to come into the geographic. It is the
walls of the... Show more content on Helpwriting.net ...
The oldest recorded rock in the Grand Canyon is Elves Chasm Gneiss. It is speculated to have formed in 1840 m.y. and is older than any other rock
found in the Grand Canyon. The specific origin of the Elves Chasm formation is unclear, but researchers believe that it may have formed from
fragments of continental crust (Dehler, et al, 1999). It is said that most of the rocks in the canyon formed between 1750 and 1680 Ma. It is most
likely that the area of the Grand Canyon was volcanic and the rest of the canyons deep crevasses were created by erosion from water. This also shows
that the canyon area was at a peak with metamorphism and igneous interference.
Vishnu Schist is common in the Grand Canyon along with three other kinds of Schist. The estimated time that this schist formed was between 1700
and 1600 Ma. Each of the schist are formed from different rock types. The most well–known, Vishnu Schist was formed from metamorphosed
sedimentary rock. The other schist Brahma and Rama Schist's are formed from metamorphosed volcanic rock. (Dehler, et al, 1999). The schist rocks,
which are metamorphic are actually categorized as Paleoproterozoic supracrustal rocks. These types of rock are found in the Upper Granite Gorge. In
their article, Tectonic evolution of Paleoproterozoic rocks in the Grand Canyon: Insights into middle–crustal process, Bradley Ilg, Karl Karlstrom,
David Hawkins,

Callytharra Formation Essay
4.3 Methods
Methods used included, taking GPS points at different rock units and marking them onto an aerial map to distinguish bearings and lithologies,
traversing the area, and identifying rock and fossils types.
4.4 Regional Geology
The Callytharra Formation and associated unit Moogooloo Sandstone are found in the Merlinleigh Sub–basin of the Southern Carnarvon Basin. The
Callytharra Formation was forming toward the end of the last major glaciation and represents formations that were deposited in a cool temperate
climate. Moogooloo Sandstone is restricted within the Merlinleigh Sub–basin, within an average thickness of 35m (Mory & Backhouse, 1997)
4.5 Lithology/Palaeontology
The Moogooloo Sandstone formed in the early Permian and consists ... Show more content on Helpwriting.net ...
Literature suggests that the Wandagee Formation conformably overlies the Quinnanie Shale (Mory & Backhouse, 1997). These two sections were
most likely deposited within a marine shelf, perhaps below the storm water wave base (notebook page 33). The Quinnanie, displaying no trace fossils
or bioturbation and generally massive in structure may suggest that it was deposited at greater depths than the Wandagee Formation or it may suggest a
cycle of shallowing and deepening waters, due to tidal influences. The Quinnanie representing deepened waters. Its more organic make–up may also
indicate that it was deposited at greater depths than the Wandagee. The Wandagee Formation contains a vast number of structures that indicate a
shallower environment than the Quinnanie. Whilst still being deposited below the storm water wave base, it may be possible that it was deposited
during a shallowing oscillation. Trace fossils that were burrowing indicate shallower waters, the stratigraphic log demonstrates these relationships,
figure 22).
5.7 Petroleum Potential
Quinnanie Shale is suggested to be a source rock, it has fair levels of organics, but has low generating potential, and is most likely more gas prone. The
Byro Group itself contains some source rocks. However, it is suggested that this system is immature (Ghori, 1998)
5.8 Discussion of the Williambury

The Best Exposure Of Rocks
The best exposure to of rocks can be seen in road cuts, because they the great variety in the rock types and formations within the area. Stray
fragments of rocks can be found in mass quantity alongside the river, held back from the road by barriers, or as a cut face that is parallel to the road.
You can clearly see the different intrusions along the roadside, dikes running along crevices, and many instances of solidrock blasted in order to clear
a way for the road. These mass capacities of the same rock are plutons that have been uplifted over geologic time1. Tonalitic plutons consisting of
primarily granodiorite and quartz are all over the Cascade Range, forming the Grotto/Index (~25m.y.) and Snoqualmie (~18m.y.) Batholiths of common
rock types. More recent Swauk sedimentary structures are seen as overlap from the nearby Blewitt (formerly Swauk) Pass region, likely formed as
result of the last ice age1,2,5. These sedimentary layers fade out deeper into the mountains, as the igneous intrusions become more predominant within
the range. White and black–grained diorite is common and clearly identifiable as well as amphibolite if looking around the Wenatchee or Skykomish
River where it has been broken, carried, and eroded to land on its banks (figure 5). Biotite schist, hornblende, and quartz intrusions are not uncommon,
seeing a new kind of whether solid or with distinct dike intrusions at each roadcut.5 Location specific granites have been mined as well as gold and
silver

The Indian Mounds Rock And Mineral Club At Rogers Plaza
1.Attend a Gem & Mineral Show such as the one sponsored by the Indian Mounds Rock and Mineral Club at Rogers Plaza on April 9–11. Hours are
9:30am–9pm Thursday and Friday, till 7pm on Sat. Plan at least 1 hour to browse through. Only bring what you can afford to spend (and think
Christmas gifts).
a.How did you apply knowledge you've learned in this geology class while you toured the show?
I used my knowledge from class when I was looking at all the different rocks and minerals. I knew the difference between the sedimentary,
metamorphic and the igneous rocks. The Gem Show was much more interesting because I knew what I was looking at. It gave the Show a whole new
meaning and a better understanding of how wonderful every rock and mineral really are.
b.Describe at least one new thing about minerals or rocks or fossils you learned from the show.
One of the new things I learned was that many of the rocks and minerals I was looking at come from either Mexico or Arizona. I learned from the
sells lady at the table I was looking at that Arizona is know as one of the richest rock and mineral zones in the world. I found that to be pretty cool.
The woman also said you will never see anything more beautiful then an Arizona skyline with all the rocks. I want to go visit Arizona now. в є
c.What was the most interesting exhibit/activity? Why was it interesting to you? (Please make this different than the answer to the previous question.)
The activity I love to do most is buying a

Classifying Rocks Essay
Classifying Rocks
Rocks are classified to make it easier on people to identify them in the future. This can be done by a numerous amount of ways. Each rock type has
their own specific ways, but there are two distinct characteristics that apply to all. These are texture and composition. These two, along with many
others helps to classify igneous, sedimentary, and metamorphic rocks.
Igneous rocks are classified first by texture. This is broken down mainly into grain size. First there are intrusive, or plutonic igneous rocks. These types
of rocks cool within the crust and forms large, visible crystals. The opposite would be extrusive, or volcanic rocks. These cool at the surface rapidly,
forming small grains. Acombination ... Show more content on Helpwriting.net ...
Depending on what the sedimentary rock is formed by, determines whether is known as clastic or chemical. Clastic rocks are composed of
particles from weathering. They are then sorted by grain size, gravel being the largest and clay being the smallest. A few examples would be
sandstones and shales. Chemical sedimentary rocks are biochemical, and contain ions in the solution from weathering. These are also further
classified. First you have limestone, which can be either organic or inorganic. An example would be fossiliferous or chalk. Next is dolostone, and
it is formed from dolomite. Chert is next; and can be organic or inorganic also. Flint and jasper are some examples of chert. Rock salt and gypsum
are what are known as evaporites. These form from the evaporation of saline waters in an arid environment. Finally there is coal, which is organic
and forms from buried plant remains and carbon. There is one more type of rock that is classified the same way as the previous two.
Metamorphic rocks are pre–existing rocks that are changed by heat and pressure. The pre–existing rock is called the parent rock, or protolith.
Metamorphism occurs in these rocks when the minerals become instable. There are two types of metamorphism, contact and regional. Contact is high
temperature, low pressure. It is basically a massive rock that is baked. Regional is high pressure and low temperature. Strong fabric, or layering,
develops from

A Report Of The Bezymianny Volcano During The Kamchatka...
Abstract
Zoning in plagioclase feldspar is often an indicator of magmatic differentiation. This is mainly due to the process of fractional crystallization changing
the chemistry of magmatic bodies, and has been documented in many localities. A case study will examine a 2010 report of the Bezymianny Volcano in
the Kamchatka peninsula of Russia, where researchers studied oscillatory zoning in the plagioclase. An interpretation of the results has shown frequent
replenishments to the magma chamber, and many magmatic differentiation processes including magma mixing, addition of volatiles, and reheating and
convection the melt body (Shcherbakov et al., 2010).
Introduction
Zoning occurs in plagioclase feldspars as they crystallize out of a melt, as composition of the magma changes. These changes occur due to the
formation of minerals consuming certain elements present in the magma (Gill, 2010). Plagioclase is an excellent indicator for this progressive
depletion of elements, as it forms a continuous series of anorthite (calcium rich, CaAl2Si2O8) to albite (sodium rich, NaAlSi3O8) (Nesse, 2011).
Because of the differences in composition, the feldspar chemistry can be used to interpret the magmatic processes which led to the production of these
feldspars. The zoning pattern reflects the chemical changes, which have occurred to the magma body and can show magmatic differentiation processes
such as magma mixing and changes in temperature, pressure and water content (Churikova

Host Rocks Essay
TYPE OF ROCK WHERE OPALS ARE FOUND
The New South Wales opal fields are all situated in arid inland areas, on ridges surrounded by black soil plains. Opal deposits mainly occur in
Cretaceous rocks formed 65 to 135 million years ago within the Great Australian Basin. Opal is found at shallow depths in sedimentary rocks through
which there has been considerable silica seepage into cavities and other structures where gradual loss of water from the silica gel has resulted in
hardening of the material and the formation of opal.
Host rocks contained a variety of voids formed by the weathering process, which leached carbonate from boulders, nodules, fossils, cracks, hollow
centres of ironstone nodules and horizontal seams. Most opaline silica deposited is common opal (or potch). It does ... Show more content on
Helpwriting.net ...
Geological mapping of the opal fields has shown that the sandstone is thickest in areas that have produced large amounts of opal. Opal is rarely
produced from areas in which the sandstone is thin or absent.
2.2 OPAL PROSPECTING METHODS1
"Geological, geophysical or geochemical exploration techniques to locate the mining site"
Opal mining at Lightning Ridge takes place within Opal Prospecting Areas (OPAs) which are within the four opal prospecting area (OPAs 1
–4)
designated within the Narran–Warrambool Reserve; established over the Lightning Ridge Mineral Claims District in 1993, covering approximately
5000 square kilometres of land surrounding the Lightning Ridge opal fields.
The reserve was designed to protect the heritage of the small miner by preventing the granting of large exploration licences and mining leases,
effectively limiting operations to small scale mining.
1

Analyse the Commodity Attractions of the Element Nickel Essay
Nickel
Introduction
The intension of the paper is to analyse the commodity attractions of the element nickel. It is highly related to physical and chemical properties of the
element because any commercial usage of this element is based on its property. Also, nickel is extracted from ore, so the ore deposit of it will be
highly related to the capital of any nickel related business. The laterite nickel ore deposit, Greenvale located in Queensland be focused on to reveal the
genesis and other attributes of this type of nickel deposit. Based on these information a conclusion of the current market status of nickel can be
portrayed.
Properties and Utility Nickel is a transition metal on the periodic table. It is solid under room temperature ... Show more content on Helpwriting.net ...
(Keim 1990). Nickel is widely used in industries.
Ore deposit condition Most of nickel is extracted from laterite nickel ores, which consist 60%–70% of nickel on earth. This kind of ore is formed by
the chemical weathering of serpentinite and other igneous rocks. Because of this requirement of weathering, deposits are located mostly in a humid
tropical environment (Figure 1). (Butt & Cluzel 2013) The major end–product of this weathering process will be: hematite, nickeliferous limonitic ore
((Fe,Ni)O(OH).nH2O) and nickeliferous silicate ore ((Ni,Mg)6Si4O10(OH)8). Nickeliferous limonitic ore and nickeliferous silicate ore are the two
dominant types of nickel ore. (Pickles 2003) uplifted oxide–rich regoliths form nickeliferous limonitic ore and nickel goes downward to saprolite and
combine with silicates to form nickeliferous silicate ore. The silicate ore deposits at a greater depth than the limonitic ore. Nickeliferous limonitic
ores are mostly weathered product of goethites. (Butt & Cluzel 2013) For both ores nickel content of each will be around 1.5%. Nickel in the silicate
ore will be more than 1.5%. (Pickles 2003) Since laterite nickel ores are from the weathering of pre–existing rock, the composition of surrounding
rocks, topography and climate are important factors. Usually laterite nickel ores will form on olivine–rich ultramafic rocks. These rocks are the basic
building blocks of nickel ores.

Glaucophane Quadrangles Research Paper
GENERAL ROCK TYPES
The oldest rocks exposed are arkosic sandstone and shale, and small amounts of thin–bedded chert and altered volcanic rocks, of the Upper Jurassic
Franciscan formation. Large masses of serpentine and smaller plugs and dikes of gabbro and diorite intrude these sediments; glaucophane schists and
their unusual mineralogical assemblages are developed locally. The series as exposed on the San Jose quadrangle consists chiefly of sandstone, shale,
and jasper; with occasional bed of heavy conglomerate. Scattered here and there throughout its area are small patches of greenstone, probably of
tuffaceous origin. In several localities it is associated with serpentine, eclogite, and diorite, each of which is supposedly intrusive into it. However,
large areas of practically unaltered sandstone and shale exist in what is known ... Show more content on Helpwriting.net ...
The picture on the left is an illustration of the above mentioned faults taken by USGS Science for a Better World. Relatively thick sequences of
sandstone that were probably deposited in deep marine environments and resemble the type Butano Sandstone of the Santa Cruz Mountains. These
Sandstones, however, overlie Franciscan rock and were probably deposited well over one hundred miles southeast of the type of Butano Sandstone they
belong to. They reached their present location by large amounts of right–lateral slip along the nearby San Andreas Fault. The sequence consists mostly
of interbedded arkosic sandstone, siltstone, and mudstone with locally abundant conglomerate lenses. A basal breccia and conglomerate that contains
fragments of Franciscan graywacke up to 15 ft long is present. Chaotically bedded zones are abundant throughout the rocks; they consist of large blocks
of sandstone set in a shredded mudstone matrix and are probably of both tectonic and synsedimentary

and several types of intrusive rocks. Mafic volcanic rocks constitute the bulk of the stratigraphy in the OB and occur as both pillowed basalts and
massive flows. They are aphanitic to fine–grained and dark green to black (Frey and Venzke 1991). Mafic volcaniclastic rocks are more common
lower in the stratigraphy. Intermediate volcanic rocks occur almost exclusively as tuffs, are feldspar–phyric and contain 20–30% mica and amphibole.
Felsic volcaniclastic rocks vary from rhyolites to dacites and occur mainly near the stratigraphic top of the volcanic pile where they directly underlie
massive... Show more content on Helpwriting.net ...
Dark brown to black tourmalinte laminae and beds contained 40% tourmaline, 40% pyrrhotite, and 20% quartz, and reach thicknesses up to 30 cm.
Iron formation beds are typically intermixed with iron silicates and sulfides, and are up to one meter thick. These individual beds of iron formation
occur as stacked lenses that span over 50 meters vertically through stratigraphy (Frey and Venzke 1991). Intrusive rocks in the OB vary from mm–scale
dikes and veins to meter–scale sills and dikes. They vary compositionally through ultramafic, pyroxenite, mafic, granodiorite, and granitic (Frey and
Venzke 1991). Ultramafic rocks are altered and difficult to constrain as intrusive or extrusive. Sparse pyroxenite dikes and veins are coarse grained
and sometimes biotite rich suggesting lamprophyre affinity. Gabbroic intrusives are the most common in the OB and occur as swarms of small
dikes with chill margins (Frey and Venzke 1991). They are a cut locally by felsic intrusive rocks. Granodiorite dikes are siliceous and porphyritic.
They locally occur as a series of small dikes but are more common as thick sills. These intrusive rocks may contain up to 60% xenolithic amphibole,
biotite, magnetite, tourmaline, and pyrrhotite. Granodiorite dikes intrude mafic rocks, and are in turn cut by granitic dikes. Granitic intrusive rocks
occur as small dikes composed of potassium feldspar and quartz. These small dikes cross–cut the intermediate and

Amu Scin138 Lab 9 Essay
Lab Lesson 9: Geologic Time (p.203) due end of week 3
Return to Assessment List
Part 1 of 1 – 100.0/ 100.0 Points
Question 1 of 31 3.0/ 3.0 Points
Questions 1 through 3 are based on the Lab Exercise, Step 2.
Record your answer to Lab Exercise, Step 2, Question 11. How long ago was the igneous rock in rock unit B formed?
A. 352 mya
B. 380 mya
C. 704 mya
D. 1408 mya
Answer Key: A
Record your answer to Lab Exercise, Step 2, Question 12. How long ago was the igneous rock in rock unit C formed?
A. 70.4 mya

B. 140.8 mya
C. 352 mya
D. 704 mya
Answer Key: B
Question 3 of ... Show more content on Helpwriting.net ...
Principle of Original Horizontality
C. Principle of Superposition
D. Principle of Vertical Continuity
Answer Key: D
Questions 4 through 8 are based on Figure 9.17 on page 208 of your lab book.
Determine the relative age each of the geologic structures shown in the geologic cross section below (Figure 9.17) from youngest to oldest; then
answer the questions below. As before, a wiggly line running across the geologic cross section indicates an unconformity and a fault is indicated with a
bold straight line.
Which is the youngest geologic structure in Figure 9.17?
A. E B. A C. B D. D
Answer Key: B
Which is the oldest geologic structure in Figure 9.17? A. A B. C C. F D. D
Answer Key: D

Which letter represents an unconformity in Figure 9.17? A. A B. C C. E D. F
Answer Key: C
Which letter represents a fault in Figure 9.17? A. A B. C C. E D. F
Answer Key: D
Feedback: F
What is the proper order of geologic structures B, C, D, and F in Figure 9.17 from oldest to youngest? A. F, B, C, D
B. D, C, B, F
C. D, F, B, C
D. B, C, F,

The Effect Of Magnetic Permeability On The Magnetic Field
Aeromagnetic Data
Theory
Scalar aeromagnetic data comprise both induced and remanent magnetic fields. Induced magnetism is caused by the earth's magnetic field and is
mainly the result of the magnetic susceptibility of the rock. Magnetic susceptibility is expressed as a unit–less proportionality constant denoted by an
International System of Units (SI), which reflects the susceptibility of a rock to become magnetized in the presence of a magnetic field. This
susceptibility is mainly a function of the rock's magnetite content. In general, higher susceptibility rocks produce greater variability in magnetic
amplitudes than low–susceptibility counterparts (Ford et al. 2008; Anderson et al. 2013; Table 2).The remanent component is a function of the
magnetic, mechanical, and thermal history of a rock and is not affected by the inducing magnetic field in which it is measured. In most cases, the
induced component of the magnetic field is predominant. However, remanent magnetization is commonly dominant in igneous rocks (Anderson et al.
2013) which can result in negative polarization and subsequent negative amplitude magnetic lows.
Structural Interpretation of Aeromagnetic Data
Aeromagnetic data indicate the OB is bound to the north by the Quetico fault and to the south by the Vermillion and Rainy Lake–Seine River faults
(Fig. 3, Fig. 4). The geometry of regional faults suggests the OB occurs in a pressure shadow of a large sigma–shaped wedge of volcanoplutonic rocks
and the

A Survey On The Creek Geological History

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