Slides related to wall rock alteration.In these slides it is described that how host rock behave when it comes in contact with the hydro thermal fluid coming from deep Earth (Mantle) and their results.
How can minerals deposits be formed; GEOLOGICAL PROCESSES; Ore Fluids; Ore Forming Processes; Concentrating Processes; Magmatic mineral deposits; Residual mineral deposits ; Placer deposits; Sedimentary mineral deposits; Metamorhogenic mineral deposits; Hydrothermal mineral deposits ; Magmatic Deposits
Cumulate deposits: fractional crystallization processes can concentrate metals (Cr, Fe, PGE, Pt, Ni, Ti, Diamond ))
Pegmatites : late staged crystallization forms pegmatites and many residual elements are concentrated (Li, Ce, Be, Sn, U, Rare Earths (REE), Feldspar, Mica, Gems).
magmatic deposits; Mode of Formation of Magmatic Ores Deposits; Mode of Formation of Orthomagmatic Ores ; Fractional Crystallization (or Crystal fractionation ); Magmatic (or Liquid ) Immiscibility; Simple crystallization without concentration (Dissemination); Segregation of early formed crystals; (Layer Types); Injection of material concentrated elsewhere by differentiation Residual liquid segregation; Residual liquid injection; Immiscible liquid segregation; Immiscible-liquid-injection; Early magmatic deposit; Late magmatic deposit; Types of Magmatic Ore Deposits:Chromite; Fe-Ti (± V) oxides; Ni – Cu – Fe (± Pt) sulfides; Platinum Group Elements (PGEs); REE, and Zr in Carbonatites; Diamond in kimberlites.
METEORITES VS ASTEROIDS VS METEORS VS COMETS METEORITE IMPACTS IN HISTORY
IMPORTANCE OF METEORITES
FORMATION OF ASTEROIDS AND METEOROIDS CLASSIFICATION OF METEORITES
Slides related to wall rock alteration.In these slides it is described that how host rock behave when it comes in contact with the hydro thermal fluid coming from deep Earth (Mantle) and their results.
How can minerals deposits be formed; GEOLOGICAL PROCESSES; Ore Fluids; Ore Forming Processes; Concentrating Processes; Magmatic mineral deposits; Residual mineral deposits ; Placer deposits; Sedimentary mineral deposits; Metamorhogenic mineral deposits; Hydrothermal mineral deposits ; Magmatic Deposits
Cumulate deposits: fractional crystallization processes can concentrate metals (Cr, Fe, PGE, Pt, Ni, Ti, Diamond ))
Pegmatites : late staged crystallization forms pegmatites and many residual elements are concentrated (Li, Ce, Be, Sn, U, Rare Earths (REE), Feldspar, Mica, Gems).
magmatic deposits; Mode of Formation of Magmatic Ores Deposits; Mode of Formation of Orthomagmatic Ores ; Fractional Crystallization (or Crystal fractionation ); Magmatic (or Liquid ) Immiscibility; Simple crystallization without concentration (Dissemination); Segregation of early formed crystals; (Layer Types); Injection of material concentrated elsewhere by differentiation Residual liquid segregation; Residual liquid injection; Immiscible liquid segregation; Immiscible-liquid-injection; Early magmatic deposit; Late magmatic deposit; Types of Magmatic Ore Deposits:Chromite; Fe-Ti (± V) oxides; Ni – Cu – Fe (± Pt) sulfides; Platinum Group Elements (PGEs); REE, and Zr in Carbonatites; Diamond in kimberlites.
METEORITES VS ASTEROIDS VS METEORS VS COMETS METEORITE IMPACTS IN HISTORY
IMPORTANCE OF METEORITES
FORMATION OF ASTEROIDS AND METEOROIDS CLASSIFICATION OF METEORITES
explanation of the seismology and study of the earth's interior besides the shadow zone and the Moho. the presentation include the gravity anomalies with the definition of the isostasy.
Page 22 2.1 IntroductIonStudying the Earth’s interior .docxalfred4lewis58146
Page | 22
2.1 IntroductIon
Studying the Earth’s interior poses a significant challenge due to the lack of
direct access. Many processes observed at the Earth’s surface are driven by the
heat generated within the Earth, however, making an understanding of the interior
essential. Volcanism, earthquakes, and many of the Earth’s surface features are a
result of processes happening within the Earth.
Much of what we know regarding the Earth’s interior is through indirect means,
such as using seismic data to determine Earth’s internal structure. Scientists dis-
covered in the early 1900’s that seismic waves generated by earthquakes could
be used to help distinguish the properties of the Earth’s internal layers. The veloc-
ity of these waves (called primary and secondary waves, or P and S waves) changes
based on the density of the materials they travel through. As a result, seismic waves
do not travel through the Earth in straight lines, but rather get reflected and re-
fracted, which indicates that the Earth is not homogeneous throughout.
The Earth’s interior consists of an inner and outer core, the mantle, and the
crust. Located in the center of the Earth is the inner core, which is very dense
and under incredible pressure, and is thought to be composed of an iron and nick-
el alloy. It is solid, and surrounded by a region of liquid iron and nickel called the
outer core. The outer core is thought to be responsible for the generation of the
Earth’s magnetic field. A very large portion of the Earth’s volume is in the man-
tle, which surrounds the core. This layer is less dense than the core, and consists
of a solid that can behave in a plastic (deformable) manner. The thin outer layer
of the Earth is the crust. The two types, continental and oceanic crust, vary from
each other in thickness, composition, and density.
2.1.1 Learning outcomes
After completing this chapter, you should be able to:
• Determine the different layers of the Earth and the distinguishing
properties of each layer
2earth’s InteriorRanda Harris and Bradley Deline
Page | 23
Introductory GeoloGy earth’s InterIor
• Understand how seismic waves behave within the different layers of the
Earth
• Understand how seismic tomography has been used to gain a better
understanding of the Earth’s interior
• Understand the Earth’s magnetic field and how it changes over time
• Learn how to use the program Google Earth for geological applications
2.1.2 Key terms
2.2 InterIor oF the eArth
The study of seismic waves and how they travel through the Earth has been
very useful in helping to determine the changes in density and composition within
the Earth and in locating the boundaries be-
tween the inner core, outer core, mantle, and
crust. Seismic waves are energy waves
generated during earthquakes; two types
known as P and S waves propagate through
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origin. P-waves are compressional waves
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The US House of Representatives is deeply concerned by ongoing and pervasive acts of antisemitic
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unwillingness to rectify this violation through action requires accountability.
Postsecondary education is a unique opportunity for students to learn and have their ideas and beliefs challenged. However, universities receiving hundreds of millions of federal funds annually have denied
students that opportunity and have been hijacked to become venues for the promotion of terrorism, antisemitic harassment and intimidation, unlawful encampments, and in some cases, assaults and riots.
The House of Representatives will not countenance the use of federal funds to indoctrinate students into hateful, antisemitic, anti-American supporters of terrorism. Investigations into campus antisemitism by the Committee on Education and the Workforce and the Committee on Ways and Means have been expanded into a Congress-wide probe across all relevant jurisdictions to address this national crisis. The undersigned Committees will conduct oversight into the use of federal funds at MIT and its learning environment under authorities granted to each Committee.
• The Committee on Education and the Workforce has been investigating your institution since December 7, 2023. The Committee has broad jurisdiction over postsecondary education, including its compliance with Title VI of the Civil Rights Act, campus safety concerns over disruptions to the learning environment, and the awarding of federal student aid under the Higher Education Act.
• The Committee on Oversight and Accountability is investigating the sources of funding and other support flowing to groups espousing pro-Hamas propaganda and engaged in antisemitic harassment and intimidation of students. The Committee on Oversight and Accountability is the principal oversight committee of the US House of Representatives and has broad authority to investigate “any matter” at “any time” under House Rule X.
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Internal Structure of Earth
1. Earth’s Interior
With Special Reference to Seismology
Mithun Ray
Department of Geography
Malda College
(University of Gour Banga)
E-mail: mithun.ray147@gmail.com
2. What do you imagine about the nature
of the earth?
a solid ball !!
or
a hollow ball !!
3. Diameter of the Earth
Equatorial= 12,756 km (7926 mile)
Polar=12,714 km (7900 mile)
Radius of the Earth
Equatorial= 6378.1 km (3,963.2 mile)
Polar= 6356.8 km (3949.9 mile)
Average Radius
6371km (3958.8)
4. How do we know
what’s inside the Earth?
Deepest Mine In
the world
Mponeng Gold Mine located at Johannesburg, South
Africa is the deepest mine in the world with an operating
depth of 4 km
6. Sources of Information about the Interior
Major Sources
The studies of the paths and characteristics of
earthquake waves travelling through the Earth, and
The laboratory experiments conducted on the surface
minerals and rocks at high pressure and temperature
Other Sources
The properties of surface rocks
Earth's motions in the Solar System,
Earth’s gravity and magnetic fields, and
The flow of heat from inside the Earth.
8. Seismic Waves /Earthquake waves
Waves
Body
Wave
‘P’ wave ‘S’ Wave
Surface
Wave
Love
wave
Rayleigh
Wave
9. ‘P’ / Primary/ Pressure/
Compressional / Longitudinal Wave
P waves travel faster than any other type of wave
They can travel through fluid or solid materials.
Material is compressed and stretched in the
horizontal direction and the wave (disturbance) also
travels in the horizontal direction.
Ordinary sound
waves in air are P
waves
Least destructive
10. ‘S’ / Secondary / Shear / Transverse Wave
‘S’ waves travel more slowly than ‘P’ waves
The material vibrates up and down i.e. perpendicular
to the direction of wave propagation
They can only travel through solid materials.
However, they may propagate in liquids with high
viscosity
11. A Rayleigh wave
is a seismic surface wave causing the ground
to shake in an elliptical motion, with no
transverse, or perpendicular, motion.
A Love wave
is a surface wave having a horizontal motion
that is transverse (or perpendicular) to the
direction the wave is traveling.
13. Reflection involves a change in direction
of waves when they bounce off a barrier.
Refraction of waves involves a change in the
direction of waves as they pass from one
medium to another.
14. Shadow Zone of
‘P’ wave
The shadow zone of P-
waves appears as a band
around the earth between
103° and 142° away from
the epicentre.
This is because P-waves
are refracted when they
pass through the transition
between the
semisolid mantle and the
liquid outer core.
However, the
seismographs located
beyond 142° from the
epicentre, record the
arrival of P-waves, but not
that of S-waves. This gives
clues about the solid inner
core.
15. S-waves do not travel
through liquids.
The entire zone beyond
103° does not receive S-
waves, and hence this
zone is identified as
the shadow zone of S-
waves.
This observation led to the
discovery of
the liquid outer core.
Shadow Zone of
‘S’ Wave
16. Shadow Zone of P-waves and S-waves
a zone
between 1
03° and
142° from
epicentre
was
identified
as
the shado
w zone for
both the
types of
waves.
19. CRUST
The Crust is the outermost layer of the earth on
which all living world exists
This is a very thin layer. It is also a brittle layer. It
is ranging from 5 km under the oceans to 100 km
under the mountainous areas of continents. Usually,
it’s about 40 km thick under the flat continents.
The crust is about 0.5 % of the earth’s total mass.
These rocks and minerals are made from just 8
elements. They are Oxygen (46.6%), Silicon (27.72%),
Aluminum (8.13%), Iron (5.00%), Calcium(3.63%),
Sodium (2.83%), Potassium (2.70%) and Magnesium
(2.09%).
20. Continental Crust (SIAL):
Composed of Silica (Si) and Aluminum (Al)
Average density is 2.7 gm/ cm3
This layer is mainly composed of Granite
Oceanic crust (SIMA):
Composed of Silica (Si) and Magnesium (Ma)
Average density is 3.0 gm/ cm3
This layer is mainly composed of Basalt
22. MANTLE
The mantle is the middle layer.
This makes up the largest volume of the Earth’s
interior. It is almost 2900 kilometers in thickness.
It is comprised of about 83% of the Earth’s total
volume.
It has an average density of 5.5 g/cm3
It is also divided into two distinct layers as upper
mantle and lower mantle.
23. Asthenosphere
The upper portion of the mantle is called
asthenosphere. The word astheno means weak.
It is considered to be extending upto 400 km.
It is the main source of magma that finds its way
to the surface during volcanic eruptions.
It is made up of peridotites.
24.
25. CORE
The core is found about 2,900 kilometers (1,802
miles) below Earth’s surface, and has a radius of about
3,485 kilometers (2,165 miles).
The core is made of two layers: the outer core,
which borders the mantle, and the inner core.
The outer core is in liquid state while the inner core
is in solid state.
The core is made up of very heavy material
mostly constituted by nickel and iron. It is
sometimes referred to as the NiFe layer.
29. Discontinuity
All layers of earth’s interior are
separated from each other through a
transition zone. These transition
zones are called discontinuities
30.
31. Conrad Discontinuity: Transition zone between
SIAL and SIMA.
Mohorovicic Discontinuity: Transition zone
between the Crust and Mantle.
Repiti Discontinuity: Transition zone between
Outer mantle and Inner mantle.
Gutenberg Discontinuity: Transition zone
between Mantle and Core.
Lehman Discontinuity: Transition zone between
Outer core and Inner core.
32. Conrad Discontinuity:
The transition zone between thee upper and lower part of the
lithosphere, is called as Conrad discontinuity. The name come
from the Austrian geophysicist Vector Conrad . Up to the
middle 20thcentury the upper crust in the continental region
was seen to consist of felsic rock such as granite and the lower
one consist of more magnesium rich mafic rocks such as
basalt. Therefore, the seismologists of that time considered
that Conrad discontinuity should correspond to a sharply
defined contact between the chemically distinct layers
of SIAL and SIMA. In passing through the Conrad
discontinuity the velocity of longitudinal seismic waves
increases abruptly from approximately 6to6.5km/sec.
33. Mohorovicic Discontinuity:
The transition zone between the crust and mantle is called as
mohorovicic discontinuity. The mohorovicic discontinuity
was discovered by Andrija Mohorovicic in the year of 1909.
The Moho lies at the depth of 35km beneath the continents
and 8km beneath the oceanic crust. The Moho separates both
the continental crust and the oceanic crust from underlying
mantle. The Moho lies almost entirely within the lithosphere,
only beneath the Mid Oceanic Ridge does it define lithosphere
and asthenosphere boundary. Immediate above the Moho
velocity of the P wave is 6km/sec and just below the Moho it
becomes 8km/sec. Moho is characterised by up to 500km
thick.
34. Gutenberg Discontinuity:
The mantle –core transition zone is called Gutenberg
discontinuity. In the year of 1912 Weichert Gutenberg
was discovered this discontinuity at the depth of 2900km
beneath the earth surface. In this zone the velocity of
seismic waves changes suddenly. The velocity of P wave
decreases and S wave completely disappear at this depth.
S wave shear material and cannot transmit through
liquid. So, it is believed that the part of above the
discontinuity is solid and part of beneath then
discontinuity is liquid or molten form. This molten
section is thought to be 700°c, hotter than the overlying
mantle. It is also denser, probably due to a greater
percentage of iron.
35. Repiti Discontinuity
it is the transition zone between Outer mantle and Inner
mantle.
Lehmann discontinuity
It is the transition zone between outer and inner core.
The Lehmann discontinuity is an abrupt increase of P-
wave and S-wave velocities at the depth of 220±30 km,
discovered by seismologist Inge Lehmann.It appears
beneath continents, but not usually beneath oceans, and does
not readily appear in globally averaged studies. Several
explanations have been proposed: a lower limit to the
pliable asthenosphere, a phase transition,[and most
plausibly, depth variation in the shear wave anisotropy.
36.
37. Seismic Waves and
the Interior of the Earth
Reflection causes P and S waves to rebound whereas
refraction makes waves move in different directions.
The variations in the direction of these waves are
inferred with the help of their record on seismograph.
Change in densities greatly varies the wave velocity. By
observing the changes in velocity, the density of the
earth as a whole can be estimated. By the observing the
changes in direction of the waves (emergence of shadow
zones), different layers can be identified.
38. For both kinds of waves, the speed at which the wave
travels also depends on the properties of the material
through which it is traveling.
Scientists are able to learn about Earth’s internal
structure by measuring the arrival of seismic waves at
stations around the world.
For example, we know that Earth’s outer core is
liquid because s-waves are not able to pass through it;
when an earthquake occurs there is a “shadow zone”
on the opposite side of the earth where no s-waves
arrive.
Similarly, we know that the earth has a solid inner
core because some p-waves are reflected off the
boundary between the inner core and the outer core.
39. By measuring the time it takes for seismic waves
to travel along many different paths through the
earth, we can figure out the velocity structure of the
earth.
Abrupt changes in velocity with depth correspond
to boundaries between different layers of the Earth
composed of different materials.
The structure of Earth’s deep interior cannot be
studied directly. But geologists use seismic
(earthquake) waves to determine the depths of layers
of molten and semi-molten material within Earth.
Geologists are now using these records to establish
the structure of Earth’s interior.
40. This Power Point Presentation (PPT) has been
prepared especially for Undergraduate Students. The
materials (Maps, Diagrams and Images) used in this
presentation were collected and compiled mainly
from variours academic blogs, research papers,
books etc. The author has designed this PPT
according to his convenience to deliver the lecture.