Video 2.6.1: What's inside the Earth?

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Our Earth: Its Climate, History, and Processes

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University of Manchester

Our Earth: Its Climate, History, and Processes

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Develop a greater appreciation for how the air, water, land, and life formed and have interacted over the last 4.5 billion years.

À partir de la leçon

Formation, evolution, and processes of the solid Earth

Video 2.1.1: How did the Moon form? - Dr. Katherine Joy 14:43

Video 2.1.2: Why is the Moon important to life on earth? - Dr. Katherine Joy 3:04

Video 2.2: What came before plate tectonics?5:43

Video 2.3: How did plate tectonics get discovered?6:12

Video 2.4.1: The Earth's magnetic field7:42

Video 2.4.2: The magnetic poles flip? You're kidding me, right?6:36

Video 2.5: How earthquakes happen14:23

Video 2.6.1: What's inside the Earth?6:05

Video 2.6.2: How do we know about the insides of the Earth?6:09

Video 2.7: How do the plates move?3:38

Video 2.8: How does magma form?11:17

Video 2.9: How were the Himalaya formed?7:56

Video 2.10: Supercontinent Pangaea9:50

Video 2.11: The supercontinent cycle4:05

Rencontrer les enseignants

Prof. David M. Schultz
Professor of Synoptic Meteorology
School of Earth, Atmospheric and Environmental Sciences
Dr Rochelle Taylor
Postdoctoral Research Associate
School of Earth, Atmospheric & Environmental Sciences
Dr Jonathan Fairman
Postdoctoral Research Associate
School of Earth, Atmospheric and Environmental Sciences

Hello and welcome to Our Earth, Its Climate, History, and Processes.

I'm David Shultz.

In this lecture, we want to talk about the interior of the Earth.

Why is it composed of these different layers, and what differences

in composition and characteristics do these different layers have.

During the formation of the solar system when the Earth was still molten,

the Earth went underwent a process called differentiation.

This is where the heavier elements sank to the center of the Earth.

We know that iron melts at a lower temperature than silicate minerals.

Silicate minerals are simply those minerals that are composed

mostly of silicon and oxygen.

At the time of this differentiation, both iron and

most of the silicates were melted on the earth.

So this allowed the heavier iron to sink to the bottom, and

the lighter silicates to rise to the top.

The sinking of the iron led to the release of gravitational energy, which produced

heat in the interior of the Earth, and of course the decay of radioactive elements

that were trapped inside the Earth also led to internal heating of the Earth.

Internal heating that goes on to this day.

So this is what happens say during the first 100 billion years or so

of earth's evolution, until we ended up with this layered Earth.

The layered Earth we are talking about has four layers.

It has the Earth's crust near the surface, the mantle,

the liquid outer core, and the solid inner core.

The crust is composed primarily of oxygen and silicon, but

also has aluminum, iron, magnesium, and many other elements.

The mantle has about the same concentration of oxygen, but

much higher magnesium concentration, little bit lower silicon concentration.

As you go to the outer core, the composition changes dramatically.

This outer core is now 85% iron, and

5% nickel, 5% oxygen, and 5% sulfur.

As you go into the inner most core, it's 94% iron and 6% nickel.

So you can see the increase in iron concentration,

nickel, as you get towards the center of the Earth, and also the reduction

in the amount of silicon and oxygen as you go into the center of the Earth.

So, let's talk about each of these different layers.

The Earth's crust is composed different plates, and there are two types of crust.

There's the oceanic crust which is primarily basalt, and

you have the continental crust which tends to be more granitic.

Currently, the crust is composed of these different plates, and

these plates move around on the earth due to the plate tectonics.

So we'll talk more about that in later lectures.

The mantle comprises 80% of the volume of the Earth.

It's mostly a rock called peridotite, which is mostly olivine and pyroxene,

and if we're lucky, we can see some pieces of the mantle that are occasionally

are brought to the surface of the Earth in what we call ophiolite sequences.

These are sections of ocean crust in upper mantle that have been uplifted

during plate tectonic processes, and exposed on the surface of the Earth.

As we go down towards the outer core, the outer core comprises one

sixth of the volume of the earth, but one third of its mass.

This is because of the much higher concentrations of iron.

As you get to the center of the Earth, the temperature is increasing, but

of course so is the pressure, and there is this zone,

where despite the increasing pressure, and the greater tendency to keep things solid,

the temperature is so high that the iron melts.

And that's exactly what happens here in the outer part of the core.

As you go to the inner core, despite the higher temperatures,

the pressure is so high, that the iron returns to a solid form.

So those those are the four layers of the Earth.

Because we live on the surface, we have a lot of experience with the crust,

both the continental crust and the ocean crust.

We have less direct experience with mantles.

I mentioned the only direct observations we have of the mantle

are the pieces of peridotite that we can find in ophiolite sequences.

We have no direct experience with what the inner and outer core look like.

So to summarize today's lecture, we saw that there were four layers of the Earth.

The crust, the mantle, the outer and inner core.

The crust has the highest percentage of silicon,

and the inner core has the highest percentage of iron.

Mantle occupies the largest volume of the Earth, but

it's mostly composed of a rock called peridotite.

Ophiolites are cross sections of the upper mantle and the crust, and these are key

elements in telling us what the structure of the upper part of the Earth looks like.

And then finally, the outer core is liquid, but

the inner core is solid, and both have a very high percentage of iron.

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