What’s in there? How do we know its there? Why do we even care?

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Presentation transcript:

What’s in there? How do we know its there? Why do we even care? Earth’s Interior What’s in there? How do we know its there? Why do we even care?

Studying the Earth’s Interior Seismic Wave Studies allow the scientists to compare different regions measure refraction measure reflection measure velocity changes measure absorption P-waves –move parallel to the direction of their propagation like sound waves S-waves – move perpendicular to the direction of their propagation

Zones of the Earth Crust outermost layer solid rock Moho thin interface crust/mantle rocks denser below Mantle mostly solid thickest zone 80% of volume

Mantle Pieces Lithosphere crust + rigid mantle sections - “plates” Athenosphere wave velocity  “plastic” partially molten melting point/temperature intersect Stiffer Mantle

Core Regions Outer Core liquid how waves refract in shadow zones how wave reflect off inner core Inner Core solid due to great pressure

Inner Core note pressure graph

Earth’s Crust Continental Crust (20-70 km) thickest by mountains less dense (2.7 g/cm3) granitic rocks Oceanic Crust (7-10 km) more dense (3.0 g/cm3) basaltic rocks

Earth’s Interior Mantle (1000-3000 km) less dense (3.3 – 5.5 g/cm3) Outer Core (3000-5000 km) more dense (9.9 – 12.1 g/cm3) iron Inner Core (5000 – 6000 km) most dense (12.7 – 13.0 g/cm3) iron and nickel