Download - ASTRONOMY Introduction to Solar System
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ASTRONOMY Introduction to Solar System
The Earth!!!
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Earth
Early Archean
Plate Tectonics
Blue Planet
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Earth Intro• http://www.youtube.com/watch?
v=Uhy1fucSRQI• 3rd Rock From Sun• Only one we KNOW has semi-intelligent life• One of 4 Terrestrial (rocky) planets
– Inner Planets (M, V, E, M)
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Light and Atoms
Shape? Not perfect sphere; Oblong Spheroid.(A) Rotation makes the Earth's equator bulge.
(B) (B) Jupiter's rapid rotation creates an equatorial bulge visible in this photograph. (Courtesy NASA.)
Back
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• Distance from Sun: 150 million kilometers (93.2 million miles)
• Orbital period: 365.256 days • Rotational period: 23.9345 hours• Tilt of axis: 23.45 degrees • Diameter: 12,756 kilometers (7,973 miles)• Mean density: 5.515 g/cc• Mean surface temperature: 15°C• Atmosphere composition: 77% N, 21% O and 2%
other.• Crustal rocks• Magnetic field• Plate tectonics-Lithosphere -Hydrosphere -Atmosphere-Biosphere
Earth Outline/Facts
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Earth Outline/Facts
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Age of the EarthEstimated age for the Earth and the rest of the solar system is about 4.55 billion years comes from Lead isotope measurements.
The oldest Earth rocks: 3.8 to 3.9 billion years
Oldest Earth minerals (zircons): 4.2 billion years
Oldest Moon rocks: 4.44 billion years
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• About 5.5-6 Billion Years Ago (BYA), the solar nebula begins to collapse
• About 4.6 BYA, Sun begins fusion • About 4.5-4.56 BYA, Proto-Earth formed from
planetesimals.• 4.44+ BYA, Earth-Moon formed by giant impact.
Earth melts, magma ocean.• 4.2 BYA, Earth was completely differentiated
(settled). • 4 BYA, earliest oceans formed, thick atmosphere
exists • 3.8 BYA, life develops • 2.5-3 BYA, photosynthesis leads to O2 in ocean • 2 BYA, O2 hits atmosphere
Early Earth Timeline
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How do we know the age?
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Giant Impact Formation of Earth-Moon System
http://www.youtube.com/watch?v=m8P5ujNwEwM
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Lunar Magma Ocean
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Early Earth’s Magma Ocean
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1000 km ?
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Fig. 15-3, p. 337
Spreading center Ocean
trench
Plate movement
Subduction zoneOceanic crust
Continental crust
Continental crust
Material cools as it reaches the outer mantle
Cold dense material falls back
through mantle
Hot material
rising through
the mantle
Mantle convection
cell
Two plates move towards each other. One is
subducted back into the mantle on a falling convection current.
Mantle
Hot outer coreInner
core
Plate movement
Collision between two continents
Tecto
nic
plat
e
Oceanic tectonic plate Oceanic tectonic plate
Oceanic crust
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Fig. 5.18The earth’s magnetic field does not point exactly north
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Fig. 5.19Charged particles from the sun (electrons and protons)
Will spiral around the magnetic field lines
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Fig. 5.20As the charged particles hit the atmosphere (close to the poles)
They emit light: the Aurora
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Fig. 5.20a
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Real time-http://
www.youtube.com/watch?v=Ezobpz55EEY
Timelaps-http://
www.youtube.com/watch?v=FcfWsj9OnsI
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Earth
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Recent Volcanism
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Fig. 15-4, p. 338
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Earthquakes produce two types of seismic waves:P waves [Primary, Pressure]: Sound waves travel
through solids and liquids.S waves [Secondary, Shear]: Transverse (side-to-
side) waves that do NOT travel through liquids.
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TWO TYPES OF SEISMIC WAVES P OR COMPRESSIONAL WAVES - VOLUME CHANGES
MATERIAL COMPRESSED OR EXPANDED IN DIRECTION WAVE PROPAGATES
S OR SHEAR WAVES - DISTORTION WITHOUT VOLUME CHANGES - MATERIAL SHEARED IN DIRECTION NORMAL TO WAVE PROPAGATES
P WAVES TRAVEL FASTER (ABOUT 1.7X) THAN S WAVES
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Seismic waves radiating through the Earth after an earthquake:
Note: S waves do not travel through the outer core!
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Convection currents in the asthenosphere have broken the lithosphere into sections called plates.
There are 15 large plates.
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Continuing convection in the asthenosphere causes plates to move relative to each other.
The study of plate motion is called plate tectonics.
The motion of continents was first suspected by Sir Francis Bacon (17th cent). Best known for leading the scientific revolution with his new 'observation and experimentation' theory.
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200 million years ago, the Americas, Europe, and Africa formed a single supercontinent, PANGAEA.
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The Earth 37
ONLINE Animations…
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The Earth 38
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The boundaries between plates are geologically active, with many volcanoes and earthquakes.
Example: the Ring of Fire around the Pacific Ocean.
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The summit of Mount Everest is made of marine limestone.
It has been lifted 9 kilometers high!
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Grand Tetons:
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Grand Tetons:
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The San Andreas transverse fault:
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Earth’s AtmosphereThe gaseous area surrounding the planet is divided into several concentric spherical strata separated by narrow transition zones.
The upper boundary at which gases disperse into space lies at an altitude of approximately 1000 km above sea level.
More than 99% of the total atmospheric mass is concentrated in the first 40 km from Earth's surface. Atmospheric layers are characterized by differences in chemical composition that produce variations in temperature
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Studies of the chemical abundance in the solar system points to the fact that our atmosphere is not a primordial atmosphere but rather a secondary atmosphere.
When the Earth (and other planets) formed, it must have been surrounded by a primordial atmosphere (mainly H2, He).
The primordial atmospheres of the inner planets were probably wiped out completely during the stage when the sun evolved to the stage of a T-Tauri star.
This was probably caused by the sun ejecting substantial mass from its surface in form of violent solar winds. These winds were effective in eroding the primordial atmospheres of the terrestrial planets.
This atmosphere erosion may have been enhanced by the lack of a strong magnetic in the early Earth.
Also, Earth’s gravity (compared to Jovian planets) is not strong enough to prevent escape of H2 & He.
Primordial Atmosphere
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Secondary Atmosphere
Gases produced were probably similar to those created by modern volcanoes (H2O, CO2, SO2, CO, S2, Cl2, N2, H2) and NH3 (ammonia) and CH4 (methane).
No free O2 at this time (not found in volcanic gases). Ocean Formation - As the Earth cooled, H2O produced by out gassing could exist as liquid in the Early Archean, allowing oceans to form.
Evidence - pillow basalts, deep marine seds in greenstone belts.
Produced by volcanic out-gassing
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Oxygen Production Photochemical dissociation
Breakup of water molecules by ultraviolet radiation Produced O2 levels approx. 1-2% current levels At these levels O3 (Ozone) can form to shield Earth surface from UV
Photosynthesis
CO2 + H2O + sunlight = organic compounds + O2 – first produced by Archean cyanobacteria, and eventually higher plants - supplied the rest of O2 to atmosphere.
Addition of O2 to Atmosphere
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CO2 is removed from the atmosphere during silicate weathering and buried as limestone (CaCO3) where it is
sequested for a long time (millions of years) until subduction and metamorphism release it.
Silicate Weathering – Carbonate Precipitation
CO2 + CaSiO3 CaCO3 + SiO2Carbon dioxide Silicate minerals Limestone Chert
Removal of CO2 from Atmosphere
(In the presence of water)
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PhotosynthesisCO2 + H2O CH2O + O2
Phytoplankton – oceans
Plants – land
Burial of organic matter reduces the level of CO2
in the atmosphere
Carbon dioxide Water vapor Organic matter Oxygen
Removal of CO2 from Atmosphere
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Removal of CO2 from Atmosphere
Once the water vapor in the atmosphere condensed to form an ocean, it became a “sink” for dissolved CO2.
Biochemical production of limestone by sedimentation of skeletal foraminifera from sea water further sequesters
CO2 in the solid Earth.
There is 60 times more CO2 dissolved in sea water than in the atmosphere, and 3000 times more CO2 buried in
sedimentary rocks than in the oceans.
Nitrogen build up in the early atmosphere was enhanced because of its low solubility in sea water.
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VENUS EARTH MARS
SURFACE PRESSURE 100,000 mb 1,000 mb 6 mb
COMPOSITION
CO2 >98% 0.03% 96%
N2 1% 78% 2.5%
Ar 1% 1% 1.5%
O2 0.0% 21% 2.5%
H2O 0.0% 0.1% 0-0.1%
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Fig. 5.16
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Fig. 5.16a
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Fig. 5.16b
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Fig. 5.16c