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Astronomy 340Fall 2005
29 September 2005
Class #8
90 minutes of homework (for 6th graders, but you can extrapolate to college…) 15 minutes looking for assignment 11 mins calling a friend for the assignment 23 mins explaining to parents why the teacher is
mean and just doesn’t like children 8 mins in the bathroom 10 mins getting a snack 7 mins checking the TV guide 6 mins telling parents that the teacher never
explained the homework 10 mins sitting at the kitchen table waiting for Mom
to do the assignment
Review
Surface composition of terrestrial planets dominated by silicates SiO2 (quartz), olivines, feldspars, etc.
Tectonics – important on the Earth Sea-floor spreading, subduction zones,
earthquakes, mountain chains, volcanic activity
Geochronology
Consider: at t=0, N=N0
t=τ, Nτ = N0 – Dτ , where Dτ is the number of“daughter” atoms after time, τ.
So, N0 – Dτ = N0exp(-λτ) τ = (1/λ)ln[1+(Dτ/Nτ)]
(Dτ/Nτ) can be easily measured.
This is great as long as D only arises from radioactivedecay of N.
Volcanic Activity
Key ingredient molten material Accretion (primordial heat)
Impact triggered Tidal heating/stretching Radioactive decay
Lunar Mare
Lunar mare – resurfacing via someImpact that releases magma.
Note low crater density.
Volcanic Activity
Key ingredient molten material Accretion (primordial heat)
Impact triggered Tidal heating/stretching Radioactive decay
ρ(magma)<ρ(rock) magma rises through “plumes” volcanoes sit atop plumes same physics on any planet/moon
Magma acts to resurface Volcanic composition
H2O, CO2, SO2 (recall that Io has SO2 or S2 gas)
Olympus Mons Viking 1
Venus’ Tectonic Activity?Smrekar & Stefan 1997 Science 277, 1289
Venus’ past Crater distribution is even & young no resurfacing over
past 300-500 Myr (Price & Supper 1994 Nature 372 756) No global ridge system and a lack of significant upwellings
(Solomon et al. Science 252 297) Why such a big difference compared with Earth?
Catastrophic loss of H2O from mantle? no convection “coronae” are unique to Venus
rising plumes of magma exert pressure on lithosphere less dense lithosphere deforms under pressure deformation of crust without tectonics
Coronae on Venus – from Magellan radar imaging
Martian Tectonic ActivityConnerney et al ’99 Science 284 794
Mars Global Surveyor Detected E-W linear magnetization in southern
highlands “quasi-parallel linear features with alternating
polarity”
Note: Earth’s global B-field is so much stronger it makes crustal sources hard to detect
Martian Tectonic ActivityConnerney et al ’99 Science 284 794
Mars Global Surveyor Detected E-W linear magnetization in southern highlands “quasi-parallel linear features with alternating polarity”
Note: Earth’s global B-field is so much stronger it makes crustal sources hard to detect
Mars has no global field so crustal field must be remnant (“frozen in time”) from crystallization
Martian Crustal Magnetization Working model
Collection of strips 200 km wide, 30 km deep Variation in polarization every few 100 km 3-5 reversals every 106 years (like seafloor
spreading on Earth) Some evidence for plate tectonics…but crust
is rigid Earth’s crust appears to be the only one that
participates in convection
Impacts and Cratering
Dominates surface properties of most rocky bodies
“Back of the envelope” calculation of the energy of an impact…
Formation of Impact Craters
Impactor unperturbed by atmosphere Impact velocity ~ escape velocity (11 km s-1)
tens of meters in diameter Impact velocity > speed of sound in rocks
impact forms a shock Pressures ~100 times stress levels of rock
impact vaporizes rocks Shock velocity ~10 km s-1 much faster
than local sound speed so shock imparts kinetic energy into vaporized rock
Contact/Compression
Projectile stops 1-2 diameters into surface kinetic energy goes into shock wave tremendous pressures P ~ (1/2)ρ0v2
Peak shock pressures ~1000 kbar; pressure of vaporization ~600 kbar
Shock loses energy Radial dilution (1/r2) Heating/deformation of surface layer Velocity drops to local sound speed – seismic wave transmitted
through surface Can get melting at impact point Shock wave reflected back through projectile and it also gets
vaporized Total time ~ few seconds
Excavation
Shock wave imparts kinetic energy into vaporized debris excavation of both projectile and impact zone (defined as radius at which shock velocty ~ sound speed (meters per second) Timescale is just a dynamical/crossing time (t = (D/g)1/2
Crater size? D goes as E1/3 empirically, it looks like ~ 10 time diameter of projectile (but see equation 5.26b).
Can get secondary craters from debris blown out by initial impact
Large impacts multiring basins (Mars, Mercury, Moon)
Craters35m 2m 4yr Small
Earthquake
1km 50m 1600yr Barringer Meteor Crater
7km 350m 51,000yr 9.6 mag earthquake
10km 500m 105 yr Sweden
200km 10km 150 Myr Largest craters/KT impactor
Crater Density
See Figure 5.31 in your book number of craters km-2 vs diameter
Saturation equilibrium – so many craters you just can’t tell…. Much of the lunar surface Almost all of Mercury Only Martian uplands Venus, Earth not even close note cut-off on Venus’
distribution Calibrate with lunar surface rocks 107 times more small craters (100m) as there are
large craters (500-1000 km)
Mercury South Pole
Lavinia Planum Impact Craters
Note ejecta surrounding crater
“It’s the size of Texas, Mr. President”
- from yet another bad movie Comets – small,rocky/icy things 10s of km Asteroids – small, rocky things a few to
10s of km the largest is the size of Texas (1000 km) 100-300 NEAs known
Close encounters…. Tunguska River in Siberia 30-50m meteroid
exploded above ground flattened huge swath of forest
You make the catastrophe…
Need high velocity max velocity ~ 70 km s-1 (combine Earth’s orbital velocity
plus solar system escape velocity) Earth-asteroid encounters 25 km s-1
Eart-comet encounters 60 km s-1
Make it big…. E ~ mv2 something 1000 km would wipe out the entire
western hemisphere, but let’s be realistic and go for ~10m (1021 J) or ~1 km (1023 J)
One impact imparts more energy in a few seconds than the Earth releases in a year via volcanism etc.