EART 160 Planetary Sciences Francis Nimmo Last Week

EART 160 Planetary Sciences Francis Nimmo

Last Week – Solar System Formation • Solar system formation involved collapse of a large gas cloud, triggered by a supernova (which also generated many of the elements) • Solar system originally consisted of gas: ice: rock in ratio 100: 1: 0. 1 (solar photosphere; primitive meteorites) • Initial nebula was dense and hot near the sun, thinner, colder further out • Inner planets are mainly rock; outer planets (beyond the snow line) also include ice and (if massive enough) gas • Planets grow by collisions; Mars-sized bodies formed within ~1 Myr of solar system formation • Late-stage accretion is slow and involved large impacts

This & Next Week – Surfaces • What are solid planet surfaces made of? • What processes modify the surfaces? – Impact craters – Volcanism – Tectonics – Erosion & Sedimentation

Surface Compositions • How can we tell? – Samples (Earth, Moon, Mars, Vesta? ) – In situ measurements by spacecraft (Venus, Mars, Moon, Titan) – Remote sensing (elsewhere)

Samples • Very useful, because we can analyze them in the lab and we (usually) know where they came from • Generally restricted to near-surface • For the Earth, we have samples of both crust and (uniquely) the mantle (peridotite xenoliths) • We have 382 kg of lunar rocks ($29, 000 per pound) from 6 sites (7 counting 0. 13 kg returned by Soviet missions) • Eucrite meteorites are thought to come from asteroid 4 Vesta (they have similar spectral reflectances) • We also have meteorites which came from Mars – how do we know this?

SNC meteorites • Shergotty, Nakhla, Chassigny (plus others) • What are they? – Mafic rocks, often cumulates 2. 3 mm • How do we know they’re from Mars? – Timing – most are 1. 3 Gyr old – Trapped gases are identical in composition to atmosphere measured by Viking. QED. Mc. Sween, Meteoritics, 1994

In Situ Measurements Venusian surface (Venera 14) • In situ measurements give us information without needing samples returned (difficult) • Problem is that only limited data can be returned • Still useful e. g. we know that the surface of Venus is basaltic, and that the surface of Titan has the texture of crème brulee • The Viking spacecraft even carried life detection experiments, but the results were negative or ambiguous

In Situ Measurements (Mars) APXS • Pathfinder (1997) measured rock and soil compositions using an Alpha Proton X-Ray Spectrometer (APXS) • This works by irradiating a sample with Alpha particles and detecting the particles/radiation given off • One problem was the “desert varnish” coating the rocks • The Mars Exploration Rovers (2004 - ) carried a “rock abrasion tool” to scrape off the varnish before carrying out their measurements • The results suggested ancient water had percolated through the sediments and produced concretions nicknamed “blueberries” RAT blueberries

Remote Sensing • Restricted to surface (mm-mm). Various kinds: – Spectral (usually infra-red) reflectance/absorption – gives constraints on likely mineralogies e. g. Mercury, Europa – Neutron – good for sensing subsurface ice (Mars, Moon) – Most useful is gammaray – gives elemental abundances (especially of naturally radioactive elements K, U, Th) – Energies of individual gamma-rays are characteristic of particular elements

Physical Properties • In the absence of other processes, ancient crusts will have been broken up by impacts at all scales • Lunar surface consists of fine-grained dust (produced by impacts) overlying brecciated, unconsolidated material (regolith) • Whether a surface is dusty or consists of solid rock can be inferred from its thermal inertia (rocks have a higher T. I. )

Summary: Planetary Crusts • Surfaces are expected to be broken up by impacts (regolith) • Remote sensing (IR, gamma-ray) allows inference of surface (crustal) mineralogies & compositions: – – Earth: basaltic (oceans) / andesitic (continents) Moon: basaltic (lowlands) / anorthositic (highlands) Mars: basaltic (plus andesitic? ) Venus: basaltic • In all cases, these crusts are distinct from likely bulk mantle compositions – indicative of melting • The basaltic compositions are all very similar, suggesting planetary mantles have similar compositions • The crusts are also very poor in iron relative to bulk nebular composition – where has all the iron gone?

Impact Cratering • Important topic, for several reasons – Ubiquitous – impacts occur everywhere – Dating – degree of cratering provides information on how old a surface is – Style of impact crater provides clues to the nature of the subsurface and atmosphere – Impacts produce planetary regolith – Impacts can have catastrophic effects on planets (not to mention their inhabitants) • What we will cover – What are the physical effects of impacts? – What can we infer about a planet from its cratering record?

Why do impacts happen? • Debris is left over from solar system formation (asteroids, comets, Kuiper Belt objects etc. ) • Object perturbed by something (e. g. Jupiter) into an orbit which crosses a planetary body • As it gets closer, the object is accelerated towards the planet because of the planet’s gravitational attraction • The minimum impact speed is the planet’s escape velocity, typically many km/s “The next big event for astronomers will be Friday April 13 th 2029. Scientists predict that the asteroid Apophis (~400 m diameter) will be coming only 32, 000 kilometres from the Earth, which is close enough to hit a weather satellite and even be visible without a telescope. ”

Gravity • Newton’s inverse square law for gravitation: r m 2 F F m 1 Here F is the force acting in a straight line joining masses m 1 and m 2 separated by a distance r; G is a constant (6. 67 x 10 -11 m 3 kg-1 s-2) • Hence we can obtain the acceleration g at the surface of a planet: • We can also obtain the gravitational potential U at the surface (i. e. the work done to get a unit mass from infinity to that point): a What does the negative sign mean? R M

Escape velocity and impact energy • Gravitational potential M R r • How much kinetic energy do we have to add to an object to move it from the surface of the planet to infinity? • The velocity required is the escape velocity: a • Equally, an object starting from rest at infinity will impact the planet at this escape velocity • Earth vesc=11 km/s. How big an asteroid would cause an explosion equal to that at Hiroshima?

Crater Basics Ejecta blanket Depth • Typical depth: diameter ratio is ~1: 5 for simple (bowl-shaped) craters Mars, MOC image

Crater Formation 1. Contact/compression 2. Excavation 3. Modification Note overturned strata at surface • Impactor is (mostly) destroyed on impact • Initial impact velocity is (usually) greater than sound speed, creating shock waves • Shock waves propagate outwards and downwards • Heating and melting occur • Shock waves lead to excavation of material • Transient crater is spherical • Crater later relaxes

Timescales v • Contact and compression • Time for shock-wave to pass across impactor • Typically less than 1 s 2 r d • Excavation • Free-fall time for ejected material • Up to a few minutes • Modification • Initial faulting and slumping probably happens over a few hours • Long-term shallowing and relaxation can take place over millions of years

Crater Sizes • A good rule of thumb is that an impactor will create a crater roughly 10 times the size (depends on velocity) • We can come up with a rough argument based on energy for how big the transient crater should be: Does this make sense? v 2 r 2 R a • E. g. on Earth an impactor of 0. 1 (1) km radius and velocity of 10 km/s will make a crater of radius 2 (12) km • For really small craters, the strength of the material which is being impacted becomes important

Craters of different shapes • Crater shapes change as size increases: – Small – simple craters (bowl-shaped) – Medium – complex craters (central peak) – Large – impact basins • Transition size varies with surface gravity and material properties SIMPLE: Moltke, Moon, 7 km COMPLEX: Euler, 28 km, 2. 5 km deep BASIN: Hellas, Mars

Shape transitions Schenk (2002) Europa, scale bar=10 km Note change in morphology as size increase Lunar curve Ganymede complex simple basins • Depth/diameter ratio decreases as craters get larger • Gravity on icy satellites similar to that on the Moon • Transition occurs at smaller diameters than for Moon – due to weaker target material? (ice vs. rock)

Unusual craters • • 1) Crater chains (catenae) 2) Splotches 3) Rampart Craters (Mars) 4) Oblique impacts • Crater chains occur when a weak impactor (comet? ) gets pulled apart by tides Crater chain, Callisto, 340 km long Comet Shoemaker-Levy, ripped apart by Jupiter’s tidal forces

Rampart Craters (Mars) • Probably caused by melting of subsurface ice leading to slurry ejecta • Useful for mapping subsurface ice Tooting crater (28 km diameter) Tooting crater, 28 km diameter Stewart et al. , Shock Compression Condens. Matt. 2004

“Airbursts” • Venus “dark splotches” • Tunguska, Siberia 1908 • Result of (weak) impactor disintegrating in atmosphere 300 km across, radar image • Thick atmosphere of Venus means a lack of craters smaller than about 3 km (they break up in atmosphere)

Oblique Impacts impact Mars, D=12 km Herrick, Mars crater consortium • Impacts are most like explosions – spherical shock wave leads to circular craters • Not understood prior to the space age – argument against impact craters on the Moon • Only very oblique (>75 o? ) impacts cause non-circular craters • Non-circular craters are rare

Atmospheric Effects • Small impactors burn up in the atmosphere • Venus, Earth, Titan lack small impact craters • Venus’ thick atmosphere may produce other effects (e. g. outflows) After Mc. Kinnon et al. 1997 Radar image of impact-related outflow feature

How often do they happen? (Earth) Hartmann

How do we date surfaces (1)? young old Sa tu ra tio n Slope depends on impactor population Effect of secondary craters? • Crater densities – a more heavily cratered surface is older • The size-distribution of craters Increasing age can tell us about the processes removing them • Densities reach a maximum • Lunar crater densities can be when each new crater destroys compared with measured one old crater (saturation). surface ages from samples Phobos’ surface is close to returned by Apollo missions saturated.

How do we date surfaces (2)? • It is easy to determine the relative ages of different surfaces (young vs. old) • Determing the absolute ages means we need to know the cratering rate (impacts per year) Number of craters >1 km diameter per km 2 • We know the cratering rates on the Earth and the Moon, but we have to put in a correction (fudge factor) to convert it to other places • So the uncertainties tend to be large, especially for “intermediate-age” surfaces

New craters on Mars • Important because we can use these observations to calibrate our age-crater density curves • Existing curves look about right Before After Malin et al. Science 2006 Probably mis-identified

Evolving impactor population • One complication is that the population of impactors has changed over time • Early solar system had lots of debris => high rate of impacts • More recent impact flux has been lower, and size distribution of impactors may also have been different • Did the impact flux decrease steadily, or was there an “impact spike” at ~4 Gyr Hartmann; W are numerical simulation results, boxes are data from Moon/Earth (Late Heavy Bombardment)?

Crater Counts frequency • Crater size-frequency plots can be used to infer saturation geological history of surfaces • Example on left shows that intermediate-size craters show lower density than large craters (why? ) size • Smallest craters are virtually absent (why? ) • Most geological processes (e. g. erosion, sedimentation) will remove smaller craters more rapidly than larger craters • So surfaces tend to look younger at small scales rather than at large scales

Complications • Rate of impacts was certainly not constant, maybe not even monotonic (Late Heavy Bombardment? ) • Secondary craters can seriously complicate the cratering record • Some surfaces may be buried and then exhumed, giving misleading dates (Mars) • Subsurface impact basins (Mars) • Very large uncertainties in absolute ages, especially in outer Pwyll crater, Europa (25 km diameter) solar system

Cratering record on different bodies • Earth – few craters (why? ) • Titan – only 2 craters identified so far (why? ) • Mercury, Phobos, Callisto – heavily cratered everywhere (close to saturation) • Moon – saturated highlands, heavily cratered maria • Mars – heavily cratered highlands, lightly cratered lowlands (plus buried basins) and volcanoes • Venus – uniform crater distribution, ~0. 5 Gyr surface age, no small craters (why? ) • Ganymede – saturated dark terrain, cratered light terrain • Europa – lightly cratered (~0. 05 Gyr) • Io – no craters at all (why? )

Where do impactors come from? • In inner solar system, mostly asteroids, roughly 10% comets (higher velocity, ~50 km/s vs. ~15 km/s) • Comets may have been important for delivering volatiles & atmosphere to inner solar system • In outer solar system, impactors exclusively comets • Different reservoirs have different freq. distributions • Comet reservoirs are Oort Cloud and Kuiper Belt • Orbits are perturbed by interaction with planets (usually Jupiter) • There may have been an “impact spike” in the inner solar system when the giant planets rearranged themselves (not quite as unlikely as it sounds)

Summary • Planetary crustal compositions may be determined by in situ measurements or remote sensing (spectroscopy) • Most planetary crusts are basaltic • Impact velocity will be (at least) escape velocity • Impacts are energetic and make craters • Crater size depends on impactor size, impact velocity, surface gravity • Crater morphology changes with increasing size • Crater size-frequency distribution can be used to date planetary surfaces • Atmospheres and geological processes can affect sizefrequency distributions

Key concepts • • • Spectroscopy (IR, gamma-ray) Regolith SNC meteorite Gravitational potential Escape velocity Simple vs. complex crater vs. impact basin Depth: diameter ratio Saturation Size-frequency distribution

halo Ejecta Wind vi vi 45 o Wind vw d

frequency A B saturation size