The enigmatic polar caps of Mars Brief summary of history of observations Theory of seasonal cap behavior Residual (permanent) polar caps and evidence for climate change 10 5 to 10 7 years 10 – 200 years Future space observations

Christian Huygens

Sir William Herschel Discovered Uranus Discovered IR radiation Deduced disc galaxy Recognized that polar caps were seasonal; used observations to measure Mars’ obliquity (1784)

G. Johnstone Stoney Suggested term “electron” for unit of charge in 1891 Applied kinetic theory of gasses to planetary atmospheres. Studied helium in earth’s atmosphere. Used this to suggest that Martian polar caps are CO 2.

Composition of Seasonal Cap Scientists (except Stoney) assumed that the caps were water ice snow This assumption was crucial to Percival Lowell’s canal theory, since he assumed the melting polar caps were the source of water. Kuiper used reflection spectra to identify water ice in cap. He also measured CO 2 in atmosphere.

Mariner 4 (1965) Radio occultations  Martian atmospheric pressure is ~ 600 pascals, over an order of magnitude less than most conservative previous estimates. Therefore, p ATM ~ p CO2.

Robert Leighton and Bruce Murray

Polar energy balance Absorbed insolation + net energy advected into region + conduction from subsurface + IR radiance from atmosphere + latent heat released by subliming CO 2 = energy radiated by surface L & M (Science, ’66) showed that CO 2 will condense and that seasonal polar caps are carbon dioxide

Viking Landers: Pressure

1980’s-1990’s Hiatus in space exploration of Mars Modeling of polar caps using the Viking pressure curves as the primary constraint One D models gave way to GCM models based on primitive atmospheric equations Curves can be fit to pressure and predicts mass of CO 2 condensed

CO 2 Condensed Mass During polar night the latent heat should be roughly equal to the radiation Unphysically low emissivities required to avoid having too much CO 2 condense leading to large amplitude pressure curve Is there an additional source of energy (in addition to CO 2 latent heat) in polar night?

Conduction from sub-surface The ability of the surface to store energy is determined by thermal inertia = √K T ρc P Thermal inertia of surface traditionally determined from diurnal temperature observations that sample ~ 1-10 cm. For that inertia, conduction is unimportant However, the seasonal penetration is much greater and samples ~ 10 cm – 1 m

Gamma Ray Spectrometer on Mars Odyssey

GRS determination of water

Thermal storage in surface GRS discovered that in the polar regions there is nearly pure water ice just beneath the surface This enhances the conduction storage term and reduces CO2 condensation to match pressure

Residual (permanent) Caps at both poles

Buffering Suppose that CO 2 remains at one of the poles all year. In equilibrium, the energy absorbed by the cap = Energy radiated by cap = σT(p) 4 Energy absorbed ~ sinα (obliquity) In pure CO 2, sublimation temperature is a function of pressure So if there is big enough block of CO 2 at poles, p will change with obliquity

Obliquity The obliquity of Mars changes greatly over relatively short time scales due to the effects of other planets. Pressure change would bring about different climate (Sagan & Malin, ’73)

One of main goals of polar orbiting Viking Orbiter 2 was to determine composition of the much larger residual north polar cap. VO2 measured water vapor concentration (MAWD) and surface temperature (IRTM) of 220 K during summer. Result: residual north polar cap water ice IRTM later showed that smaller residual south cap is CO 2 ice because its temper- ature remains at ~ 150 K all summer.

Polar Layered Terrain Viking discovered that ground underlying the caps is composed of many layers Possibly responds to variation of orbital parameters with T ~ 10 5 – 10 7 years Layers composed of various mixtures of dust and water ice

Mars Orbiter Camera on MGS Two wide angle (140˚ FOV) cameras make daily global map in red and blue wavelengths High resolution camera can resolve features as small as ½ meter at nadir; minus blue filter

Earth and Moon from Mars Mars Odyssey from MGS

Residual South Cap: MOC Color images of the residual south polar cap at LS=306º on (A) February 22, 2000, (B) January 9, 2002, and (C) November 28, 2003.

MGS – Viking – M9 RSPC

“Swiss cheese” terrain

One Mars Year Change

Changes since Mariner 9 (16 MY)

2001 Dust Storm

Mountains of Mitchel 1999/01

Effects of Atmospheric Dust on Sublimation

Flux redistribution by dust Visible flux at surface CO 2 frost decreases with increasing dust optical depth However, infrared flux increases with increasing optical depth because of emission by hot dust

Albedo / Emissivity of CO 2

Effect of dust on sublimation Region with 0% dust sublimes more rapidly with increasing optical depth Region with large dust content and low visible albedo sublimes more slowly Effect on sublimation small for typical areas in the seasonal cap

RSPC Albedo Measurements from HST HRC at 2003 opposition Dashed lines are albedos assuming τ = 0; solid lines τ = 0.2 Albedos sufficient to stabilize residual cap Dust will increase sublimation rate

Conclusions The RSPC is a unique feature totally unlike other portions of the polar caps The RSPC is dynamic on time scales of years. Stratigraphy suggests short deposition periods separated by longer periods of erosion The timeline, together with Mariner 9 B images, suggest that the last period of deposition was somewhere around 1970 Late season dust storms could effect removal of RSPC units May also be connected with H 2 O ice distribution

Mars Reconnaissance Orbiter HIRISE: hi res with some color MARCI 180˚ FOV 5 vis + 2 uv bands CTX: 5 meters / pixel CRISM: imaging spectrometer.4 - 4μm MCS: atm profiles SHARAD: 15 meter depth resolution

Polar Observations 3pm orbit (compare 2 pm for MGS 5 pm Odyssey) Periapsis over south pole at 255 KM Apoapsis over north pole at 320 Km After one (earth year) < 5 km between ground tracks at equator 12 orbits cross the poles every day

MARCI Polar Science Acquire albedo maps of the poles in five bands and two UV channels Study behavior of dust storms and condensate clouds associated with the frost boundaries of both poles Search for interannual variability of and within seasonal caps Diurnal behaviors of storms and clouds Study frost phase functions at various wavelengths

Polar Observations CTX is ideal for monitoring temporal changes in “Swiss cheese” features in RSPC, spiders, dark spots, etc. in the South Polar Region Similarly, CTX should be useful for monitoring albedo features and specific areas in the north polar region. CTX should reveal details of polar dust storm and cloud structures