new survey of phobos’ grooves further evidence for groove origin
DESCRIPTION
John Murray. CEPSAR Centre for Earth, Planetary, Space & Astronomical Research. The Open University. New survey of Phobos’ grooves Further evidence for groove origin. New map of Phobos’ grooves from HRSC, HiRISE and Viking images. - PowerPoint PPT PresentationTRANSCRIPT
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New survey of Phobos’ grooves
Further evidence for groove origin
John MurrayJohn Murray
CEPSARCentre for Earth, Planetary, Space & Astronomical ResearchT
he
Op
en
Un
iver
sity
T
he
Op
en
Un
iver
sity
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New map of Phobos’ grooves from HRSC, HiRISE and Viking images.
-different from all other planetary and satellite lineaments
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Each groove traces a plane through Phobos
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Each groove traces a plane through Phobos
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Several “families”of parallel grooves
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Each family of grooves is of a different age
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For each groove family, the plane passing through the centre of Phobos also passes through its leading apex
Leadingapex
Leadingapex
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All grooves become parallel along the sub- & anti-Mars
meridianS
ub
-Mars m
eridian
Su
b-M
ars merid
ian
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1 2
3
1 2 3
Each groove family extends
over no more than one half of Phobos
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Zone of avoidanceat trailing apex ofPhobos
Zone of avoidanceat trailing apex ofPhobos No grooves
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All grooves are younger than
Stickney
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Groove families are obstructed by topography near the edge of their hemisphere
Groove families are obstructed by topography near the edge of their hemisphere
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Grooves are not radial to Stickney crater
Grooves are not radial to Stickney crater
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Grooves are crater chains with raised rims, with apparent deposition in places
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Proposed origins of parallel grooves
opened by Stickney impact
Fractures: caused by tidal forces
caused by drag forces during capture
tidal fractures re-opened by Stickney impact
from Stickney crater
Secondary impacts: from rolling boulders from Stickney
from impacts on Mars
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Directio
n of
impact
Stickney impact fractures? Analogue experimentsImpact at 4 km sec into aluminium sphereFrom Nakamura & Fujiwara (1991)
Map of polygonal fractures formed from above impact. No straight or parallel grooves seen
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Stickney re-opening of tidal fractures
1. Stickney impact: no sign of radial outward compression:
2. Radial outward movement of laboratory hypervelocity impact into sand:
(Oberbeck et al 1977)
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Stickney re-opening of tidal fractures
1. Stickney 10 km:
2. 12.6 km diameter Aorounga impact crater, Chad:
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Problems with all fracture hypotheses:No sign of lateral movement that would occur if grooves were fractures
Upper limit of c.20 metres horizontal fracture opening
Phobos GanymedePhobos Ganymede
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No sign of lateral movement that would occur if grooves were fractures
Upper limit of c.20 metres horizontal fracture opening
Phobos GanymedePhobos Ganymede
Problems with all fracture hypotheses:No sign of lateral movement that would occur if grooves were fractures
Upper limit of c.20 metres horizontal fracture opening
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Moon Hyginus rille Mars
Pit craters over fissuresPit craters over fissuresFracture models require a very thick regolith - 100-400 mFracture models require a very thick regolith - 100-400 m
200m
20m maximum width
En echelonfaulting
Always associated
with faulting
Always associated
with faulting
Faults not straight or planar
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If Phobos is a captured asteroid, then it has twice lost its regolith
1. During capture (Thomas, Veverka, Bloom & Duxbury 1979,
JGR)
2. During Stickney impact(Horstman & Melosh 1989, JGR)
If Phobos is a captured asteroid, then it has twice lost its regolith
1. During capture (Thomas, Veverka, Bloom & Duxbury 1979,
JGR)
2. During Stickney impact(Horstman & Melosh 1989, JGR)
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Grooves cannot be faults or fractures of any kind.
1. Propagation through voids2. Detached slices would be unsupported:
could not remain open for regolith drainage
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Mercury Phobos Moon PhobosMercury Phobos Moon Phobos
Secondary impact hypotheses
Secondary impact hypotheses
Grooves have raised rims, and appear similar to secondary impact cratersGrooves have raised rims, and appear similar to secondary impact craters
38 km 6 km 18 km 4 km
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Escape velocity: <11 m sec-1Secondary impact hypotheses
1. From Stickney Crater:
- Velocities too low to form craters
Secondary impact hypotheses
1. From Stickney Crater:
- Velocities too low to form craters
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Escape velocity: <11 m sec-1Secondary impact hypotheses2. Rolling ejecta:
- No boulders at end of grooves- Grooves do not run downhill- No repeated pattern- Boulders do not roll around obstacles
Secondary impact hypotheses2. Rolling ejecta:
- No boulders at end of grooves- Grooves do not run downhill- No repeated pattern- Boulders do not roll around obstacles
Moon
Phobos
Moon
Phobos
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Secondary impactchains from Mars craters
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Formation of ejecta strings
Formation of ejecta strings
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Tracing thegroove familiesback to Mars
2. ARRIVAL at PHOBOS. For each ejecta batch, the orientation and velocity of the ejecta strings impacting Phobos was calculated.
MOST EJECTA ARRIVES AT A VELOCITY OF 4km sec-1
1. LAUNCH from MARS. Several different launch latitudes were chosen, from which the ejecta was launched at an angle of 49o +3o, the mean launch angle of ejecta in 45o impacts, the most likely impact angle.
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family A (oldest)
family B
family C
family D
family E
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2ndry impactModel with 12 groove families included.
HRSC map of Phobos grooves
2ndry impactModel with 12 groove families included.
HRSC map of Phobos grooves
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STICKNEY EJECTA (after Thomas 1988) TIDAL STRESS (Dobrovolskis 1982)
STICKNEY ROLLING BOULDERS (Head & Wilson) SECONDARY IMPACTS FROM MARS (Murray 1994)
STICKNEY FRACTURING (Fujiwara & Asada 1983) MAP OF PHOBOS’ GROOVES
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THE ENDTHE END
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Tracing the grooves back to Mars craters:
Experimental laboratory impacts in vacuum
Similar results from recent numerical modelling
49oEarly
eje
cta
trave
lling
at ~
4 km
sec
-1
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Tracing thegroove familiesback to Mars1. The centre of the grooved hemisphere indicates the direction from whence the ejecta came, but not its velocity
2. By varying the velocity, we can find the latitude on Mars from which the ejecta was launched at an angle of 49o +3o, the mean launch angle of ejecta in 45o impacts, the most likely impact angle
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At what distance do we place Phobos?
Phobos was furtherfrom Mars in the past
At what distance do we place Phobos?
Phobos was furtherfrom Mars in the past
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We have to increase
Phobos’ orbit to 14,000 km to
get groove family A to
trace back to Mars
At 49° launch, it traces back to a
crater at +37° latitude (± a lot)
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Easy to detect craters older
than the grooves
Age of groove family A can be
determined from crater
counting
What age is family A ?
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The age of groove family A is 3.3 Gy
Pre-groove: 4.3 Gy Post-groove: 3.3 Gy
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There is only one Mars basin as young as3.3 Gy: the basin Lyot. It is at latitude +52o
Model at ejection angle 49° latitude = 37°
latitude = 52°
Lower ejection angles
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1. Phobos has been in synchronous orbit around Mars since at least 3.3 Gy.
2. Phobos mean secular acceleration during this time has been between 3 x 10-5 and 4.5 x 10-5 deg. year -1
3. Lyot is probably the source impact basin for groove family A
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What is Phobos’ regolith thickness?
Method of Quaide & Oberbeck 1968
What is Phobos’ regolith thickness?
Method of Quaide & Oberbeck 1968
Regolith
Solid rock
Normal Central mound
Flat-bottomed Concentric craters
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Mean regolith thickness = 20 metresExtremes are 8m to 42m
Mean regolith thickness = 20 metresExtremes are 8m to 42m
Concentric double craters on PhobosConcentric double craters on Phobos
0
1
2
3
4
5
0 10 20 30 40 50
Regolith Depth in metres
Phobos regolith depth from crater
geometry
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0
10
20
30
40
50
-90 -60 -30 0 30 60 90 120 150 180 210 240 270
Longitude
Phobos regolith
depthRe
go
lith
de
pth
in
me
tre
sLeading Trailingapex apex
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Will Mars rocks be found on Phobos?
At secondary impact speeds of 4 km sec-1 most will be ejected at >11 m s-1 :
Look for Mars rocks near a groove within a topographically-protected hollow
Will Mars rocks be found on Phobos?
At secondary impact speeds of 4 km sec-1 most will be ejected at >11 m s-1 :
Look for Mars rocks near a groove within a topographically-protected hollow