Remarks on the Iapetus’ bulge and ridge
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Iapetus is a medium sized icy satellite of Saturn. It has two spectacular features: the equatorial ridge (ER) and the abnormally large flattening. The flattening is usually explained in terms of large non-hydrostatic fossil equatorial bulge (EB) supported by a thick lithosphere. Here we show, building on the principle of isostasy, that EB and ER could be a result of low density roots underlying the lithosphere below the equator. The low density matter formed the layer over the core of the satellite. Such situation was unstable. The instability led to origin of axially symmetric plumes that formed equatorial bulge and equatorial ridge. So, we explain both: EB and ER in the frame of one hypothesis.
Key wordsIapetus satellite shape satellites surface tectonics
The interiors of MIS behave like viscous liquid in geological time scale, therefore the gravity and the centrifugal force give them a hydrostatic shape, i.e. an oblate ellipsoid (approximately a sphere with an equatorial bulge— EB) with flattening depending on period of rotation T r (flattening decreases if T r increases). Iapetu’ flattening is equal to 0.046 and it corresponds T r = 16 hours although the present T r is 79.33 days. The initial T r was probably a few hours but tidal forces slowed the rotation down establishing synchronous rotation, i.e. T r = Torbital. The time of despin-ning tdesp is proportional to a−6 (a is the distance from Saturn) and depends also on the dissipation factor Q. Q is high for rigid and elastic bodies and low for viscous, e.g. partially melted ones. Assuming typical Q = 100 one obtains tdesp ≈ 240 Gyr, which is longer than the age of Iapetus! This shows that Q was several orders of magnitude lower for a long time. However, the large flattening indicates the opposite, i.e. a thick and rigid lithosphere that could support the non-hydrostatic shape for billions of years.
These two facts are difficult to reconcile, although (Castillo-Rogez et al., 2007, 2009) found that they could be explained if the accretion of Iapetus had been completed shortly (3.5–4 Myr) after the formation of CAI (i.e. Calcium-Aluminium Inclusions in chondrites). More advanced model of Robuchon et al. (2010) further reduces the range of possible time of accretion and indicates that special Burgess rheology is necessary.
Exogenic origin. ER is the build up of in-falling material from a ring or disk of the orbiting material (Ip, 2006; Levison et al., 2011; Walsh et al., 2011; Dombard et al., 2012). Walsh et al. (2011) present mechanical simulations of the ridge growth from an in-falling ring of debris. Dombard et al. (2012) consider formation of ER from a subsatellite created in a giant impact. According to them, the impact’s ejecta formed the subsatellite. The tidal interaction between the bodies of the system eventually leads to origin of the ridge.
Contraction of Iapetus. Sandwell and Schubert (2010) have proposed the model that does not require high initial spin rate or the short lived radioactive isotopes (SLRI). Initially Iapetus is a slightly oblate spheroid with the porosity higher than 10%. Radioactive heating by long-lived isotopes warms the interior to about 200 K, at which point the interior becomes ductile and compacts by 10%, while the 120 km-thick external shell remains solid. The shell deforms to match the reduced volume of the interior. The deformation occurs along the equator, probably as a result of a thinner shell below the equator. To maintain this non-equilibrium shape, the thickness of the shell must exceed 120 km.
In the present paper we follow some suggestions of Czechowski and Leliwa-Kopystyński (2008), i.e. we try to explain the Iapetus shape and existence of ER without assuming a large non-hydrostatic equatorial bulge. Instead of purely thermal convection we propose gravitational differentiation followed by convection driven by difference of the density.
2. Isostasy and Scale of Differentiation
Let us note that the considered here Cassini data concern the geometric shape only (e.g. Giese et al., 2008; Thomas et al., 2007; Thomas, 2010). The comparison of this shape with the shape of equipotential surface, i.e. the geoid, is necessary to prove that the flattening is non-hydrostatic. Most of terrestrial mountains are in isostatic equilibrium, i.e. they are underlain by ‘root’ formed from low density matter. The gravity acting on the elevated parts is compensated by buoyancy force acting on the roots. The iso-static equilibrium is a result of the fluid-like properties of the rocks in the Earth’s mantle.
The rheology of icy satellites is similar to terrestrial rocks although for different range of temperature and pressure. The uppermost layer (’lithosphere’) is elastic for small deformation and brittle for large deformations. It means that mountains on the surface could exist for billions of year. The medium below the lithosphere is also solid but for very slow geologic processes it behaves like a viscous fluid.
3. Model of Thermal History and Differentiation
Differentiation starts when the temperature exceeds the melting temperature of the ice. Calculations (e.g. Castillo-Rogez et al., 2007) indicate that temperature in the substantial part of Iapetus (30–50%) was high enough for melting. However their calculations do not include the role of convection. Czechowski (2012) develops the model based on the finite difference method combined with parameterized model of convection. It includes solid state convection, melting, convection in molten region and differentiation. The heating from the decay of the short-lived and the long-lived radioactive isotopes are included as well as the heat of accretion. The model has 3 basic parameters: (i) tini time from formation of CAI to beginning of accretion, (ii) tacr duration of accretion, (iii) η0 viscosity of the satellite interior at the temperature of melting (but before melting).
4. Molten Region and the Coriolis Force
5. The Model of the Overturn
After the overturn the present stable state was established. Let us note that axial symmetry of the flow is a consequence of latitude dependent thickness of the ice layer. In the absence of this factor the uprising matter would form several small separate plumes. It is analogous to thermal convection when initial pattern consists of small downward currents (e.g. Robuchon et al, 2010).
The thermal convection evolves to the steady state (e.g. Czechowski and Leliwa-Kopystyński, 2005). For moderate values of the Rayleigh number the steady state often forms two-cell pattern consisting of two torus-like cells with a common region of upward motion (below the equator) and two regions of downward motion (below the polar regions). The process of displacement of the ice layer is too short for similar evolution. When the whole ice concentrates close to the surface, the stability is restored and the motion stops. Then the isostatic vertical motion forms the EB (density of the upper layer around the equator is lower than the density in the polar regions).
The substantial redistribution of mass inside the satellite changes its moments of inertia and consequently its rotation axis. However in the case of the considered overturn the redistribution was axially symmetric and the rotation axis kept its direction.
There are a few advantages of our hypothesis. It explains both: EB and ER in the frame of one hypothesis. The lithosphere is not treated as an ideal layer that can support large (and large scale) non-hydrostatic load for billions of years. The lithosphere could be a realistic one (e.g. fractured by large impacts during HBE). Note, that strength of the intack rock is not a crucial parameter in the basic theory of thrust faulting (e.g. Watts, 2001, pp. 253–271; Turcotte and Schubert, 2002, pp. 343–350). Usually the medium contains many pre-existing faults. Under the tectonic stresses those pre-existing zones of weakness are activated. The effective strength of the rock layer depends mostly on the coefficient of friction and on weight of the rock layer. Let us note also, that our hypothesis does not require any special reological properties of the interior of Iapetus (compare e.g. Robuchon etal., 2010).
All hypotheses of the origin of ER require the material building the equatorial ridge is of different composition than the average of the satellite. Endogenic (e.g. volcanic) origins assume differentiation of the primitive matter. It means that material of ER is enriched in volatiles. The hypotheses assuming origin of ER from debris put into orbit require enrichment of ER in non-volatiles as a result of heating by impacts. So, the bulk composition of ER could indicate way of origin. Unfortunately most of the surface of Iapetus is covered by material that probably is different than material of underlying layer. In our hypothesis most of the roots of EB could be covered by the crust of primitive composition (see Fig. 2).
Why the excess flattening and the equatorial ridge are found on the Iapetus only? Let us consider the situation of other MIS of Saturn. Iapetus is a specific satellite for many reasons (e.g. Mosqueira and Estrada, 2005; Giese et al., 2008). It is the most distant of all other MIS of Saturn. It accreted in other part of nebula, so it could include more volatiles. Moreover, the uniform model of all MIS of Saturn developed by (Czechowski 2006, 2009) indicates problems of including Iapetus. Our hypothesis allows also for other explanations. Czechowski (2012) indicates that partial differentiation is possible only for small range of parameters of the model. For low tini usually the whole celestial body is differentiated. For large tini there are not melting and no differentiation at all. For both cases densities of the crust in the equatorial region and polar region would the same, so formation of EB and ER would be not possible. It is also possible that ER is not unique. Some structures on other satellites could be analogous to ER (Czechowski and Leliwa-Kopystyński, 2005).
We hope that Cassini mission will provide data about gravity of Iapetus necessary to discriminate between hypotheses of hydrostatic and non-hydrostatic flattening.
Acknowledgments. This work was partially supported by the Polish Ministry of Education and Science (grant 4036/B/H03/2010/39) and National Science Centre (grant 2011/01/B/ST10/06653). Computer resources of Interdisciplinary Centre for Mathematical and Computational Modeling (ICM) of Warsaw University are also used in the research.
This work was partially supported by the Polish Ministry of Education and Science (grant 4036/B/H03/2010/39) and National Science Centre (grant 2011/01/B/ST10/06653). Computer resources of Interdisciplinary Centre for Mathematical and Computational Modeling (ICM) of Warsaw University are also used in the research.
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