Volume 583, November 2015
|Number of page(s)||8|
|Section||Planets and planetary systems|
|Published online||05 November 2015|
The gravitational potential energy of n different subsystems with volumes Di and densities (MacMillan 1958) is (A.1)where and the potential10 of each subsystem (MacMillan 1958) is given by (A.2)In our case we have three constituents (i,j = m,f,s), hence (A.3)The difficulty in evaluating this expression is related to the geometry of the region occupied by the fluid. To overcome this problem, we take into account (Escapa & Fukushima 2011) that (A.4)the superscript (0) referring to the configuration when Rm = Rs. In this way, from Eqs. (A.2) and (A.4) the gravitational potential of the fluid can be written in the form (A.5)The potential is that of a fluid with density ρf and volume given by an sphere of radius dm centered at the mantle barycenter; the potential corresponds to a fluid with density ρf and volume given by an sphere of radius ds centered at the inner core barycenter.
Accordingly, the gravitational potential energy of the system is (A.6)The subsystems involved in this equation are spheres or spherical shells with constant or spherical symmetric density functions. Their potentials can be obtained from that of a spherical shell (B) with interior radius d1, which would be 0 for a sphere, and exterior radius d2, whose density is a piecewise continuous function ρ of the distance from the center. This has the expression (A.7)If in this equation the density is , we recover the formulas given in Escapa & Fukushima (2011, Eq. (B3)11).
The application of Eqs. (A.7) to (A.6) provides the constant k1, arising from the terms and , and from , , , and . The first group is constant because it is the case for the potential when evaluated at interior points of the spherical shell. The second group is constant because it provides the gravitational self-energy of spheres or spherical shells referring to the same region of space.
The remaining terms in can be cast as (A.8)With the expression of arising from Eq. (A.7), it reads (A.9)A change of variable R′′ = R−Rs = R−Rm−r allows computing this integral with respect to a reference system whose origin is located at the center of sphere . In this way, we obtain (A.10)where k2 comprises all the constant terms resulting from the integration, and Vol Vol Ds is the volume of the inner core.
Appendix B: Expression of the amplitude ratio of the mantle to the inner core for the stratification of the rigid layers assumed in Coyette et al. (2012)
Here, we follow the same notation as Coyette et al. (2012). With this, we can write12 for the mass of the mantle, the fluid, and the inner core (B.1)The mean density of the inner core reads as (B.2)The amplitude ratio of the mantle to the inner core (Eq. (9)) can be written as (B.3)From Eqs. (B.1) and (B.2), with ρf = ρic + 1, we obtain (B.4)where [ρ]j = ρj−ρj + 1,j = 1,...,N−1, [ρ]N = ρN.
© ESO, 2015
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