Thermal evolution and sintering of chondritic planetesimals - IV. Temperature dependence of heat conductivity of asteroids and meteorites

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Table 1

Pure mineral species considered for calculating the properties of chondrite material.

Solid solution	Chemical	A	ϱⁱ	K		n^j	Θ_a
component	formula		g/cm³	W/mK	K		K
Quartz	SiO₂	60.09	2.65	6.49^b	567	9	273
Olivine
forsterite	Mg₂SiO₄	140.70	3.227	5.158^a	747	28	246
fayalite	Fe₂SiO₄	203.77	4.402	3.161^a	532^f	28	203
Orthopyroxene
enstatite	Mg₂Si₂O₆	200.79	3.204	4.909^d	719	40	210
ferrosilite	Fe₂Si₂O₆	263.86	4.002	3.352^d	541^h	40	158
Clinopyroxene
diopside	CaMgSi₂O₆	216.56	3.279	5.376^a	654	40	191
(+ en + fs)
Plagioclase
albite	NaAlSi₃O₈	262.23	2.610	2.349^a	462	52	124
anorthite	CaAl₂Si₂O₈	278.36	2.765	1.679^a	518	104	131
orthoclase	KAlSi₃O₈	278.33	2.571	2.315^a		52
Troilite	Fe_1−δS	87.91	4.91	4.60^b	270^g	1.875
Iron–nickel alloy
iron	Fe	55.45	7.81	71.100^c
nickel	Ni	58.69	8.91	80.800^c

Notes. The table lists: the chemical composition, atomic weight, A, mass-density, ϱ, thermal conductivity, K, at 300 K, Debye temperatureΘ_D from heat capacity, number of atoms, n, per unit cell, estimated Debye temperature, Θ_a, for heat conductivity according to Eq. (3). The minerals form the indicated solid solutions.

References. ^(a) Horai & Simmons (1969), ^(b) Clauser & Huenges (1995), ^(c) Ho et al. (1978), ^(d) extrapolated value from Horai & Baldridge (1972), ^(e)from Kiefer (1980), ^(f)from Kobayashi et al. (1999), ^(g)from Chung (1971), ^(h)from Cemič & Dachs (2006), ⁽ⁱ⁾from Smyth & McCormick (1995), ^(j)number of formula units per primitive cell taken from Smyth & McCormick (1995).

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