Gravimetric Forward and Inverse Modeling Methods of the Crustal Density Structures and the Crust-Mantle Interface - Planetary Exploration and Science: Recent Results and Advances - page 70

Tabl e 4. 1 Statistics of the stepwise consolidated crust-stripped gravity disturbances (as shown in

Fig. 4.1 )
Gravity disturbances Min [mGal] Max [mGal] Mean [mGal] STD [mGal]

ı g 225 257 1 29

ı g T 647 156 72 107

ı g TB 511 636 260 233

ı g TBI 508 639 285 202

ı g TBIS 492 667 327 192

ı g cs 1,416 473 18 332

Fig. 4.2 The complete crust-stripped isostatic gravity disturbances computed globally on a 1 1

arc-deg surface grid

according to the expression in Eq. ( 4.18 ). The inverse solution was carried out
iteratively using a Gauss-Seidel scheme (e.g., Young 1971 ). The regularization
was applied to stabilize the ill-posed solution. The gravimetric Moho solution is
shown in Fig. 4.3 . The Moho depths vary globally between 3.6 and 85.1 km, with
a mean of 13.6 km and a standard deviation of 13.4 km. The global map revealed a
typical pattern of the Moho geometry with the enhanced contrast between the thick
continental crust and thinner oceanic crust. The largest Moho depths were confirmed
under Andes and Himalayas with extension beneath the Tibetan Plateau, where the
maximum Moho depths exceed 70 km.