The CPD can provide an approximation to the depth to the bottom of the magnetised crust that defines the depth to which ferromagnetic minerals lose their magnetisation. This depends on the magnetic mineralogy of the crust which is usually magnetite which has a Curie temperature of ~580?C (Ross et al., 2006; Spector & Grant, 1970). However, this value changes depending on the magnetic mineral composition within the rocks (Chiozzi et al., 2005).
Spectral methods have been intensively used in the determination of the depth to the Curie isotherm. These methods are best in determining the regional CPD by examining the spectral properties of the magnetic anomalies over relatively large regions (Blakely, 1988; Hussein et al., 2013; Shuey et al., 1977).