Table 1 A comparison between the RTP and the T_a -transform.

Prior knowledge of the source magnetization vector’s (inclination I and declination D) and geomagnetic field’s (inclination I₀ and declination D₀) directions is required for the RTP estimation to operate effectively. For the T_a calculation, only the direction (I₀ and D₀) of the geomagnetic field is required.

Whereas the RTP maps, like the measured field, can have both positive and negative values, T_a only has nonnegative values. This makes it easier to compare the T_a maps with those from geological sources and to interpret them visually.

I = I₀ and D = D₀ are the main limiting assumptions for applying the RTP transformation, which states that the source magnetization is exclusively induced. This assumption will result in inaccurate RTP field mapping, which will affect how the RTP anomalies are interpreted both quantitatively and qualitatively. This is particularly risky because many inversion techniques employ the RTP field instead of directly inverting the observed magnetic field, as in⁵. As a result, inaccurate estimations will be generated by any ineffective inversion technique.

No assumptions regarding the nature of source magnetization are generated by the transform T_a.

T_a has greater potential than RTP for simplified magnetic field representations especially when the same map has sources that have distinct magnetization directions or remaining source magnetization [5][39][40]

Low magnetic latitudes produce instability in the RTP operator. At latitudes I₀ = 20° and D₀ = 0, the RTP transform maps are deformed and difficult to comprehend. Special stabilization procedures for low magnetic latitudes^62,63 are needed to calculate interpretable RTP maps, which result in neater-looking but occasionally inaccurate maps. The issue of the frequently inaccurate assumption of induced magnetization additionally pertains up.

The T_a calculation can provide accurate and well-centered maps.

Low magnetic latitudes cause instability in the RTP transfer function¹⁶.

The frequency domain T_a estimate techniques have a denominator that is one degree below the RTP transfer function’s denominator¹⁶.

Special methodologies are required to calculate the RTP throughout extensive regions⁶⁴.

The same is true for the T_a transforms [65], however the RTP requires more complicated processes than the T_a computation. Another challenge with RTP computation across large regions is the assumption that source magnetizations are solely induced, which is rarely achieved.

In regard to signal dependence, T_a could more accurately represent the magnetic field that revolves on each of the associated sources¹.

In contrast to the measured magnetic field, the centricity is substantially better for the 3D situation, even though the magnetic anomalies are not precisely centered over the magnetic sources¹⁷.

When induced-only source magnetization is present, the transform T_a to RTP’s primary drawback occurs. The primary benefits of MMTs are their centricity to the sources of their anomalies and their shape regarding the geomagnetic field’s orientation (D₀ & I₀).

A complicated and memory-intensive process is the RTP computation.

Simple calculation