Polar anisotropy is the same as Transverse isotropy. It involves elastic properties that are the same in any direction perpendicular to a symmetry axis (the "pole"), but different parallel to the axis, and it has five independent elastic constants; see Thomsen anisotropic parameters and see Figure T-13.This symmetry is like a crystal having hexagonal symmetry; see Figure S-29.
A sequence of generally horizontal, thin isotropic (or polar isotropic) layers (such as sedimentary bedding) tends to produce layering anisotropy (sometimes called periodic thin-layer anisotropy, although the layering need not be periodic) for wavelengths that are appreciably larger than the layer thickness. The axis of symmetry is generally perpendicular to the bedding, more-or-less vertical, with the velocities of P-waves parallel to the bedding and S-waves that are polarized parallel to the bedding being larger than for those perpendicular to the bedding. Parallel isotropic layering, where there are more than eight or so layers per wavelength, behaves as a polar anisotropic medium. Roughly horizontal layering is also called transverse isotropy because properties are the same in any transverse direction with a vertical axis of symmetry (TIV). See also azimuthal asymmetry.
With a vertical symmetry axis, pure P- and S-waves may exist only in certain directions. SH-wavefronts are ellipsoidal in shape (see Figure A-14c) and SV- and P-modes of propagation are coupled with nonelliptical wavefronts that in general are not othogonal to the directions of wave propagation. Phase velocity (wavefront velocity) perpendicular to the wavefront surface of constant phase and ray velocity in the direction of energy transport (also called group velocity) are generally not in the same direction (see Figure A-14a). The reciprocal of phase velocity (also a vector quantity) is called slowness. SV-wavefronts may have cusps. See Thomsen, 2002.