Two types of metamorphic phengites are known: one is linked to high pressure and is 3T, the other is 2M(1), and its composition is linked to rock-compositional constraints. This work investigates the octahedral sheet crystal-chemical differences between the two phengite types. Seven dioctahedral micas were studied: (1) one 3T phengite from an ultrahigh-pressure metagranitoid in the Dora Maira massif, Italy (P similar to 4.3 GPa, T similar to 730 degrees C); (2) five 2M(1) phengites from medium-P orthogneisses in the Eastern Alps metamorphic basement, Italy (P <= 0.7 GPa, T similar to 500-600 degrees C); and (3) one 2M(1) ferroan muscovite from pegmatite in Antarctica (P <= 0.2 GPa, T similar to 500 degrees C). All micas display significant extents of celadonite substitution. In particular, the 2M(1)-phengite formulae (calculated on the basis of 11 O) have 0.68 < Al-IV < 0.82 atoms per formula unit (apfu); octahedral atoms are dominated by Al (1.6-1.8 apfu), with minor and variable Fe (0.20-0.35 apfu) and Mg (0.05-0.17 apfu), and very minor Ti, Mn, and Cr. Total octahedral occupancies are slightly above 2.00 apfu, i.e., there seems to be partial occupancy of the third M site. For all micas, we recorded XAFS spectra on mosaics of carefully separated flakes oriented flat on a plastic support that could be rotated so as to account for the polarization of the synchrotron radiation beam, and we processed them on the basis of the AXANES theory. Spectra show angle-dependent absorption variations for Al and Fe, which can be deconvoluted and fitted by dichroic effects. Pre-edges consistently show most Fe to be Fe3+ and little angle-dependent intensity variations. The 2M(1)-ferroan muscovite from Antarctica displays the same AXANES behavior as 2M(1)-phengites. By contrast, the ultrahigh-pressure 3T-phengite from Dora Maira (having Al-IV = 0.42 apfu, and Al and Mg as the dominant octahedral constituents) has XAFS spectra that differ significantly. Not only is the Al-IV feature strongly reduced, in agreement with the increased Si content, but also Fe XAFS spectra show one broad feature only, indicating that all Fe is Fe 21 in a fully disordered distribution with no angle-dependent variations. We conclude that this 3T-phengite is actually contaminated by exsolved Fe-bearing pyrope platelets, which cannot be resolved under SEM examination; by contrast, the 2M(1)-phengites, unrelated to high-pressure, suggest Al/Fel(3+) order over the M1 and (M2, M3) sites, as also does the 2M(1) pegmatitic muscovite.