Tourmaline from six pegmatites of the lepidolite-subtype was examined to de
termine compositional trends: symmetrically zoned Lastovicky, Dobra Voda, R
ozna, Dolni Bory and Radkovice dykes, Czech Republic, and relatively homoge
neous dykes at Red Cross Lake, Manitoba. The five symmetrically zoned lepid
olitesubtype pegmatites contain the following zones from the outermost zone
inward: 1) granitic zone, (2) graphic zone, (3) blocky K-feldspar zone, (4
) albite zone, (5) lepidolite zone, (6) quartz core and (7) rare-to-absent
small pockets. The crystallization sequence of tourmaline was determined fr
om the characteristic composition of tourmaline for each pegmatite zone and
from the compositional zoning within individual crystals. In granitic and
outer albite zones, black tourmaline ranges from foitite-schorl to schorl-f
oitite, and is associated with minor biotite close to the contact with the
host rocks, and with abundant Fe-bearing muscovite. In the albite zones, da
rk blue and green elbaite-schorl is associated with pale greenish yellow Na
-bearing muscovite. In the lepidolite zones, pink elbaite-rossmanite to ros
smanite-elbaite occurs with purple lepidolite and minor pink and green lepi
dolite. Green (Fe, Mn)-bearing elbaite occurs in the quartz core at Rozna a
nd is associated with cookeite in late pockets at Dobra Voda and Dolni Bory
. Late hydrothermal foitite occurs as terminations on zoned tourmaline crys
tals in pockets at Dobra Voda. Based on paragenesis and textural relations,
rossmanite-elbaite is the last tourmaline composition to crystallize in th
e Radkovice, elbaite-rossmanite is the last at Lastovicky and Red Cross Lak
e dykes, (Fe, Mn)-bearing elbaite is the last at Rozna and Dolni Bory, and
foitite is the last at Dobra Voda. Lepidolite-subtype pegmatites contain fo
itite as the most primitive composition in the outermost pegmatite zones, a
nd rossmanite or (Fe, Mn)-bearing elbaite as the most fractionated composit
ions in the innermost pegmatite zones. In contrast, elbaite-subtype pegmati
tes in the literature contain Mg-rich schorl and either elbaite or rarely l
idicoatite, respectively. Typically, tourmaline from lepidolite-subtype peg
matites is Ca- and Mn-poor (<0.03 apfu Ca, <0.30 apfu Mn), whereas tourmali
ne from elbaite-subtype pegmatites is relatively Ca- and Mn-rich, commonly
with up to 0.30 apfu Ca and locally up to 1.1 apfu Mn. Schorl in lepidolite
-subtype pegmatites is rich in X-site vacancies, whereas schorl in elbaite
subtype pegmatites is Na rich. A negative correlation exists between Fe and
Al + Li at the Y-site in tourmaline due to fractional crystallization of t
he evolving pegmatite-forming melt. The positive correlation between Na and
F in tourmaline is due to crystal-chemical constraints. Sodium and Mn are
preferentially partitioned into tourmaline, and F is preferentially partiti
oned into lepidolite.