Paper Number: 2503
U-Pb geochronology and Nd isotope contributions to the interpretation of a peculiar ring massif: the Santa Eulália plutonic complex (SW Iberia, Portugal)
Carrilho Lopes, J.1, Sant’Ovaia, H.2, Martins, H.C.B.2, Nogueira, P.3, Lopes, L.3
1 Instituto Dom Luiz / Dept. Geociências, E.C.T., Universidade de Évora, Portugal, carrilho@uevora.pt
2 Instituto de Ciências da Terra / Dept. G.A.O.T., F.C., Universidade do Porto, Portugal.
3 Instituto de Ciências da Terra / Dept. Geociências, E.C.T., Universidade de Évora, Portugal.
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The Santa Eulalia plutonic complex (SEPC) is a late-Variscan granitic body placed in the Ossa-Morena Zone. The host rocks of the complex belong to metamorphic formations from Proterozoic to Lower Paleozoic. The SEPC is a ring massif (ca. 400 km2 area) composed of two main granitic facies with different colours and textures. From the rim to the core, there is (i) a peripheral pink medium- to coarse-grained granite (G0 group) involving large elongated masses of mafic and intermediate rocks, from gabbros to granodiorites (M group), and (ii) a central gray medium-grained granite (G1 group).
The mafic to intermediate rocks (M group) are metaluminous and show a wide range of compositions: 3.34–13.51 wt% MgO; 0.70–7.20 ppm Th; 0.84–1.06 (Eu/Eu*)N (Eu* calculated between Sm and Tb); 0.23–0.97 (Nb/Nb*)N (Nb* calculated between Th and La). Although involving the M-type bodies and forming the outer ring, the G0 granites are the most differentiated magmatic rocks of the SEPC, with a transitional character between metaluminous and peraluminous: 0.00–0.62 wt% MgO; 15.00–56.00 ppm Th; and 0.19–0.42 (Eu/Eu*)N ; 0.08–0.19 (Nb/Nb*)N [1][2]. The G1 group is composed of monzonitic granites with a dominant peraluminous character, and represents the most homogeneous compositional group of the SEPC: 0.65–1.02 wt% MgO; 13.00–16.95 ppm Th; 0.57–0.70 (Eu/Eu*)N ; 0.14–0.16 (Nb/Nb*)N . According to SiO2 vs. (Na2O+K2O–CaO) relationships, the M and G1 groups predominantly fall in the calc-alkaline field, while the G0 group is alkali-calcic; on the basis of the SiO2 vs. FeOt/(FeOt+MgO) correlation, SEPC should be considered as a magnesian plutonic association [3].
New geochronological data (U-Pb on zircons) slightly modify the age of the SEPC obtained by other methods (290 Ma, [4]). These data provide ages of 306 ± 2 Ma for the M group, 305 ± 6 Ma for the G1 group, and 301 ± 4 Ma for the G0 group, which confirm the late-Variscan character of the SEPC, indicating however a slightly older emplacement, during the Upper Carboniferous. Recently obtained whole-rock isotopic data show significant post-magmatic disturbance to the Rb-Sr system, but reveal a consistent set of Sm-Nd results that are valuable for inferring the magmatic sources of this massif: M group (−2.9 < εNdi < +1.8); G1 group (−5.8 < εNdi < −4.6); G0 group (−2.2 < εNdi < −0.8).
These geochemical data suggest a petrogenetic model for the SEPC explained by a magmatic event developed in two stages. Initially, magmas derived from long-term depleted mantle sources (εNdi < +1.8 in M group) were emplaced into the crust, promoting its partial melting and extensive mixing and/or AFC magmatic evolution, thereby generating the G1 granites (εNdi < −4.6). Subsequently, a later emplacement of similar primary magmas in the same place or nearby, could have caused partial melting of some intermediate facies (e.g. diorites) of the M group, followed by magmatic differentiation processes, mainly fractional crystallization, able to produce residual liquids compositionally close to the G0 granites (εNdi < −0.8). The kinetic energy associated with the structurally controlled (cauldron subsidence type?) motion of the G0 liquids to the periphery is considered to have been strong enough to drag up the M group rocks as blocks occurring inside the G0 granitic ring.
References:
[1] Lopes JC et al. (1998) Comun. Inst. Geol. Min. 83: 127-142.
[2] Sant’Ovaia H et al. (2015) Geol. Mag. 152(4): 648-667.
[3] Frost BR et al. (2001) J. of Petrol. 42: 2033-2048.
[4] Pinto MS (1984) Memórias e Notícias, 97: 81-94.