Gondwana Research 17 (2010) 676–687

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Gondwana Research

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Ediacaran Águas Belas pluton, Northeastern : Evidence on age, emplacement and magma sources during Gondwana amalgamation

Adejardo F. da Silva Filho a,⁎, Ignez P. Guimarães a, Valderez P. Ferreira a, Richard Armstrong b, Alcides N. Sial a a Departamento de Geologia—CTG, Universidade Federal de , Rua Acadêmico Helio Ramos S/N Cidade Universitária, , Pernambuco, 50740-530, Brazil b Research School of Earth Sciences, the Australian National University, Canberra, Australia article info abstract

Article history: Ediacaran syenogranites from the Águas Belas pluton, Borborema Province, Northeastern Brazil were investigated Received 12 January 2009 in this work. The studied granitoids show high SiO2, Fe# [FeO/(FeO+MgO)], total alkalis (K2O+Na2O) and BaO Received in revised form 29 September 2009 contents and medium Sr and low Nb contents. They show gentle fractionated rare earth patterns with discrete Eu Accepted 6 October 2009 negative anomalies. Major and trace element data point to chemical features of transitional high-K calc-alkaline Available online 17 October 2009 to alkaline post-collisional magmatism. Structural data coupled with geochronological data suggest that NNE– SSW-trending sinistral movements at shear zones were initiated at ca. 590 Ma and have activated E–W pre- Keywords: existing structures at the current crustal level. The synchronism of these shear zones allowed the dilation to Ediacaran Syenogranite generate the necessary space for the emplacement of the Águas Belas pluton. Geochemistry U–Pb SHRIMP zircon data show a cluster of ages around 588±4 Ma which is interpreted as the crystallization age. U–Pb SHRIMP geochronology Some zircon grain cores yielded ages within 2060–1860 Ma and 1670–1570 Ma intervals. Oxygen isotope Oxygen isotopes compositions of zircon grains with distinct ages were measured using SHRIMP techniques. Twenty three analyses in the same zircon spots previously analyzed for U–Pb show δ18O values ranging from 5.79‰ to 10.30‰ SMOW. This large range of values results from variations both between grains and within grains (core–mantle/rim), and is interpreted as the result of mixing of components with distinct oxygen isotope compositions. The U–Pb zircon 18 ages and the δ O values associated with Paleoproterozoic Nd TDM model ages suggest that the protolith of these granitoids involved a mantle component (Paleoproterozoic lithospheric mantle), Paleoproterozoic and Mesoproterozoic igneous rocks. Interactions with Mesoproterozoic or Neoproterozoic supracrustal rocks, may have occurred during the intrusion. The resulting magma evolved through biotite and K-feldspar fractionation. © 2009 International Association for Gondwana Research. Published by Elsevier B.V. All rights reserved.

1. Introduction similarities with A-type granites (Liegéois et al., 1998). As pointed out by Pearce (1996), the post-collisional granites are the most The Brasiliano orogeny (650–550 Ma) in the Borborema Province, difficult to classify, since some of them have subduction-like mantle northeastern Brazil, is marked by a large number of granitoid sources with many characteristics of volcanic-arc granites while intrusions associated with either low- or high-angle large scale others show within plate character. According to Eby (1992), A-type shear zones (e.g. McReath et al., 2002; Guimarães et al., 2005; Bueno granitoids can be divided into A1- and A2-types. The A1-type occurs in et al., 2009). Geochronological data of these granitoids can constitute a true anorogenic setting and it has OIB signatures, while the A2-type an important tool in dating these tectonic events. occurs in post-collisional or post-tectonic setting, usually shortly (10– The post-collisional tectonic setting is characterized by large 20 million years) after compressional tectonics, is rarely, or not intrusion of high-K calc-alkaline magmas. This tectonic setting usually associated with silica-undersaturated alkaline rocks, have trace ends with minor amounts of highly evolved high-K calc-alkaline or element signatures similar to sub-continental lithosphere and crust, alkaline magmatism, which mark the end of the orogeny. Highly and never have OIB signature. evolved high-K calc-alkaline magmatism generally shows some Oxygen isotope ratios of magmas reflect their source and contaminants. According to Eiler (2001) the mantle is a homogeneous reservoir. Igneous zircons in high temperature equilibrium with mantle magmas have an average of δ18O=5.5±0.3‰ (Valley et al., 1998). This value remains approximately constant during fraction- ⁎ Corresponding author. Tel.: +55 81 21268240; fax: +55 81 21262834. ation processes, and change can only be achieved by adding a material E-mail address: [email protected] (A.F. da Silva Filho). of a distinct oxygen isotope composition to the magma (Valley, 2003).

1342-937X/$ – see front matter © 2009 International Association for Gondwana Research. Published by Elsevier B.V. All rights reserved. doi:10.1016/j.gr.2009.10.002 A.F. da Silva Filho et al. / Gondwana Research 17 (2010) 676–687 677

Significant deviations from the mantle value are the result of magma to diatexites from the margin to the centre of the western part of the interactions with low temperature rocks (supracrustal rocks) and batholith. rocks from near the surface associated with large oxygen isotope The ages of the PEAL domain units are still poorly constrained. It is fractionation. probable that grouping units based primarily on rock-type has Granites are classically considered by various authors to probe the lumped together units having primary depositional or plutonic ages crust, giving important clues to the understanding of the crustal ranging from Paleoproterozoic (or older) to Brasiliano (Neoproter- evolution. The Pernambuco–Alagoas domain, which is among the ozoic). Brito Neves et al. (1995) presented Rb–Sr isochron ages major crustal domains of the Borborema Province, was shown by Silva ranging between 1.13 Ga (diatexites) and 0.96 Ga for rocks assigned Filho et al. (2002) to be comprised by various crustal sections of very to the Cabrobó and Belém do São Francisco complexes (Santos, 1995) different Nd TDM ages. The Águas Belas pluton shows Paleoproterozoic in western PEAL domain. The TDM model ages for rocks of these Nd TDM (Silva Filho et al., 2002) but is surrounded by supracrustals complexes range between 1.50 Ga to 1.30 Ga (Santos, 1995). and volcanics of Mesoproterozoic Nd TDM age (Van Schmus et al., Very few U–Pb (zircon) ages are available for the PEAL domain. 2008), and then has been considered among the main metaluminous Van Schmus et al. (1995) reported a zircon upper-intercept apparent granitic intrusion from the Pernambuco–Alagoas domain, with some age of 1577±73 Ma for garnet-bearing migmatite, west of Palmeira A-type petrographic and geochemical signature (Silva Filho et al., dos Indios town. A single U–Pb age in zircon obtained by LA-ICPMS 1996). The aim of this paper is to present geochemical, U–Pb SHRIMP from migmatized tonalitic orthogneisses in the area, NE of zircon and oxygen isotopic data for discussing the age, the sources and , yields an age of 2000 Ma (Neves et al., 2005a,b). The early the tectonic setting of a large granite intrusion, the Águas Belas pluton, interpretations of a Paleoproterozoic to Archean age for most of the located in the Pernambuco–Alagoas domain of the Borborema PEAL domain have not been confirmed by the few new zircon ages. Province, which altogether could shed light on the last stages of the U–Pb zircon ages in granitoids of the PEAL domain show an Gondwana amalgamation. interval from 570 Ma to 625 Ma (Silva Filho et al., 1997, 2008; Silva

Filho and Guimaraes, 2000) and Nd TDM model ages range from 1200 2. Regional geology to 2000 Ma (Silva Filho et al., 2006). A larger data set reported by Silva

Filho et al. (2002, 2006) expanded the range of TDM ages from 900 to The Borborema Province (Almeida et al., 1977) is located in north- 2800 Ma and the data show a bimodal distribution, indicating that eastern Brazil, north of the São Francisco craton (Fig. 1a). Although the most of the Nd formation ages are either Neoproterozoic or region was highly deformed and metamorphosed during the Brasiliano Paleoproterozoic. The low frequency of samples with TDM ages from orogeny, many features of pre-Brasiliano geology can still be recognized 1500 to l800 Ma may indicate that Cariris Velhos (980–920 Ma) from the rocks, including isotopic signatures. In a pre-drift reconstruc- igneous rocks, which commonly have TDM ages in this range (Van tion (De Wit et al., 1988), the Borborema Province lies adjacent to coeval Schmus et al., 1995; Brito Neves et al., 2001), are scarce or not found in Pan-African and cratonic terranes from western Africa (Toteu et al., the PEAL domain. Silva Filho et al. (2002) evaluated the evolution of 2001). the PEAL domain based on Sm–Nd isotopic data from the Neoproter- The Pernambuco–Alagoas crustal domain (PEAL) is one among the ozoic granitoids, and defined two crustal sub-domains: Garanhuns six crustal domains identified by Van Schmus et al. (2008) in the and Água Branca sub-domain. Borborema Province. It is limited to the north with the Transverse Silva Filho et al. (2006) based on new Nd isotopic data from Zone domain, to the south with the Sergipano domain, and its eastern granitoids, orthogneisses and supracrustal rocks proposed three crustal part is cut by large granitic batholiths (Fig. 1b). sub-domains for the PEAL domain: (i) Garanhuns with TDM model ages Medeiros and Santos (1998) recognized some metamorphic in the interval 1600 to 2600 Ma, (ii) Água Branca with TDM model ages sequences in the Pernambuco–Alagoas domain: (i) The Cabrobó ranging from 900 to 1590 Ma and (iii) Palmares—TDM model ages complex is a dominantly supracrustal unit comprised of biotite garnet around 1110 Ma. The Àguas Belas pluton is intruded into rocks from gneisses, locally migmatized, intercalated with quartzite, schist, calc- the Agua Branca sub-domain (Fig. 1b). This sub-domain is comprised by silicate and amphibolite, orthogneisses and migmatite; (ii) The Belém the Águas Belas–Caninde batholith (Silva Filho et al., 2002) and by the do São Francisco complex is an infra-crustal segment composed of Inhapi Sequence (Van Schmus et al., 2008). It has been shown that the migmatites, biotite-gneisses, tonalitic orthogneisses, and leuco-gran- Agua Branca sub-domain is comprised mainly by rocks of TDM model odiorites to leuco-monzogranites. The occurrence of a low-angle ages from 900 Ma and 1590 Ma, and various granitic plutons and foliation and a swarm of small granitic intrusions, controlled by a orthogneisses of TDM ca. 2000 Ma, among them the Águas Belas pluton. transpressive deformation, suggest that thrusting has operated in the These data point to a setting where tectonic blocks of different ages have area (Silva Filho et al., 2002). Geological and geochronological data been put in contact during a collisional process. Collisional process has collected in the past few years showed that the PEAL domain geology is been constrained at 628±12 Ma in the adjoining Sergipano Terrane comprised by a Paleoproterozoic basement complex (Osako, 2005; (Oliveira et al., 2006). Previous geological and geochemical reconnais- Neves et al., 2005a,b), supracrustal sequences, and Neoproterozoic sance of the Àguas Belas pluton (Silva Filho et al., 1996) showed that it is granitic batholiths. comprised by late-tectonic metaluminous and high-K calc-alkaline Silva Filho et al. (1996, 1997, 2002) have identified various late- rocks. Metaluminous and amphibole±pyroxene suites are classically tectonic granitic intrusions and suites in the eastern part of the PEAL extracted from the lower crust or from the upper mantle. This pluton domain, with compositions ranging from high-K to calc-alkaline, was selected to study because it would bear inheritance from lower shoshonitic, mildly alkaline or peraluminous (± garnet-bearing) crust or upper mantle, and, as it shows high and restricted SiO2 contents, granites. These intrusions were grouped into four granitic batholiths: which is typical of crustal-derived granites, it would bear as well an Buique–Paulo Afonso, Águas Belas–Canindé, Marimbondo–Correntes, inheritance from the middle to the upper crust. So, the whole set of data and –Atalaia. The Águas Belas granitoids are part of the Águas could shed light into the Brasiliano collisional process. This paper tries to Belas–Canindé batholith. approach some complexities of the crustal evolution of this crustal The Águas Belas–Canindé batholith is limited to the south by the domain of the Borborema Province, using SHRIMP U–Pb zircon, oxygen Sergipano domain, to the north and to the east by migmatites from the isotopes and trace elements geochemistry from the Águas Belas pluton. Belem do São Francisco complex, and to the west by the supracrustal A brief evaluation on the emplacement of this pluton has been done in Inhapi sequence (Fig. 2). It comprises biotite, amphibole syenogra- order to position it in relation to the chronology of the adjoining shear nites and amphibole–pyroxene bearing syenogranites cutting meta- zones and to the flat-lying foliation from the adjoining supracrustal texites and diatexites of tonalitic composition. The metatexites grade sequences. 678 ..d iv ih ta./Gnwn eerh1 21)676 (2010) 17 Research Gondwana / al. et Filho Silva da A.F. – 687

Fig. 1. a) Sketch geological map of the Borborema Province. The main tectonic domains are from Van Schmus et al. (1995) and Van Schmus et al. (2008). PESZ=Pernambuco shear zone; PSZ=Patos shear zone. 1—Palaeozoic sedimentary basin. b) Schematic map for the crustal sub-domains of the PEAL domain. A.F. da Silva Filho et al. / Gondwana Research 17 (2010) 676–687 679

Fig. 2. a) Simplified geological map of the PEAL Domain, showing the location of the studied area. 1—Palaeozoic sedimentary cover; 2—Brasiliano granitoids; 3—Ipojuca–Atalaia Batholith; 4—Buique–Paulo Afonso Batholith; 5—Águas Belas–Canindé Batholith; 6—Garanhuns Batholith; 7—Palmares Sequence; 8— Sequence; 9—Garanhuns Quartzites; 10—Inhapi Sequence; 11—Alagoana Sub-belt; 12—Belém do São Francisco Complex; 13—Archean block; 14—Transcurrent Shear zones (PESZ—Pernambuco; RCSZ—Rio da Chata; PSZ—Palmares; LCSZ—Limitão–Caetés; ISZ—Itaíba; SBUSZ—São Bento do Una); 15—Transpressive shear zones (GSZ—Garanhuns; MSZ—Maravilha shear zone). b) Simplified geological map of the studied area. 1—The Águas Belas pluton (c—pyroxene syenogranites, d—amphibole, biotite syenogranite); 2—Garnet-two micas bearing granites from the Serrote dos Macacos (580 Ma); 3—Águas Bela—Canindé batholith; 4—Metasediments from the Inhapi Sequence; 5—Belem do São Francisco Complex; 6—Transpressive Maravilha shear zone; 7—Limitão–Caetés transcurrent shear zone; 8—Fractures; 9—Photo structural lineaments; 10—Milonitic foliation; 11—Location of the sample AB-08, analyzed for U–Pb and Sm–Nd.

3. Geology and petrography the north are sillimanite–garnet–biotite-gneisses, to the west biotite– muscovite–garnet gneisses both from the Inhapi Sequence, and to the The Águas Belas pluton constitutes an elongated intrusion with an south are other Neoproterozoic granitic plutons from the Águas 18 km long E–W-trending major axis (Fig. 2b). It is intruded along the Belas–Canindé Batholith. The contacts of the pluton are sharp with contact between the Inhapi supracrustal sequence and the Águas both gneisses and granitoids. An E–W-trending mylonitic foliation has Belas–Canindé batholith, being part of the Água Branca crustal sub- been identified in the northern contact. Xenoliths of migmatized domain (Silva Filho et al., 2006). Northwards and very close to the gneisses are observed along the northern outer contact. The Águas pluton the Venturosa Sequence crops out. This sequence is comprised Belas pluton truncates the Maravilha ductile low-angle shear zone by metasedimentary rocks and orthogneisses. Structural analysis of which runs NE–SW (Fig. 2b). The NE–SW Limitão–Caetés ductile shear this sequence shows a main Sp low-angle foliation with SE–NW zone cuts the Venturosa Sequence and terminates at the NE tip of the stretching lineations (Silva Filho et al., 2007). Another main feature of Águas Belas pluton. This shear zone shows low-angle foliation (Osako, this sequence is a high-angle foliation related to NE–SW shear zones, 2005) dipping eastward. The Águas Belas pluton cuts the Inhapi which are younger than the Sp low-angle foliation and spatially Sequence foliation at a high angle. Within the pluton an E–W weak related to various high-K calc-alkaline granitoids. The country rocks to lineation, parallel to its main axis has been recognized. Remote 680 A.F. da Silva Filho et al. / Gondwana Research 17 (2010) 676–687 sensing imagery (Osako, 2005) shows internal E–W and NE–SW high Fe# [FeOt/(FeOt+MgO)] values (0.8 to 0.92, Fig. 3d), which brittle foliations as well. classify them as belonging to the ferroan series granitoids (Frost et al., A geophysical discontinuity has been identified a few kilometres 2001). All the analyzed samples fall within the shoshonitic field in the to the north of the Águas Belas pluton (Silva Filho et al., 2007). It runs K2O vs. SiO2 diagram (Fig. 3e). from the E–W Pernambuco shear zone, the northern limit of the The Águas Belas granitoids show high Ba contents (1300–2650 ppm), Pernambuco–Alagoas domain, with trends ranging from NE–SW to medium Sr contents (430–690 ppm) and low to medium Rb contents E–W, suggesting that the Águas Belas pluton is intruded close to an (203–258 ppm). The contents of the high field-strength elements important E–W-trending crustal discontinuity. Syn- to late-tectonic (HFSE) are relatively low (Nb=8–14 ppm; Ta=0.2–2.0 ppm; granitoid intrusions, with ages ranging from 580 to 590 Ma have Zr=81–189 ppm). One sample from the southern border of the been mapped along NE–SW shear zones (Neves et al., 2006; Silva batholith shows high Ba (6155 ppm) and Sr contents (1660 ppm) and

Filho et al., 2007). have high K2O/Na2Oratio(2.2). The data available suggest that intrusion of the Águas Belas The REE patterns (Fig. 4) normalized to chondrite values of occurred after the peak of the Brasiliano metamorphism, which was Nakamura (1974) are characterized by gentle fractionated pattern, probably associated with the flat-lying foliation in both Venturosa with CeN/YbN ranging from 8.7 to 3.3, with only one sample showing (Limitão–Caetés shear zone) and Inhapi Sequences (Maravilha shear higher value (19.5), without substantial negative Eu anomalies (0.98 zone). The E–W-trending lineation recorded within the Águas Belas to 0.86). pluton and lack of large mylonitic zone within it suggest that the Bivariate plots between elements that readily enter rock-forming intrusion took place at the beginning of the operation of a discrete minerals may be used to test the fractional crystallization hypothesis ductile E–W shear zone. The pluton was later cut by brittle faults, by comparing model mineral fractionation vectors with observed data which were the channels for the ascent of bimodal volcanic rocks that arrays. Ba versus Sr correlations can provide information particularly include pyroclastic rhyolites and basalts. These brittle faults are on the feldspars and biotite fractionation. The Ba versus Sr data for the associated with the initial stage evolution of the interior sedimentary Águas Belas granitoids define a trend compatible with K-feldspar and basins of Gondwana break-up. biotite fractionation (Fig. 5a), which agrees with the negative Eu The Limitão–Caetés high-angle shear zone is a splay of the anomalies recorded in the REE patterns. The lack of correlation Pernambuco shear zone, and it terminates at the east contact of the between Ba and Sr with Eu/Eu* (Fig. 5b, c) does not support plagioclase Águas Belas pluton. A two-mica granite, the Serrote dos Macacos fractionation during the evolution of the Águas Belas granitoids. On the pluton, intruded a few kilometres north of the Águas Belas pluton, other hand, the positive correlation between Na2O and SiO2 reflects within the Limitão–Caetés shear zone (Fig. 2), yielded U–Pb monazite the later crystallization of Na-rich amphiboles, as observed in the age of 580±3 Ma (Osako, 2005). petrographic studies. Two main petrographic facies were recorded in the Águas Belas Nd isotopic analysis for one sample was carried out at the Isotope pluton (Fig. 2b): amphibole±biotite syenogranite to quartz syenite and Geochemistry Laboratories—Kansas University. It shows negative εNd pyroxene±amphibole syenogranite. They are coarse to medium (600 Ma) values (−12.4) with Paleoproterozoic TDM (2130 Ma) grained rocks with low concentration of modal mafic minerals (less model age. than 6%). Evidence of deformation under low temperature was recorded in the northern and southern border of the Águas Belas pluton. The low temperature deformation is characterized by recrystallized quartz as 5. Geochemical signature micro grains and elongated quartz grain showing undulose extinction. Amphibole-rich clots are frequently recorded. In the pyroxene± In spite of their high Ba contents, the studied granitoids do not amphibole syenogranite, the amphibole is green, bluish, and Fe-rich, meet the criteria established by Tarney and Jones (1994) for high Ba– formed by the reaction of light green pyroxene and the magma. Na-rich Sr (HiBaSr) granitoids, due to their medium Sr contents and low LREE amphibole (afverdsonite) is recorded as a later crystallized phase in the and high HREE contents. The REE patterns of the studied granitoids amphibole±biotite syenogranite to quartz syenite. Anti-rapakivi are distinct from either HiBaSr granites, which have highly fraction- texture was recorded in both petrographic units reflecting later ated patterns and from A-type granites, which have gentle fraction- crystallization of K-feldspar. Biotite occurs in very small modal amounts ated patterns but with substantial negative Eu anomalies. (<1%) always as inclusions in amphiboles or, as a later phase, replacing Multi-element diagrams normalized to the values suggested by amphiboles. Sphene is the main accessory phase. It occurs as sub- Thompson (1982) for the studied granitoids and the average element idiomorphic to idiomorphic orange crystals reflecting high LREE concentration of I-type S-type and HiBaSr granites (Fowler et al., 2008) concentrations (Guimarães et al., 1993). Zircon, opaque minerals, are shown in Fig. 6a and b. The studied granite patterns are characterized allanite and apatite are the other accessory minerals recorded in the by troughs at Nb, Ti, P and either peak or troughs at Sr. Compared to the Águas Belas granitoids. average of I-type and HiBaSr granites (Tarney and Jones, 1994)the studied granitoids have lower Sr, P and Ti concentrations. 4. Geochemistry and Sm–Nd data Morrison (1980) pointed out the main characteristics of the

shoshonitic association: high total alkalis (K2O+Na2O>5), low TiO2 Representative samples from the Águas Belas pluton were analyzed (<1.3 wt.%), no Fe enrichment in the AFM diagram and high contents for major elements by ICP-AES and for trace elements by ICPMS at of LILE (Ba, Sr, Rb), low Nb, and steep REE patterns. The Águas Belas ACME Laboratories in Canada. The results are shown in Table 1. granitoids show some distinctions when compared to granitoids of The Águas Belas granitoids range from metaluminous to slightly the shoshonitic association because they have low Sr contents and peraluminous, straddling the boundary with the peralkaline field have REE patterns characterized by lower (Ce/Yb)N ratios. (Fig. 3a). They plot in the fields of alkaline to highly fractionated calc- The Águas Belas granitoids exhibit a trans-alkaline and ferro- alkaline granites (Fig. 3c) in the scheme proposed by Sylvester (1989). potassic character. These features are common to most alkaline The plutonic TAS diagram (Fig. 3b), with fields after Middlemost granite suites. However, the studied granitoids show high Ba and low (1997), emphasizes the trans-alkaline character of the Águas Belas Nb and Y contents, whereas the alkaline granites have low Ba and high granitoids. They have high SiO2 (69.1–73.1 wt.%) and total alkalis, Nb and Y contents. According to Liegéois et al. (1998), alkaline with Na2O+K2O ranging from 8.3 to 10.5 wt.% and K2O/Na2O ratios granites, not peralkaline granites, show K-feldspar always dominating ranging from 1.2 to 1.9. One sample analyzed from the southern over plagioclase, i.e. they are alkali-feldspar granite and syenogranite border of the batholith shows higher K2O/Na2O ratio (2.2). They have in composition. The alkaline granites show petrography very similar A.F. da Silva Filho et al. / Gondwana Research 17 (2010) 676–687 681

Table 1 Representative geochemical and isotopic data for granites from the Águas Belas Pluton.

Sample AB-02 AB-08 AB-10 AB-11 AB-12 AB-13 AB-14 AB-15 AB-17 AB-20 AB-21 AB-22

SiO2 70.36 69.14 70.4 71.16 70.55 70.64 72.4 73.12 72.39 72.12 71.09 71.44

Al2O3 14.22 14.39 15 14.88 14.69 14.5 14.8 14.2 14.23 14.26 14.41 14.16 MnO 0.06 0.07 0.05 0.04 0.04 0.06 0.04 0.04 0.05 0.06 0.05 0.06 MgO 0.38 0.42 0.32 0.33 0.31 0.34 0.26 0.22 0.27 0.19 0.34 0.33

Fe2O3 1.07 2.99 2.24 1.99 2.16 2.28 1.51 1.63 1.77 2.12 2.19 1.6 CaO 3.73 1.15 0.67 0.76 0.7 0.96 0.84 0.87 0.85 0.88 1.0 0.87

Na2O 6.75 3.55 3.53 3.73 3.76 3.78 4.12 4.22 4.2 4.15 3.77 4.08

K2O 0.27 6.92 6.20 6.03 6.64 6.47 4.88 5.23 5.25 5.44 6.23 5.51

TiO2 0.06 0.25 0.18 0.16 0.16 0.18 0.13 0.11 0.13 0.11 0.17 0.12

P2O5 2.33 0.07 0.06 0.08 0.09 0.08 0.08 0.04 0.05 0.04 0.07 0.06 Total 100.15 99.7 99.8 99.89 99.1 99.65 99.9 99.91 99.47 99.66 99.66 98.49

Trace elements in ppm Ba 2427 2566 1968 1893 1983 1848 1500 1335 1297 1384 1757 1323 Cs nd nd nd nd 7.1 5.0 nd 5.8 4.1 5.6 4.2 4.9 Ga nd nd nd nd 19.3 19.3 nd 19.4 19.3 19.5 18.9 19.9 Hf nd 3.6 4.2 3.1 4.4 3.8 nd 3.1 3.3 3.4 3.5 3.9 Nb nd nd nd nd 8.9 9.8 nd 9.4 10.4 10.5 12.1 14.4 Rb nd 203 211 29 243 236 nd 231 224 257 258 262 Sr 664 710 592 613 569 542 490 460 458 429 558 427 Ta nd 0.2 0.7 1.0 0.7 0.7 nd 0.8 1.0 1.3 0.9 2.0 Th nd 11.1 11.1 2.7 14.1 16.7 nd 12.3 19 22.9 14.3 20 U nd 1.5 6.0 0.8 1.9 2.4 nd 2.7 3.5 4 3.6 5.1 Zr nd 159 121 106 143 127 89 87 92 101 111 93 Y nd 19 28 13 19.5 17.6 10 13.9 13 18.4 17.1 14.1 La 189 31 78.4 16.5 44.7 25.3 9.49 16.4 15.7 20.4 22.7 20.8 Ce 17 59 205 36 80.8 45.9 22 29.3 29.9 33.4 40.7 34.8 Pr nd nd nd nd 8.1 4.67 nd 3.22 3.08 4.04 4.25 3.68 Nd nd 23.1 56.2 18.0 30.2 18.4 7.0 12.1 12.3 16 17.7 13.8 Sm nd 4.09 8.94 3.95 4.6 3.2 1.58 2.3 2.3 2.6 2.9 2.4 Eu nd 1.11 2.15 1.31 1.02 0.61 0.5 0.5 0.5 0.59 0.53 0.37 Gd nd nd nd nd 3.74 2.78 nd 2.28 2.03 2.73 2.7 1.86 Tb nd nd 0.9 0.7 0.6 0.45 0.3 0.36 0.32 0.46 0.46 0.38 Dy nd nd nd nd 3.45 2.66 nd 2.36 2.06 2.8 2.8 2.12 Ho nd nd nd nd 0.6 0.53 nd 0.44 0.4 0.54 0.55 0.39 Er nd nd nd nd 1.61 1.56 nd 1.38 1.26 1.61 1.53 1.23 Tm nd nd nd nd 0.27 0.28 nd 0.24 0.22 0.28 0.26 0.2 Yb nd 1.73 2.67 2.75 1.59 1.84 0.94 1.42 1.6 1.95 1.75 1.67 Lu nd 0.26 0.37 0.41 0.27 0.28 0.15 0.24 0.27 0.34 0.31 0.29 Fe# 0.860 0.877 0.875 0.858 0.874 0.870 0.853 0.881 0.868 0.918 0.866 0.829 147Sm/144Nd 0.1211 0.1171 εNd(0) −18.29 −18.50 εNd(0.6 Ga) −12.50 −12.41

TDM (Ma) 2214 2139

# Nd=not determined. Fe2O3 =Total iron. Fe =FeOt/(FeOt+MgO).

to evolved calc-alkaline granitoids, and the distinction can be attained total rock sample (AB-08) using standard crushing, washing and on geochemical grounds. heavy liquid. Hand-picked selected zircons were placed onto double- The Águas Belas granitoids are mainly syenogranite in composi- sided tape and mounted together with chips of the reference zircons tion and, plot (Fig. 7) within the post-collisional field in the Rb versus (FC1and SL13) in epoxy resin, ground to half thickness, and polished (Y + Nb) diagram (Pearce, 1996). They have high values of Fe# with 3 µm and 1 µm diamond paste. A conductive gold-coating was (>0.8), Fe-rich and Na-rich amphiboles, REE patterns characterized applied just prior to analysis. The grains were photographed in by low (Ce/Yb)N values and high total alkalis, with Al2O3 /(Na2O+ reflected and transmitted lights, and cathodoluminescence (CL) K2O) molecular ratios ~1.0. In the Yb/Ta versus Y/Nb diagram (Fig. 8) images were produced in a scanning electron microscope in order theÁguasBelas granitoidsplot alonga trendbetweenthe OIBandIAB to investigate the internal structures of the zircon crystals, to average fields, showing trace element signature distinct from OIB- characterize different populations, and to ensure that the spot was like signature (Fig. 9). In spite of the many similarities with A2-type wholly within a single age component within the sectioned grains. granites, the studied granitoids have much lower contents of Y and The U–Th–Pb analyses were made using the SHRIMP II of the Zr, and higher Sr concentrations, when compared to those for Research School of Earth Sciences, The Australian National University, alkaline granites. The geochemical signature of the Águas Belas Canberra, Australia. Each analysis consisted of 6 scans through the granitoids favours their classification as a transitional high-K calc- mass range. SHRIMP analytical procedures followed the methods alkaline to alkaline post-collisional magmatism. described in Williams (1998, and references therein). The standard zircon SL13 (Claue-Long et al., 1995) was used to determine U 6. SHRIMP U–Pb and oxygen isotope zircon data concentration and the Pb/U ratios were normalized relative to a value equivalent to an age of 1099 for the FC1 reference zircon (Paces and 6.1. Analytical methods Miller, 1993). Raw isotopic data were reduced using the Squid program (Ludwig, 2001), and age calculations and Concordia plots SHRIMP U–Pb dating was used to determine the age of zircons were done using both Squid and Isoplot/Ex software (Ludwig, 2003). from the studied granitoids. Zircon grains were separated from the The results are listed in Table 2. 682 A.F. da Silva Filho et al. / Gondwana Research 17 (2010) 676–687

Fig. 3. a) Shand's Index for the granitoids of the Águas Belas granitoids. Fields after Maniar and Piccoli (1989); b) the studied granitoids in the TAS diagram with fields after Middlemost tot tot (1997); c) The studied granitoids are projected in the Sylvester (1989) diagram. d) The composition range of the studied granitoids in the FeO /(FeO +MgO)versusSiO2 diagram. Fields of ferroan and magnesian granitoids are from Frost et al. (2001).Thefields of RRG+CEUG (anorogenic granitoids); POG (post-orogenic granitoids) and IAG+CAG+CCG (orogenic granitoids) after Pearce et al. (1984). e) The studied granitoids plotted in the K2OversusSiO2 diagram with fields after Peccerillo and Taylor (1976).Opentriangle—syenogranites; closed triangle—enclave.

6.2. Zircon description and results Twenty three zircon grains were analyzed, totalling 26 analyzed spots. A cluster of 14 concordant analyses yields a 206Pb/228U age of The analyzed zircon crystals are pale yellow, with rare inclusions. 588±4 Ma (Fig. 11). The euhedral shape and the high Th/U ratio of They are usually elongate, prismatic, length/width ratio ranging from the grains suggest that this age must correspond to a best estimation 4:1 to 4:2 (Fig. 10), with length ranging from 100 µm up to 270 µm. All for the emplacement age of the Águas Belas pluton. of them, except the core of crystal 4 (Fig. 10), show oscillatory zoning The analyzed sample also shows inherited zircon cores that yield and many show a clear overgrowth. The contact core-overgrowth is slightly discordant 207Pb/206Pb ages (Table 2). The zircon cores yield irregular and sharp, and the core usually shows elongate shape. The ages of 1594±13 Ma, 1895±14 Ma, and 2060±23 Ma. The core of the analyzed zircons show Th/U ratios ranging from 0.2 to 0.7, which is crystal 4 (Fig. 10) yielded an age of 1594±13 Ma while the rim shows typical of magmatic zircons (Williams and Claesson, 1987). an age of 613±6 Ma. The core shows no oscillatory zoning, but the rim A.F. da Silva Filho et al. / Gondwana Research 17 (2010) 676–687 683

Fig. 4. Chondrite-normalized REE patterns (Nakamura, 1974) of the Águas Belas granitoids.

does show. Both of them show high Th/U ratios, suggesting that at least the zircon rim has igneous origin.

6.3. Oxygen isotopes

The oxygen isotope analyses were conducted using the SHRIMP II in 23 spots in the same zircon spots analyzed previously for U–Pb (Fig. 11), and results are reported in the SMOW scale. The δ18O values lie between 6.35‰ and 10.30‰. Only spot 23.2 (Table 2), with 207Pb/ 206Pb age=1315±300 Ma, shows a significantly lower δ18O value=5.79‰. Due to being highly discordant (66%) and large age error, this analyzed spot is not going to be taken under further consideration. Grain 4 shows the lowest δ18O values, 6.69‰ and 6.35‰, for core and rim respectively. Grain 11 shows 18O/16O values of 8.19‰ and 10.01‰ for the rim and core respectively. The core of zircons, spots 11.2 and 22.1, show rounded shape and high values of 18O/16O. The δ18O values for rims of Neoproterozoic age range from 6.69 to 10.30‰, with average value of 8.26±0.71‰. This >2‰ variation is large and not compatible with cogenetic rocks crystallized in a closed system. Average δ18O (zircon) value is lower (8.23±0.46‰) when the highest (10.30‰) and the lowest (6.69‰) values are not considered. In this case, considering whole rock silica contents, calculated average whole rock δ18O values, following Valley et al. (1994), vary from 10.06±

0.46‰ to 10.30±0.46‰ for SiO2 contents of 69.14% and 73.12%, respectively, the silica range observed for the Águas Belas rocks. These average values are consistent and compatible with high δ18O crustal- derived magmas crystallized in a closed system. The highest δ18O (zircon) values (10.01 and 11.01‰) from the Paleoproterozoic cores are 2–3‰ higher than the δ18O (zircon) values observed for zircons of this age studied by Valley et al. (2005), who reported that during the Proterozoic the range of δ18O (zircon) gradually increases in a secular Fig. 5. Bivariate trace element diagrams monitoring feldspar involvement in the evolution of the Águas Belas granitoids. The fractionated vectors were built using the δ18 change that documents maturation of the crust. The high O values partition coefficients from Villemant et al. (1981). of Proterozoic zircon cores of this study are compatible with high δ18O values of (meta) sedimentary rocks. The δ18O (zircon) values of Mesoproterozoic cores are lower (6.35‰ and 6.89‰) and can be interpreted as resulting from the exchange of crustal rocks and lithospheric mantle magmas. The involvement of a protoliths with surface waters at low temperature followed by melting crustal component in the Águas Belas granitoids protolith is or contamination, as suggested by Valley et al. (2005) for Archaen supported by the presence of zircon grains with Paleoproterozoic zircons that show δ18O values in the range 6.5–7.5‰. and Mesoproterozoic age and their Nd isotopic data. However, this crustal component could be incorporated to the magma, during its 7. The granitoid source and tectonic setting ascent through the crust. Mesoproterozoic zircon grains with low δ18O values were probably Values of δ18O (zircon) lower than 7‰ recorded in the 592±7 Ma inherited from igneous rock originated from a protolith involving zircon grain from the studied granitoids reflect interactions between mantle and minor crustal components. Mesoproterozoic igneous 684 A.F. da Silva Filho et al. / Gondwana Research 17 (2010) 676–687

Fig. 8. The Yb/Ta versus Y/Nb plot showing the Águas Belas granitoids plotting in between the OIB and AIB fields.

intercept of 538±34 Ma. The presence of zircons of Mesoproterozoic age within the Pernambuco–Alagoas Domain suggests that part of its crust should contain rocks with this age. The only well documented Mesoproterozoic igneous suite within the Borborema Province is the Taquaritinga orthogneisses (Sá et al., 2002), which occur within the Transverse Domain. They show a clear A-type granite character and Fig. 6. a) Multi-element chondrite-normalized plots (normalizing values from yielded U–Pb zircon age of 1521±6 Ma. The presence of zircon with Thompson, 1982) to demonstrate the essential differences between the Águas Belas 1560 Ma and mantle oxygen isotope value within the Águas Belas granitoids (a) and the average of I-type, S-type and High Ba–Sr granites (b). I-type, S- type and High Ba–Sr granites are from Tarney and Jones (1994). granitoids favours the presence of juvenile Mesoproterozoic rocks in the PEAL Domain. This hypothesis should be further investigated because there is no oscillatory zoning in this zircon. The Paleoproterozoic Nd T model age recorded in the studied fi DM rocks have not been identi ed so far within the PEAL Domain. Neves granitoids cannot support the presence of juvenile lithospheric – et al. (2008) have determined U Pb zircon age of 1560±16 Ma for the mantle in the Águas Belas granitoids protolith. The involved Cabanas pluton in the Garanhuns sub-domain, but with no clear lithosphere should have a Paleoproterozoic age otherwise. If a indication of an igneous origin for it. Van Schmus et al. (1995) had juvenile Neoproterozoic lithosphere had been involved, the εNd found migmatitic garnet-gneiss with similar age near Palmeira dos (0.60 Ga) value showed by the Águas Belas pluton would be much less Indios, yielding an upper intercept of 1577±73 Ma and lower positive than −12.4.

Fig. 7. The studied granitoids in the tectonic discriminant diagram of Pearce (1996). WPG=within plate granite; ORG=oceanic ridge granite; Syn-COLG=syn-collisional Fig. 9. Multi-element OIB-normalized plots show the geochemical distinct signatures granite; Post-COLG=post-collisional granite. between the Águas Belas granitoids and the OIB. A.F. da Silva Filho et al. / Gondwana Research 17 (2010) 676–687 685

Table 2 U–Pb and oxygen isotopic data of the sample AB-08 from the Águas Belas Pluton.

232 206 238 207 206 207 ⁎ 207 206 18 Grain. % U ppp Th Th/ ppm (1) Pb/ (1) Pb/ % Dis (1) Pb / ±% (1) Pb⁎/ ±% (1) Pb⁎/ ±% Err δ 206 238 206 206 ⁎ 235 238 spot Pbc ppm U Pb⁎ U age Pb age Pb U U corr O‰ 1.1 0.10 608 118 0.20 49.6 583.7 ±5.9 577±18 −1 0.0593 0.83 0.774 1.3 0.0948 1.1 .789 8.04 2.1 0.40 691 234 0.35 56.5 584.2 ±5.9 575±29 −2 0.0592 1.3 0.774 1.7 0.0948 1.1 .618 8.72 3.1 – 496 128 0.27 41.3 596±6.1 597±16 0 0.0598 0.75 0.799 1.3 0.0969 1.2 .820 10.30 4.1 0.24 431 138 0.33 37.0 613±6.4 548±27 –11 0.0585 1.2 0.804 1.7 0.0998 1.3 .657 6.69 4.2 0.00 149 104 0.72 35.2 1565 ±16 1594±13 2 0.0984 0.7 3.727 1.4 0.2747 1.1 .859 6.35 5.1 0.12 597 203 0.35 49.3 591.7 ±7.5 595±19 1 0.0598 0.89 0.792 1.6 0.0961 1.4 .832 8.56 6.1 0.00 671 227 0.35 56.1 598.9 ±6.1 572±16 −5 0.0591 0.74 0.794 1.3 0.0974 1.1 .820 8.35 7.1 12.16 1136 335 0.30 93.3 520.1 ±6.8 671±170 29 0.0619 8.0 0.717 8.1 0.084 2.7 .168 7.45 8.1 0.42 805 345 0.44 63.9 567.5 ±5.7 593±24 4 0.0597 1.1 0.758 1.5 0.09203 1.1 .683 7.04 9.1 0.30 654 176 0.28 47.7 524±14.0 584±23 12 0.0595 1.1 0.694 2.9 0.0847 1.8 .930 8.61 10.1 0.81 778 331 0.44 65.7 600.2 ±6.2 608±59 1 0.0601 2.7 0.809 2.9 0.0976 1.7 .368 8.44 11.1 0.29 390 102 0.27 31.7 582±10 585±29 1 0.0595 1.3 0.775 2.3 0.0945 1.1 .804 8.19 11.2 0.04 388 10 0.03 99.0 1675 ±25 1895±14 13 0.1160 0.76 4.747 1.8 0.2968 1.1 .911 10.01 12.1 0.05 560 152 0.28 46.6 595.7 ±6.1 592±17 −1 0.0597 0.77 0.796 1.3 0.0968 1.1 .811 8.67 13.1 2.06 816 243 0.31 59.0 510.8 ±5.3 618±63 21 0.0604 2.9 0.687 3.1 0.08246 1.1 .347 8.41 14.1 0.20 694 298 0.44 57.3 590.8 ±60 588±19 0 0.0596 0.9 0.788 1.4 0.096 1.1 .765 8.55 16.1 0.22 679 199 0.30 55.3 582.9 ±5.9 606±21 4 0.0601 0.96 0.784 1.4 0.0946 1.1 .741 8.74 16.2 0.38 528 210 0.41 42.8 579.9 ±60 611±29 5 0.0602 1.3 0.781 1.7 0.0941 1.2 .634 8.67 17.1 0.49 761 267 0.36 61.4 576±5.8 598±25 4 0.0599 1.2 0.771 1.6 0.09347 1.1 .671 8.26 18.1 0.04 692 365 0.55 57.8 598.2 ±7.1 572±16 −4 0.0591 0.74 0.793 1.4 0.0972 1.2 .860 8.07 19.1 0.10 330 101 0.32 27.0 586.5 ±6.3 604±26 3 0.0600 1.2 0.788 1.6 0.0953 1.1 .690 7.81 20.1 0.12 597 186 0.32 49.2 590.6 ±6.7 589±19 0 0.0596 0.9 0.788 1.5 0.0959 1.1 .796 8.27 21.1 0.14 745 225 0.31 73.3 697.8 ±7.1 1041±29 49 0.0740 1.4 1.166 1.8 0.1143 1.2 .598 6.89 22.1 0.15 241 6 0.03 73.6 1956 ±19 2060±23 5 0.1272 1.3 6.220 1.7 0.3545 1.8 .649 11.01 23.1 3.54 905 280 0.32 73.3 561.2 ±6.6 616±99 10 0.0603 4.6 0.757 4.7 0.091 1.1 .258 7.57 23.2 6.53 250 115 0.47 30.1 794±14 1315±300 66 0.0850 15 1.540 16 0.1311 1.1 .116 5.79 ⁎ Errors are 1-sigma; Pbc and Pb indicate the common and radiogenic portions, respectively. Error in standard calibration was 0.24% (not included in above errors but required when comparing data from different mounts). (1) Common Pb corrected using measured 204Pb. % Dis=% discordant.

Flat-lying foliation is dominant in the area, including metasedi- the Águas Belas pluton emplacement involved activation of E–W pre- mentary (Inhapi) and metaigneous (Venturosa) sequences. This flat- existing crustal structure by the NNE-trending Limitão–Caetés lying foliation is always cross-cut by subvertical sinistral shear zones. sinistral shear zones. The E–W-trending structure acted as a Granulitic orthogneisses from the Venturosa Sequence have U–Pb continental transform fault, and was reactivated during a high-angle zircon (TIMS) age of 642±15 Ma (Osako et al., 2006). An elongated tectonic regime, creating the necessary space for the intrusion of the E–W-trending granitic intrusion mapped in the north part of the PEAL Águas Belas pluton. A similar model has been proposed for the Domain, shows flat-lying foliation and a 206Pb/238Uweighted Donegal Batholith (Stevenson et al., 2008). These arguments are apparent mean age of 606±8 Ma (Neves et al., 2008). This age is consistent with the post-collisional geochemical signature of the interpreted as the age of the high-grade Brasiliano metamorphism Águas Belas granitoids, if it is taken into account that a high-angle and consequently the age of the flat-lying foliation. The age obtained tectonic regime occurred after the collisional process. for the Águas Belas pluton is similar to the 40Ar/39Ar ages (581±2 Ma and 591±3 Ma) recorded by Araújo et al. (2004) for the E–W- 8. Conclusions trending Belo Monte–Jeremoabo shear zone, within the Sergipano Domain, and to the U–Pb zircon age (587±8 Ma) for the beginning of All the chemical features suggest that the Águas Belas granitoids the transcurrent regime that produced the dextral E–W-trending East correspond to a transitional high-K calc-alkaline to alkaline magma- Pernambuco shear zone (Neves et al., 2008). Ages ranging from tism, emplaced during the late stage of the Brasiliano orogeny, under 630 Ma to 608 Ma determined in orthogneisses and granitoids have the control of a set of shear zone, in between the Inhapi Sequence to been used to constrain the flat-lying foliation in the Pernambuco– the north and Neoproterozoic granitoids to the south. Alagoas domain and in the Transversal Zone Domain (Guimarães The structural and geochronological data suggest that NNE–SSW- et al., 2004; Neves et al., 2005a,b; Neves et al., 2008). trending sinistral shear zones were initiated at ca 590 Ma, and The lack of penetrative ductile deformation within the Águas Belas activated E–W pre-existing structures at the current crustal level. The Pluton, and the E–W-trending of its main axis, suggests that it was not synchronicity of these shear zones allowed the dilatation needed to intensively affected by NNE strike–slip-related deformation. It also facilitate the space required to the emplacement of the Águas Belas suggests that the emplacement occurred during the early stage of the Pluton. transcurrent tectonic regime. A similar model has been proposed by The magma evolved through K-feldspar and biotite fractionation,

Neves et al. (2008) for the intrusion of the NE–SW-trending but lack of plagioclase fractionation, which increased the Na2O Cachoeirinha Pluton, which shows similar age to the Águas Belas contents in the magma promoting the later crystallization of Na-rich pluton (587±8 Ma). However, the Águas Belas pluton shows an E– amphiboles. W-trending main axis, and, as pointed out by Guimarães et al. (2004, The U–Pb SHRIMP age associated with oxygen isotopes in zircon, 2009) and Neves et al. (2008), plutons intruded along E–W geochemical and Nd isotopic data suggest that four intervening transcurrent shear zones in the Transversal Zone domain, in the components: Paleoproterozoic lithospheric mantle, Paleoproterozoic North Tectonic domain and in the northern part of the Pernambuco– crustal rocks, Neoproterozoic supracrustal sequences, and Mesopro- Alagoas domain show younger ages (~570 Ma). The presence of E–W- terozoic igneous rock were involved in the studied granitoids trending flat-lying foliation within the Pernambuco–Alagoas domain, magmas. The necessary heating for promoting fusion was probably in the Jupi orthogneisses and in quartzites from Venturosa Sequence, the Paleoproterozoic lithospheric mantle magmas, which invaded the which occur along the Garanhuns low-angle shear zone, suggest that crust through the deep-seated shear zones during the transition 686 A.F. da Silva Filho et al. / Gondwana Research 17 (2010) 676–687

Fig. 10. CL images of zircon crystals. Circles indicate the position of the U–Pb and oxygen isotope analysis listed in Table 2. between compression and extension, during the final stage of the Acknowledgments Brasiliano orogeny. During its emplacement, the magma may have interacted with Paleoproterozoic and/or Neoproterozoic supracrustal AFSF thanks CAPES for a post-doctoral scholarship (BEX 3534/07-3). rocks and, Mesoproterozoic igneous rocks. A grant from the PRONEX/FACEPE program (APQ-0479-1.07/06) made possible SHRIMP analyses at the ANU-Research School of Earth Sciences at Canberra, Australia. We are thankful to Sam Mertens and Shane Paxton for their assistance with the sample preparation. This manuscript has been improved by the constructive review of William R. Van Schmus and one anonymous reviewer from Gondwana Research.

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