Jardim do Seridó Suite: first example of Ediacaran peraluminous magmatism in the Rio Piranhas-Seridó Domain, Borborema Province, Northeast Brazil

Peraluminous granitoids were recently mapped in the Rio Piranhas-Serido Domain, the northeastportion of the Borborema Province. These bodies occur as stock and intrusive dikes in the metapelites of the Serido Formation, constituting the Jardim do Serido Suite. This suite has two facies. The first and most expressive facies consists of a medium-grained and whitish leucocratic monzogranite with muscovite, garnet, and biotite, while the second is represented by fine-grained and greyish leucocratic granodiorites with biotite, cropping out mainly on the edges of the main body. The thermobarometric conditions for the crystallization of the monzogranites were estimated between 2-5 kbar and 690-950 oC, whereas the lithochemical data indicate a syn-collisional peraluminous signature. Neoproterozoic garnet-biotite schist xenoliths of the Serido Formation are sometimes observed partially assimilated in the main body (stock). A U-Pb zircon age of 592 ± 2 Ma obtained in the main body is considered as the crystallization age of the Jardim do Serido Suite, corroborating the proposed existence of peraluminous magmas associated with the Brasiliano Orogenesis in the Rio Piranhas-Serido Domain. The chemical and petrographic data identified this suite as fertile to that it can generate dikes of rareelements-bearing pegmatites.


Introduction
The Rio Piranhas-Seridó Domain (DPS) of the Borborema Province is marked by significant Ediacaran-Cambrian magmatism that is represented by several batholiths, stocks, and dikes. Based on the petrographic, geochemical and geochronological data, Nascimento et al. (2015) grouped the granite bodies of this domain into six suites: Shoshonitic, Porphyritic high-K Calc-Alkaline, Equigranular high-K Calc-Alkaline, Calc-Alkaline, Alkaline, and Charnockite Alkaline, characterized as metaluminous or weakly peraluminous.
Recently, Cabral Neto et al. and Souza et al. (2018) identified and mapped leucocratic granitoids bearing muscovite, garnet and biotite in the region just south of Jardim do Seridó, in Rio Grande do Norte state. These intrusive bodies comprise the first records of peraluminous Ediacaran granite-granodiorites in the DPS, located in the same tectonic-geological context of important deposits and mineral occurrences (e.g., gold, tungsten, iron, Sn, Be, Li, Ta-Nb and Ta).
This work presents the field correlations, petrographic, geochemical and geochronological data of the peraluminous Ediacaran granite-granodiorites in the DPS, discussing the possible tectonic environment in which they formed and their fertility for rare elements, such as Ta, Be, Li, Cs, Nb, and Rb.

Regional Geology
The Borborema Province covers the extensive geologicalstructural domain located in northeastern Brazil that was consolidated in the Brasiliano/Pan-African Cycle (Almeida et al. 1977(Almeida et al. , 1981Jardim de Sá et al. 1992). Its boundaries are defined by the São Francisco Craton (Archaean to In this context, the study site is located in the Brasilianoage Rio Piranhas-Seridó Domain (DPS) bordering the Picuí-João Câmara, Portalegre and Patos shear zones to the east, west, and south, respectively, while the northern boundary is covered by the Mesozoic and Cenozoic sediments of the Potiguar Basin (Figure 2).
The Shoshonitic Suite includes pyroxene-biotite gabbro/ diorites and quartz diorites, sometimes with amphibole, and U-Pb zircon ages varying from 599 to 579 Ma. In the Porphyritic high-K Calc-Alkaline Suite predominate biotite + amphibole porphyritic granites (subordinate granodiorites and quartz monzonites) with U-Pb zircon ages between 591 and 544 Ma. The Equigranular high-K Calc-Alkaline Suite is represented mainly by biotite granites (sometimes granodiorites), fine/ medium equigranular, leucocratic, colored light gray, and U-Pb zircon ages from 582 to 527 Ma (Nascimento et al. 2015 and references therein).
The main Cambrian magmatism in the region refers to the bodies and dikes of pegmatitic granites and granitic pegmatites, with columbite and monazite U-Pb ages varying from 528 to 509 Ma (Baumgartner et al. 2006). Besides being an important source of industrial minerals (e.g. muscovite, K-feldspar, kaolinite, and quartz), most of these pegmatites are enriched with rare elements.
According to Jardim de Sá (1994), at least three important deformation events are recorded in the DPS. According to this author, the first event marked by gneiss-migmatite bands restricted to the basement rocks could have occurred in the Paleoproterozoic, reaching the amphibolite facies. The second phase is characterized by compression shear zones of dextral kinematics and isoclinal folds, inverted and recumbent, which originated a low angle S 2 foliation associated with metamorphism of green shale to amphibolite facies. This second deformation phase would have occurred during the Brasiliano Cycle. Transcurrent (dextral and sinistral) and transtensional shear zones, as well as isoclinal folds, mark the third deformation phase in the Jardim de Sá (1994) model, which is more widespread and marked by the refolding of the structures generated in the second deformation phase. The interference generates a NE-NNE trending coaxial refolding pattern. The metamorphism from greenschist facies to amphibolite is similar to that of the second deformation phase.

Local Geology
In this work, we refer to the Jardim do Seridó Suite (GJS), according to Cabral Neto et al. (2018), as consisting of a semicircular granitic stock with about 2 km 2 (GJS), associated with other smaller bodies and dikes that crop out 1 km south of Jardim do Seridó town, being intrusive in the garnet-biotite schists of the Seridó Formation ( Figure 3). These porphyro-lepidoblastic shales (garnet porphyroblasts varying from millimetric to 1.0 cm, Figure 4) are grayish colored with medium grain while some portions have a higher amount of quartz and plagioclase, providing a gneissic aspect to the rock. Its essential minerals are quartz (20-50%), plagioclase (5-20%), biotite (15-35%), and garnet (5-8%). Opaque minerals, zircon, apatite, tourmaline, muscovite and chlorite occur as accessories/traces (<3%). Quartz crystals are xenomorphic, elongated, oriented, and commonly exhibit undulating extinction. The oligoclase-type plagioclase occurs as xenomorphic crystals, oriented and altered to sericite sometimes. The oriented biotite crystals are lamellar, exhibiting brownish pleochroism and zircon and/or apatite inclusions. The octahedral garnet is hypidiomorphic to idiomorphic, showing atoll and poikiloblastic textures, with inclusions of quartz and opaque minerals. Its growth is late or postdates the main foliation (S 3 ). This foliation in the schists is quite evident and defined by the alignment of the biotite crystals and the stretching of the quartz crystals and venules. This structure is truncated by the bodies of the Jardim do Seridó Suite.
The Jardim do Seridó Suite generally crops out as large slabs ( Figure 5A), dikes or blocks/boulders ( Figure 5B). Two facies were identified here in the GJS. The main one consists of whitish leucocratic, medium-grained monzogranites, bearing muscovite, garnet and biotite ( Figure 6A). The rare opaque minerals observed are magnetite and chalcopyrite/ pyrite.
Subordinate facies emerge in restricted areas, mainly at the edges of the main body (or near them, Figure 3) or as intrusive narrowbodies in the metapelites of the Seridó Formation, being represented by greyish biotite granodiorites, leucocratic, and fine-grained ( Figure 6B).
Planar foliations lacking tectonic effects and indicative of magmatic flow (Figure 7), evidenced by the alignment of biotite crystals and feldspars, are features commonly observed in the main facies of the GJS.
In some outcrops, gradations were observed between the GJS medium grained facies and pegmatite portions ( Figure  8A), as well as the capture of pegmatite phenocrysts by the GJS monzogranitic facies ( Figure 8B). Some field features evidence the intrusive relationship of the bodies of this suite in the metapelites of the Seridó Formation, such as: GJS dikes in the metapelites ( Figure 5B) and the presence of garnet-biotite schist xenoliths (Seridó Formation) in GJS ( Figure 9A) and partially assimilated, sometimes ( Figure 9B).
The GJS intrusion relationship in the metapelites of the Seridó Formation is locally affected by pegmatite dikes that intrude both lithotypes (schists and granites), as highlighted in Figure 10.

Materials and methods
The lithochemical study was carried out from five analyses of the main facies (monzogranitic) of the GJS. The following methods were used: (i) X-ray fluorescence after dissolution with lithium metaborate or determining major elements and loss on ignition; (ii) ICP-MS after lithium metaborate fusion for determining trace and rare earth elements, and multi-acid digestion (HCl, HNO 3 , HF and HClO 4 ) for trace elements; and (iii) specific ion for fluorine. The samples were prepared and analyzed in the SGS Geosol Laboratórios Ltda. Total iron is reported as Fe 2 O 3 .  Sá and Salim (1980), Jardim de Sá (1984, 1994, Medeiros et al. (2017), Costa and Dantas (2014), and .        A fresh and homogeneous sample of the monzogranitic facies was collected and used for the U-Pb zircon dating. The zircon crystals were prepared in the Grinding Laboratory of the Department of Geology of the Universidade Federal do Rio Grande do Norte, starting by crushing and wet sieving (˂500μ) the samples to separate and concentrate the heavy minerals (batting). After drying, the material went through the Frantz Magnetic Separator where the zircon grains were separated manually using a binocular loupe and analyzed in the Geochronology Laboratory of the Universidade de Brasília. The mounts were prepared, and the equipment used according to the methodology described by Cavalcante et al. (2018) and the procedures presented by Bühn et al. (2009). Further details on the adopted dating method can be obtained in Cavalcante et al. (2018). The ages were calculated and the corresponding graphs were plotted using the resources of the ISOPLOT 3.0 Ludwig (2003).

Petrography
Two facies were identified in the GJS. The first one is the most expressive and is described in detail below. The second facies consists of greyish, leucocratic biotite-bearing granodiorite of equigranular and fine phaneritic texture. The essential minerals are plagioclase (40%), quartz (33%), K-feldspar (17%) and biotite (9%) whereas muscovite, opaque minerals, apatite, epidote, and zircon occur as accessories (1%). The feldspar crystals are commonly saussuritized.
The microcline (0.4-5.0 mm) occurs as idiomorphic to subordinate hypidiomorphic crystals, presenting a myrmekitic texture of the bulbous type at the plagioclase contact ( Figure  11A), with inclusions of biotite, epidote I, zircon, apatite, quartz, muscovite I and opaque minerals. Muscovite II and saussurite crystals are the alteration products of this feldspar.
Quartz (0.1-2.4 mm) appears as xenomorphic to hypidiomorphic crystals with a commonly weak undulose extinction while elongated crystals with subgrains and recrystallized edges occur rarely. Quartz crystals can occur included in feldspars and garnet or having inclusions of zircon, biotite, apatite, opaque minerals and/or titanite.
Plagioclase (0.3-4.0 mm) of the oligoclase type (An 23-25 ) occurs as idiomorphic to hypidiomorphic crystals, having straight contacts with the microcline and biotite crystals. Inclusions of biotite, muscovite I, apatite, opaque minerals, zircon and/or titanite may be present whereas epidote II, muscovite II and calcite are the alteration products observed in this feldspar.
Muscovite I (0.3-3.5 mm) occurs as idiomorphic to hypidiomorphic crystals, elongated, lamellar, perfectly cleaved, situated in intergranular spaces ( Figures 11B, C,  D). It is observed dispersed and associated with biotite, in intergrowths with quartz (sharp and serrated contacts) and feldspar, which may contain zircon and/or quartz inclusions.
Garnet (1.0-5.0 mm) appears as idiomorphic to hypidiomorphic crystals, commonly with inclusions of quartz and feldspars (poikilitic texture), corroded edges, fractures and skeletal texture ( Figure 11D) that may show contacts with quartz and feldspars varying from curved to straight.
The biotite (0.2-2.0 mm) is mostly present as idiomorphic to hypidiomorphic crystals with straight to serrated contacts with quartz and feldspar, where it is commonly included. It may contain inclusions of opaque minerals, zircon and/ or apatite and sometimes occurs associated with chlorite, muscovite and allanite.
The titanite (0.5 mm) is hypidiomorphic, showing straight contacts with quartz and plagioclase, being included in these minerals. Epidote I (0.05-0.10 mm) is xenomorphic to hypidiomorphic, occurs included in quartz, feldspars, and biotite and, sometimes, bordering allanite (crown texture). The allanite is mostly hypidiomorphic, with crystals smaller than 0.1 mm and crowned by epidotes. Opaque minerals (0.1-0.2 mm) are crystalline to xenomorphic crystals appearing in quadratic or elongated sections, occurring dispersed in the matrix and rarely associated with biotite. They appear included in quartz, feldspar, and biotite. Apatite (0.1 mm) occurs as ovoid or prismatic crystals included in quartz, feldspars, and biotite. Zircon (<0.25 mm) occurs as idiomorphic to hypidiomorphic crystals, prismatic, sometimes zoned and rounded, and included in quartz, feldspar, biotite, and muscovite I.
The secondary minerals (0.1-0.4 mm) are usually xenomorphic to hypidiomorphic and represented mainly by muscovite II, epidote II and chlorite, of which the first two are associated with the alteration of plagioclase and the third, of biotite.
The crystallization of the magma for this facies ( Figure  12) began with the formation of crystals of zircon, apatite and opaque minerals, while allanite, epidote I and titanite, are probably also of this phase, followed by the crystallization of biotite and muscovite I. In the sequence, feldspars and quartz were formed, followed by garnet. Epidote II, calcite, muscovite II, chlorite, and myrmekite represent the subsolidus phase.

Crystallization conditions
The crystallization conditions were estimated based on the crystallization pressure, liquidus and solidus temperatures and oxygen fugacity (fO 2 ) from the CIPW normative data and total rock analysis of SiO 2 and P 2 O 5 .
The titanite + magnetite + quartz paragenesis, observed in thin section, indicates moderate to high fO 2 conditions above the FMQ buffer, according to Wones (1989). The late-magmatic processes are marked mainly by volatile-rich fluids (CO 2 , H 2 O, and O 2 ), denoted by the carbonatization of plagioclase, myrmekitic texture, chloritization of biotite and saussuritization of plagioclase.
The pressures estimated based on the normative diagram of Tuttle and Bowen (1958) vary from 2 to 5 kbar ( Figure 13). When plotted in the Harrison and Watson (1984) diagram, most samples occupy a field near the 800°C isotherm and only one sample plots in the vicinity of the 950°C isotherm. Early crystallization of apatite indicates that such temperatures are close to the liquidus ( Figure 14A). The temperature estimated based on the normative diagram of Luth et al. (1964) shows values between 690-710ºC, attributed to the solidus temperature ( Figure 14B).
Despite the narrow variation range of SiO 2 values and the small number of analyses, the results suggest possible correlations, positive for silica with Na 2 O, Rb and Y; and negative for silica with Al 2 O 3 , Fe 2 O 3 , TiO 2 , K 2 O, Sr, Ba, Th, Nb, and Zr (Figures not included).
Using the alumina saturation index, the samples plotted in the weakly peraluminous field ( Figure 15A and 15B), consistent with Sylvester (1989) classification, showing affinity with strongly fractionated alkali-to-alkali granitic rocks ( Figure  16). However, the samples are predominantly calc-alkaline using the classification of Frost et al. (2001), ( Figure 15B).    The analytical data on rare earth elements (REE, Table  2) were normalized for chondrite according to Evensen et al. (1978). The summation values oscillate between 47.71-128.93 ppm, averaging about 91.21 ppm, probably indicating an impoverishment trend of the total REE content from the increasing SiO 2 content (Table 2). In general, the fractionation pattern has negative slope between La and Lu (La/Yb)N = 1.81-6.47, where the light rare earth elements (LREE) display a fractionated and slightly convex characteristic (La/Sm)N = 2.88-4.92, but the heavy rare earth elements (HREE) have sub-horizontal and smooth concave distribution (Gd/Yb)N = 0.55-1.03. The lower Ce and Lu values observed in two samples ( Figure 17) can be attributed to the probable incipient alteration processes associated with the microfractures observed in thin section.
The Eu/Eu* ratios vary from 0.29 to 0.40, revealing pronounced negative anomalies that may be related to the greater plagioclase fractionation during the magma evolution that generated the rocks of this granite stock or the partial melting of continental crustal sources at low pressures.  FIGURE 17 -REE diagram for the monzogranitic facies with normalizing factors according to Evensen et al. (1978). The GJS samples were plotted in discriminant diagrams of tectonic environment. In the discriminant diagrams of Pearce et al. (1984) and Thiéblemont and Cabanis (1990), the granites show affinities with rocks from syn-collisional environments (Figures 18, 19).

U-Pb zircon dating
A monzogranite sample containing biotite, muscovite and garnet was collected from the outcrop FV-125 for U-Pb zircon dating (Figure 20). The analyzed zircon crystals are generally clear, free of fractures or rims intergrowth, prismatic and elongated, about 150-200 μm long (length/width = 2.5 to 4.5). They are euhedral and usually present zoning parallel to the crystal faces (igneous). Some crystals, however, present small (10-20 μm) circular or ovoid inclusions (among them monazite), fractures and areas with dark spots (percolation of fluids). For more precise results, the analyses were preferably performed in clean areas, without inclusions ( Figure 21A). Despite this, the data of nine crystals were discarded due to high analytical error (1sigma) or common lead content (both greater than> 3%).
This cut-off criterion allowed the data of 26 crystals that are distributed in two populations. The first group is very discordant and dispersed (Table 3, crystals 4, 6, 14, 18, 19, 23, 26, 29,2, 30 and 33), a dispersion that may have been caused by mixing the zircon composition with not obseved inclusions (submicroscopic and/or in depth). The other group is more concordant and presents 206 Pb/ 238 U apparent ages between 577 and 625 Ma, which were calculated using a coherent group of points for which the 206 Pb/ 238 U and 207 Pb/ 235 U age discordance are lower than 1%. This filter allowed five data (crystals 10, 17, 20, 24, 25) that indicated the concordia age of 592 ± 2 Ma ( Figure 21B), associated with MSWD of 2.8, interpreted as the best estimate for the crystallization age of the monzogranite of the Jardim do Seridó stock. Selway et al. (2005) define fertile granite as a parental granite of pegmatite dikes mineralized to rare elements commonly presenting: (i) high silica content (> 69% SiO 2 ); (ii) Al 2 O 3 /CaO + Na 2 O + K 2 O ratio> 1 (peraluminous); (iii) muscovite, garnet, tourmaline, apatite, cordierite, andalusite and/or topaz; (iv) low Fe, Mg and Ca contents; (v) enrichment in rare elements (Li, Ta, Cs, Ga, Nb, Rb and/or Sn), generally greater than three times the average value of the upper continental crust (Table 4); (vi) K/Rb and K/Cs ratios lower Additionally, these rocks are enriched in Be, Li, Nb, Rb, and Ta, with values greater than three times the average upper continental crust and comparable to those of fertile leucogranites (Table 4). The Nb and Ta levels in these monzogranites are, in general, substantially higher than in fertile leucogranites. Cerný and Meintzer (1988) and Cerný (1989), based on chemical analyses of total rock of granites, used elemental ratios to characterize the fertile suite. Table 5 presents the GJS values for some of these ratios.

Discussion about the GJS fertility
The K/Rb and K/Cs ratios in the GJS monzogranite vary respectively from 91 to 121 and from 2550 to 6250 (Table 5), being well below the mean values of the upper continental crust and within the range of fertile granites ( Figures 22A,  B). The K/Ba (80-403) and Rb/Sr (3-15) ratios (Table 5) are within the ranges of 48 -18,200 and 1.6-185 for fertile granites ( Figures 22C, D), respectively, according to Cerný (1989). Four samples presented Mg/Li ratio values below 10 (Table 5), thus being within the range of 1.7-50 ( Figure 22E) characteristic of fertile granites according to Cerný (1989). The Nb/Ta ratio of all analyzed samples are within the compositional range of fertile granites (0.1-12, according to Cerný and Meintzer 1988), three of them having values equal to or lower than 8 for this ratio (Table 5 and Figure 22F), indicating high fertility. Peraluminous granitoids with similar ratios were characterized as fertile and possible source of pegmatites mineralized to rare elements in the Eastern Pegmatitic Province of Brazil (Médio Jequitinhonha region), in Minas Gerais (Paes et al. 2016).

Conclusions
Two facies were recognized in the GJS. The dominant facies consists of a whitish, leucocratic, medium-grained, phaneritic, equigranular to inequigranular monzogranite containing muscovite, garnet and biotite. The less expressive facies consists of a greyish-colored, fine-grained, phaneritic, equigranular biotite-bearing leucocratic granodiorite.   (Cerný and Meintzer 1988;Cerný 1989) and the mean values of the K/Rb and K/Cs ratios of the upper continental crust in dashed thick line, according to Taylor and McLennan (1985).
The estimated pressures for the monzogranite samples based on the normative quartz-albite-orthoclase composition vary from 2 to 5 kbar, while crystallization temperatures ranged from 690 (solidus) to 950ºC (liquidus).
The monzogranite lithochemical data indicate that these rocks have a peraluminous signature, a fact that is corroborated by the muscovite and garnet paragenesis, while the tectonic setting diagrams suggest that these rocks are syn-collisional.
The 592 Ma age obtained for the GJS allowed to define an Ediacaran age and, consequently, to record the existence of a peraluminous suite associated with the Brasiliano Orogenesis in the Rio Piranhas-Seridó Domain of the Borborema Province.
Altogether the analysis of the GJS characteristics allows characterizing it as a fertile granite, i.e., a granite capable of generating pegmatites mineralized to rare elements. of the Universidade de Brasilia for their support in the sample preparation and the acquisition of analytical results, as well as to the reviewers for their suggestions, which greatly contributed to the improvement of this manuscript.