Challenges in classifying I- and S-type granites: insights from the Sana and Itaoca plutons

Abstract

The Sana (Sana suite) and Itaoca (Nova Friburgo suite) granites, emplaced in the Oriental Terrane of the Ribeira Belt during the Cambrian–Ordovician, provide key insights into post-collisional magmatism in a Gondwana segment marked by crustal recycling. We present new Sm–Nd and Rb–Sr isotope data for 26 samples from both plutons, combined with petrographic information, to evaluate magma sources and the applicability of I- and S-type classification. The Sana Granite is strongly peraluminous and dominantly S-type, derived mainly from metasedimentary sources of the São Fidélis Group with minor arc-derived input, supported by isotopic evidence and rare titanite (< 1%). In contrast, the Itaoca Granite is metaluminous, titanite-rich, and consistent with I-type, reflecting melting of mafic to high-K orthogneisses of the Rio Negro Magmatic Arc. Mixing models suggest ternary contributions from arc and sedimentary reservoirs but remain exploratory due to limited Sr data for sources. Both plutons share overlapping Nd and Sr isotope fields, with initial ⁸⁷Sr/⁸⁶Sr ratios of 0.7008–0.7078 and consistently negative ε_Nd(t) (–11 to –13), highlighting isotopic convergence in the Oriental Terrane. These results show that, despite contrasting S- and I-type traits, both granites reflect hybridization and a shared tectonic framework, emphasizing the limitations of strict isotopic classification and the need for integrated petrographic approaches.

KEYWORDS:
Ribeira Belt; post-collisional magmatism; magma source mixing; Sm-Nd isotopes; Sr-Sr isotopes

1. INTRODUCTION

Granitic rocks are key indicators of crustal evolution, with their chemical and isotopic signatures reflecting the nature and interaction of crustal and mantle sources (Wu et al., 2017; Wang et al., 2019). In the Oriental Terrane of the Central Ribeira Belt, voluminous pre-, syn-, and post-collisional granitic magmatism developed between the Neoproterozoic and Ordovician (Valeriano et al., 2011, 2016). This terrane is interpreted as an arc system that evolved from an intra-oceanic setting to a primitive continental arc, comparable to the modern Japanese arc (Heilbron et al., 2017; Peixoto et al., 2017).

Post-collisional magmatism was emplaced mainly during the Cambrian–Ordovician, producing several granitic suites, including Suruí and Nova Friburgo, classically interpreted as I-type granites with a hybrid origin involving mantle- and crust-derived melts (Valeriano et al., 2011, 2016; Tupinambá et al., 2012a). Recent work, however, demonstrated that this magmatism is not exclusively I-type: Potratz et al. (2021) identified that the Sana Granite was derived primarily from partial melting of metasedimentary sources, making it representative of S-type granites.

Distinguishing metaigneous from metasedimentary sources in these plutons is challenging. Diagnostic minerals such as amphibole, cordierite, or garnet are absent in most bodies (Potratz & Valeriano, 2017; Porto Junior et al., 2018; Bione et al., 2019; Potratz et al., 2021). Additionally, compositional convergence at high SiO₂ levels (Gao et al., 2016) and the restriction of post-collisional magmatism to the Oriental Terrane, which is spatially associated with the Rio Negro Magmatic Arc (Tupinambá et al., 2012b; Heilbron et al., 2017), further complicates classification.

The Sana and Itaoca granites, focus of this study, represent contrasting examples of post-collisional magmatism in the Ribeira Belt, corresponding to S- and I-type suites, respectively (Tupinambá et al., 2012b; Potratz et al., 2021). This work aims to: provide a detailed isotopic characterization (Sm–Nd and Rb–Sr) of both plutons; evaluate possible magma sources through two- and three-component isotopic mixing models; and discuss the applicability and limitations of I- and S-type granite classification schemes when based solely on isotopic evidence.

2. GEOLOGICAL SETTING

The Ribeira Belt (Figure 1) represents the root of a complex, deeply eroded fold belt that developed in parallel to the border of the São Francisco Craton between the Neoproterozoic to the Ordovician (Heilbron et al., 2004). This belt is commonly divided into four tectonostratigraphic terranes imbricated towards NW/W (Trouw et al., 2000). From base to top, the terranes are:

Figure 1
Ribeira Belt tectonic organization and NW-SE cross-section of Central Ribeira Belt showing the tectonic-stratigraphic terranes and sutures zones. Legend: 1 – Autochthonous basement; 2 – Neoproterozoic authochtonous metasedimentary rocks; 3-6) Units of the Occidental terrane; 7) Metassedimentary rocks of the Paraíba do Sul Group; 8) Quirino Complex; Cambuci Domain (Inner Magmatic Arc System);10 – Rio Negro Magmatic Arc (Outer Magmatic Arc System); 11 – Costeiro Domain; 12 – Leucogranites; 13 – Italva Domain (Outer Magmatic Arc System); 14 – Búzios and Palmital successions; 15 –Região dos Lagos Complex. Modified from Trouw et al. (2000), Heilbron et al. (2008, 2020), and Freitas et al. (2021).

• Occidental Terrane (Figure 1) – Also called the Autochthonous domain, it is composed of the reworked margin of the São Francisco Craton, interspersed with metasedimentary rocks belonging to the Neoproterozoic passive margin (Heilbron et al., 2004).

• Central Terrane (Figure1) – Comprises a system of arcs resulting from the subduction and collision between the São Francisco and Paranapanema cratons. The Central terrane is considered the internal magmatic arc system of the Ribeira Belt (Trouw et al., 2013; Peixoto et al., 2017; Corrales et al., 2020; Heilbron et al., 2020).

• Oriental Terrane (Figure 1) – Include the Rio Negro and Serra da Prata Magmatic arcs, also known as the external magmatic arc system (Heilbron et al., 2020), in addition to syn-, late- and post-collisional granites (Valeriano et al., 2011, 2016; Tupinambá et al., 2012a; Potratz & Valeriano, 2017; Potratz et al., 2021) and metasedimentary rocks of the São Fidélis Group. The Sana and Itaoca granites intrude rocks of the Oriental Terrane, especially orthogneisses associated with the Rio Negro Magmatic Arc and paragneisses of the São Fidélis Group.

• Cabo Frio Terrane (Figure 1) - Represent a Paleoproterozoic basement composed of orthogneisses tectonically intercalated with Neoproterozoic metavolcanosedimentary successions (Schmitt et al., 2004; Machado et al., 2017). This crustal segment is considered part of the Congo Craton (Fernandes et al., 2015).

The Rio Negro Magmatic Arc extends for approximately 600 km, from the northern part of the São Paulo state to the southern part of the Espírito Santo state (Heilbron et al., 2020). This magmatic arc comprises batholiths of tonalitic to trondhjemitic composition and stocks of hornblende-gabbro and quartz diorite (Tupinambá et al., 2012b). The rocks of the Rio Negro Magmatic Arc exhibit distinct geochemical signatures associated with different geographic distributions: the low to medium-K calc-alkaline association extends from the northwestern limit of the arc to the central portion; the high-K calc-alkaline association predominates in the southwestern segment of the arc, also cropping out in the northeastern area; and the shoshonitic association is restricted to the region of Trajano de Moraes (Tupinambá et al., 2012b; Heilbron et al., 2020).

According to Tupinambá et al. (2012b), the low to medium-K calc-alkaline association comprises orthogneisses of quartz dioritic, tonalitic, granodioritic, and trondhjemitic compositions. The high-K calc-alkaline association comprises orthogneisses of granitic, granodioritic and quartz monzonitic, compositions. The shoshonitic association comprises orthogneisses of dioritic and granitic compositions. Finally, gabbro and diorite sills cut the magmatic arc assemblages (Tupinambá et al., 2012b; Heilbron et al., 2020).

The crystallization ages of the orthogneisses of the Rio Negro Magmatic Arc range from 790 to 607 Ma, with a higher occurrence of ages between 635 and 607 Ma (Tupinambá et al., 2012b; Heilbron & Machado, 2003; Peixoto et al., 2017). Tupinambá et al. (2012b) obtained Sr and Nd isotopic data indicating juvenile and more immature signatures, with ⁸⁷Sr/⁸⁶Sr ratios varying between 0.700 and 0.715 and ε_Nd(t) values ranging from -14 to +5.

In addition to the orthoderived rocks, paraderived rocks, referred to as the São Fidélis Group, occur within the magmatic arc domain. According to Fernandes et al. (2015), this unit comprises kinzigitic gneisses rich in garnet and sillimanite, impure quartzites, biotite gneisses, amphibolites, and calc-silicate rocks. Heilbron et al. (2020) describe the São Fidélis Group as representative of a back-arc basin and U-Pb ages in zircon grains for two samples of rocks of this group pointed two age peaks at 650 Ma and 690 Ma and an age peak at 1.0 Ga in one of the samples (Fernandes et al., 2015). Regarding Hf isotopic data, Fernandes et al. (2015) observed distinct sources for zircon grains younger than 700 Ma. One source is characterized by ε_Hf(t) varying from +6 to -4 with an Hf model age (T_DM) around 1.3 Ga. Another source is characterized by ε_Hf(t) < -4 and a Hf model age (T_DM) between 2.2 and 1.8 Ga.

2.1 Cambro/Ordovician magmatism in the Ribeira Belt

In the Ribeira Belt, the igneous bodies of the Cambrian/Ordovician age, located in the Oriental terrane, represent the magmatism that developed in the late- to post-collisional stage. In total, 19 bodies were identified and distributed throughout Rio de Janeiro state, especially in the south and central regions. Brief descriptions or detailed information about these plutons can be found in Mendes et al. (2002), Heilbron & Machado (2003), Eirado et al. (2006, 2007), Valeriano et al. (2011, 2016), Tupinambá et al. (2012a), Potratz & Valeriano (2017), Porto Junior et al. (2018), Bione et al. (2019), Potratz et al. (2021), Coelho et al. (2023) and references therein.

These late- to post-collisional bodies intrude the rocks of the Rio Negro Magmatic Arc and the paragneisses of the São Fidélis Group. These igneous bodies are mainly composed of isotropic granites, generally leucocratic, with varied textures and the presence of centimetric to metric microgranular mafic enclaves (MME). This magmatism developed for about 25 Ma. (510 to 485 Ma.) (Valeriano et al., 2016; Bione et al., 2019; Potratz et al., 2021). They were grouped into three suites based on their compositional, structural, geochronological, and petrogenetic characteristics (Table 1) (Valeriano et al., 2011; Tupinambá et al., 2012a; Potratz et al., 2021): Suruí; Nova Friburgo; and Sana.

Table 1
Geochronological data compilation of some of the post-collisional in the Ribeira belt.

Unit	Suite	Age (Ma)	Method	Reference
Paraty	Suruí	502 ± 7 513 ± 5	LA-ICPMS (zircon)	Coelho et al. (2023)
Pedra Branca	Suruí	513 ± 5	ID-TIMS (zircon)	Heilbron and Machado (2003)
		515 ± 7 503 ± 5 505 ± 7 516 ± 8 497 ± 4 508 ± 6	LA-ICPMS (zircon)	Moterani et al. (2020)
Suruí	Suruí	512 ± 8	LA-ICPMS (zircon)	Valeriano et al. (2011)
Mangaratiba/Mambucaba	Nova Friburgo	492 ± 15	ID-TIMS (titanite)	Machado et al. (1996)
Favela	Nova Friburgo	482 ± 6	LA-ICPMS (zircon)	Heilbron and Machado (2003)
		501 ± 4 486 ± 8	LA-ICPMS (zircon)	Moterani et al. (2020)
Andorinha	Nova Friburgo	490 ± 9	LA-ICPMS (zircon)	Valeriano et al. (2011)
Teresópolis/Frades	Nova Friburgo	481 ± 6	LA-ICPMS (zircon)	Valeriano et al. (2011)
Nova Friburgo	Nova Friburgo	489 ± 4	LA-ICPMS (titanite)	Valeriano et al. (2011)
Itaoca	Nova Friburgo	476 ± 2	ID-TIMS (monazite)	Aguiar Neto et al. (2014)
Morro do Coco	Nova Friburgo	496 ± 3	SHIRIMP (zircon)	Bione et al. (2019)
Sana	Sana	491 ± 10	LA-ICPMS (zircon)	Valeriano et al. (2011)
		480 ± 6 495 ± 4 508 ± 5 506 ± 10	LA-ICPMS (zircon)	Potratz et al. (2021)

3. MATERIALS AND METHODS

This work presents new isotopic data (Sm-Nd and Sr-Sr) for the Itaoca and Sana granites. Preliminary information on the eight samples from the Sana Granite and eighteen samples from the Itaoca Granite were presented in previous studies by Valeriano et al. (2016) and Potratz & Valeriano (2017), respectively.

3.1 Sample preparation

Samples were prepared in the Geological Sample Preparation Laboratory (LGPA) at the State University of Rio de Janeiro (UERJ). All samples were washed and oven dried. The external portions were sawed off, and the samples were manually crushed and milled in tungsten ball mills.

3.2 Isotopic analysis

The isotopic analyses of Sm-Nd and Sr-Sr were carried out at the Laboratory of Geochronology and Radiogenic Isotopes (LAGIR) at UERJ, and the methodology is described in Valeriano et al. (2008, 2009) and Aguiar Neto et al. (2023). The analytical procedure was divided into chemical sample preparation and spectrometric analysis. The chemical preparation of the samples was carried out as follows: cleaning the preparation room with positive air pressure and double air HEPA filtration; separation of an aliquot of 50 mg mixed with a solution of ¹⁴⁹Sm and ¹⁵⁰Nd tracers in Savillex^TM PFA vials in single digestion procedure; chemical digestion of the samples plus tracer with a mixture of HF 48% (6 ml) and HNO₃ 7M (0.5 ml) for two periods of 3 days followed by 2 days with HCl 6M (3 ml); primary extraction of Sr and rare earth elements (REE) using an ion exchange column filled with BIORAD® AG50W-X8 resin (100-200 mesh); secondary extraction of Nd and Sm from the REE solution using Eichrom® LN-spec resin (50-100 mesh), in a smaller column.

Isotopic analyses were carried out using thermal ionization mass spectrometer (TIMS), model TRITON – Thermo Finnigan® Multicolector. The samples were arranged in Rhenium filaments with a double mount. The analytical procedure was performed in static mode (Faraday collectors), acquiring isotopic ratios of 160 cycles for Nd, 80 for Sm, and 100 for Sr. The absolute standard error was calculated to 2 sigma, and normalization was performed with the value of the natural ratios ¹⁴⁶Nd/¹⁴⁴Nd = 0.7219, ¹⁴⁷Sm/¹⁵²Sm = 0.5608, and ⁸⁸Sr/⁸⁶Sr = 8.3752. The reliability of the data obtained is achieved through reference materials JNdi-1 and NIST SRM 987, with values following the literature cited in Aguiar Neto et al. (2023).

3.3 Data processing

Equations 1 and 2 were used to calculate the initial ⁸⁷Sr/⁸⁶Sr ratios. Equation 1 was used for the potential sources, whose ⁸⁷Rb/⁸⁶Sr values were obtained by isotope dilution. Equation 2 was applied to calculate the initial ⁸⁷Sr/⁸⁶Sr ratios for the Sana and Itaoca samples, as the ⁸⁷Rb/⁸⁶Sr ratios were not obtained by isotope dilution. Similarly, equations 3 and 4 were used to calculate the ¹⁴³Nd/¹⁴⁴Nd ratios for the crystallization ages of the Sana and Itaoca granites. Equation 3 was used for the samples whose ¹⁴⁷Sm/¹⁴⁴Nd ratio was obtained by isotope dilution. Equation 4 was used for the samples where the ¹⁴⁷Sm/¹⁴⁴Nd ratio was not obtained by isotope dilution. All samples from the Sana Granite and the set of samples from the Itaoca Granite, ranging from samples ITA-01 to ITA-09, do not have ¹⁴⁷Sm/¹⁴⁴Nd data obtained by isotope dilution. Details on the equations used can be found in Faure & Mensing (2005).

${\left(\frac{{}^{87}\text{Sr}}{{}^{86}\text{Sr}}\right)}_{\text{t}}={\left(\frac{{}^{87}\text{Sr}}{{}^{86}\text{Sr}}\right)}_{\text{M}}-\left(\frac{{}^{87}\text{Rb}}{{}^{86}\text{Sr}}\right)\ast \left(e^{\text{nt}}-1\right)$ (1)

$${\left(\frac{{}^{87}\text{Sr}}{{}^{86}\text{Sr}}\right)}_{\text{l}}={\left(\frac{{}^{87}\text{Sr}}{{}^{86}\text{Sr}}\right)}_{\text{M}}-2.89\left(\frac{\text{Rb}}{\text{Sr}}\right)\lambda \text{t}$$ (2)

${\left(\frac{{}^{143}\text{Nd}}{{}^{144}\text{Nd}}\right)}_t={\left(\frac{{}^{143}\text{Nd}}{{}^{144}\text{Nd}}\right)}_M-\left(\frac{{}^{147}\text{Sm}}{{}^{144}\text{Nd}}\right)*\left(e^{\lambda t}\text{-1}\right)$ (3)

${\left(\frac{{}^{143}\text{Nd}}{{}^{144}\text{Nd}}\right)}_1={\left(\frac{{}^{143}\text{Nd}}{{}^{144}\text{Nd}}\right)}_M-0.602\left(\frac{\text{Sm}}{\text{Nd}}\right)\lambda \text{t}$ (4)

For the mixing tests, Sm-Nd isotopic data from the Rio Negro Magmatic Arc (Tupinambá et al., 2012b), Serra da Prata Magmatic Arc (Peixoto et al., 2017), São Fidélis Group (Fernandes et al., 2015), Buzios-Palmital Sequence (Schmitt et al., 2008), and Juiz de Fora Complex (Araujo et al., 2019) were used. All ¹⁴³Nd/¹⁴⁴Nd ratios were calculated for the Sana and Itaoca granites ages and used for two- and three-component mixing tests. The mixing equations used are present in Faure & Mensing (2005).

4. RESULTS

4.1 Sana granite

The Sana Granite outcrops in Casimiro de Abreu, Nova Friburgo, Macaé, Silva Jardim, and Trajano de Moraes regions (Figure 1). This granite is intrusive in paragneisses of the São Fidélis Group and in syn-collisional granites. The Sana Granite is represented by: central batholith with approximately 270 km²; and twenty smaller stocks and tabular bodies, which crop out to the southwest and northeast of the main body (Supplementary Material – Figure S2). This unit predominantly comprises isotropic rocks, with a leucocratic to hololeucocratic color index and an inequigranular texture with grain size ranging from fine to coarse (0.1 mm to 3.0 cm) (Figure 2). The lithological variation in the Sana Granite includes alkali-feldspar granite, syenogranite, and monzogranite (Supplementary Material – Figure S3).

Figure 2
Sana Granite samples of monzogranite (A) and syenogranite (B) compositions with equigranular texture and grain size ranging from fine to medium. (C) Sample of coarse-grained Itaoca Granite with porphyritic texture. (D) Sample with porphyritic monzogranite rocks + mafic micro granular enclave + white pegmatite. (E) Monzogranite sample with inequigranular texture. (F) Xenolith of mafic rock associated to the Rio Negro Magmatic in the Itaoca Granite.

The Sana Granite is a two-mica granite, as biotite and muscovite are primary minerals. Table 2 is a summary of the mineralogical composition and textures/structures of the granite.

Table 2
Mineralogical composition and texture/structure of the collected samples.

UNIT	SAMPLE		MAIN MINERALOGY*	SECONDARY MINERALOGY	TEXTURE/STRUCTURE
Itaoca granite	Porphyritc facies	ITA-06	Quartz, plagioclase, microcline, biotite	Allanite, apatite, titanite, opaques, zircon	The rocks are isotropic, with microcline (2.0 to 5.0 cm) tabular to slightly oval phenocrysts. The matrix's grain size varies from fine to coarse.
		ITA-09		Allanite, apatite, titanite, opaques, zircon
		ITA-12		Allanite, apatite, opaques
		ITA-13		Allanite, apatite, opaques
		ITA-14		Allanite, titanite, opaques, zircon
	Inequigranular facies	ITA-01	Quartz, plagioclase, microcline, biotite	Allanite, apatite, opaques, zircon	Rocks are isotropic, hololeucocratic to leucocratic, inequigranular texture, grain sizes ranging from fine to coarse (1.0 mm to 5.0 mm).
		ITA-02		Allanite, apatite, titanite, monazite, opaques, zircon
		ITA-03		Allanite, apatite, monazite, opaques, zircon
		ITA-04		Allanite, apatite, monazite, opaques, zircon
		ITA-05		Allanite, apatite, monazite, opaques, zircon
		ITA-07		Allanite, apatite, opaques, zircon
		ITA-08		Allanite, apatite, titanite, monazite, opaques, zircon
		ITA-16		Allanite, titanite, monazite, opaques, zircon
		ITA-17		Apatite, opaques, zircon
		ITA-18	Quartz, plagioclase, microcline, biotite	Allanite, zircon, muscovite
	Enclaves	ITA-10	Quartz, plagioclase, microcline, biotite	Allanite, titanite, opaques, zircon	The rocks are isotropic, with microcline (2.0 to 5.0 cm) tabular to slightly oval phenocrysts. The matrix's grain size varies from fine to coarse.
		ITA-11
		ITA-15
	Xenolith	X-ITA-01	Horblende, plagioclase, biotite and quartzo	Opaques and apatite	The foliation of the rock is marked by the orientation of biotite and hornblende
Sana granite	Inequigranular facies	SANA-01	Quartz, microcline, biotite	Plagioclase, muscovite, zircon, allanite, opaques	Rocks are isotropic, hololeucocratic to leucocratic, inequigranular texture, and grain sizes ranging from fine to coarse (1.0 mm to 3.0 cm)
		SANA-02	Quartz, plagioclase, microcline, biotite	Muscovite, Opaques, zircon
		SANA-03	Quartz, microcline, biotite	Plagioclase, muscovite, zircon, allanite, opaques
		SANA-04	Quartz, microcline, plagioclase, biotite	Allanite, opaques, zircon
		SANA-05	Quartz, microcline, plagioclase	Biotite, muscovite, opaques, zircon
		SANA-06	Quartz, microcline, biotite	Plagioclase, muscovite, zircon, allanite, opaques
		SANA-07	Quartz, microcline, plagioclase	Muscoviete, biotite, allanite, opaques, zircon
		SANA-08	Quartz, microcline, plagioclase, muscovite	Biotite, allanite, opaques, zircon

4.2 Itaoca granite

The Itaoca Granite crops out in the Campos dos Goytacazes region, intrudes paragneisses of the São Fidélis Group and is partially covered by two types of sediments (alluvials and associated to the Barreiras Group). This granite is represented by a central body, approximately elliptical with a maximum diameter of 5 km (Supplementary Material – Figure S1). The rocks in this unit exhibit concentric textural variation (from the edges to the center of the body), where the rocks at the edges show inequigranular porphyritic texture with phenocrystals of feldspar with 6 cm of size immersed in a medium to coarse-grained matrix, and the rocks at the center of the body have equigranular texture with medium grain size. The transition between the different textures occurs gradually.

This unit comprises monzogranites, quartz-monzonites, and syenogranites (Figure 2). Microcline, plagioclase, quartz and biotite are the main minerals, while allanite, opaques, apatite, titanite, monazite, and zircon as accessory minerals. A summary of the mineralogical composition and textures/structures of the Itaoca Granite is presented in Table 2. Centimeter-sized surmicaceous enclaves, metric-sized leucocratic autoliths, decametric-sized metatonalite xenoliths, fine to medium-grained granite dykes, and pegmatites are frequently observed.

4.3 Isotopic data

Eight samples of Sana Granite, six to Sm-Nd and eight to Sr-Sr, and eighteen of Itaoca Granite were analyzed. Samples of Itaoca Granite included: fifteen granitic rocks (host rock) and three of leucocratic enclaves. Sm concentrations range from 9.2 to 26.7 ppm in the Sana Granite and from 14.3 to 24.0 ppm in the Itaoca Granite, whereas Nd contents vary between 56.9 and 187 ppm and 98.7 to 173 ppm, respectively. Initial ¹⁴³Nd/¹⁴⁴Nd_(t) ratios, calculated at 500 Ma for Sana and 476 Ma for Itaoca, range from 0.50846 to 0.50915 (Figure 3A) and from 0.50871 to 0.50938 (Figure 4A), respectively. Model ages (T_DM) cluster between 1.3 and 1.6 Ga for both granites, with consistently negative εNd_(t) values ranging from -11.4 to -13.2. The Sm-Nd isotopic data are summarized in Table 3.

Figure 3
Box plot with the isotopic ratios of ¹⁴³Nd/¹⁴⁴Nd (A) and ⁸⁷Sr/⁸⁶Sr (B) for the Sana Granite compared with data from the Rio Negro Magmatic Arc (Tupinambá et al., 2012b) and the São Fidélis Group (Fernandes et al., 2015), calculated for 500 Ma. The yellowish band of each diagram (A and B))) represents the isotopic ratios obtained for the Itaoca Granite. legend: M – Mafic rocks; MS – transition between the shoshonitc and medium-K groups; S – Shoshonitic group; MK – Medium-K group; HK – High-K group; SF – São Fidélis Group; SA – Sana Granite.

Figure 4
Box plot with the isotopic ratios of ¹⁴³Nd/¹⁴⁴Nd (A) and ⁸⁷Sr/⁸⁶Sr (B) for the Itaoca Granite compared with data from the Rio Negro Magmatic Arc (Tupinambá et al., 2012b) and the São Fidélis Group (Fernandes et al., 2015), calculated for 476 Ma. The reddish band of each diagram (A and B))) represents the isotopic ratios obtained for the Itaoca Granite. Legend: M – Mafic rocks; MS – the transition between the shoshonitc and medium-K groups. MK – Medium-K group; HK – High-K group; S – Shoshonitic group; SF – São Fidélis Group; ITA – Itaoca Granite.

Table 3
Sm-Nd isotopic data for the Sana and Itaoca granites. Concentrations of Sm and Nd are reported in ppm. Initial ¹⁴³Nd/¹⁴⁴Nd_(t) ratios were calculated at 500 Ma for the Sana Granite and 476 Ma for the Itaoca Granite. T_DM model ages are given in Ga. εNd₍₀₎ and εNd_(t) values are presented relative to CHUR.

Sample	Unit	Sm (ppm)	Nd (ppm)	1/Nd (ppm)	Age (Ma)	143Nd/144Nd	Error	143Nd/144Nd(t)	TDM (Ma)	ε Nd (0)	ε Nd (t)
SA-01	Sana	11.1	76.9	0.013	500	0.511823	5E-06	0.508921	1.4	-15.8	-12.5
SA-02	Sana	22.7	171.0	0.006	500	0.511798	9E-06	0.509129	1.4	-16.3	-12.6
SA-03	Sana	19.1	153.0	0.007	500	0.511660	2E-05	0.509150	1.5	-16.2	-12.1
SA-04	Sana	26.7	187.0	0.005	500	0.511699	6E-06	0.508828	1.6	-15.7	-12.3
SA-05	Sana	9.6	58.6	0.017	500	0.511824	2E-06	0.508530	1.6	-14.9	-12.1
SA-06	Sana	9.2	56.9	0.018	500	0.511843	7E-06	0.508592	1.5	-14.7	-12.8
SA-07	Sana	13.2	94.1	0.011	500	0.511770	7E-06	0.508949	1.5	-15.6	-11.8
SA-08	Sana	13.2	78.6	0.013	500	0.511836	9E-06	0.508459	1.6	-15.0	-11.4
ITA-01	Itaoca	18.9	140.0	0.007	476	0.511839	7E-06	0.509257	1.4	-15.6	-11.8
ITA-02	Itaoca	14.7	107.0	0.009	476	0.511869	1E-05	0.509242	1.3	-15.0	-11.4
ITA-03	Itaoca	10.0	69.0	0.014	476	0.511851	2E-06	0.509079	1.4	-15.4	-12.2
ITA-04	Itaoca	18.8	133.0	0.008	476	0.511823	3E-06	0.509119	1.4	-15.9	-12.6
ITA-05	Itaoca	21.1	166.0	0.006	476	0.511811	4E-06	0.509380	1.3	-16.1	-11.9
ITA-06	Itaoca	15.0	105.0	0.01	476	0.511831	8E-06	0.509098	1.4	-15.8	-12.5
ITA-07	Itaoca	18.0	134.0	0.007	476	0.511820	3E-06	0.509250	1.4	-16.0	-12.2
ITA-08	Itaoca	14.3	108.0	0.009	476	0.511822	3E-06	0.509289	1.4	-15.9	-12.0
ITA-09	Itaoca	21.0	155.0	0.006	476	0.511804	7E-06	0.509212	1.4	-16.3	-12.6
ITA-10	Itaoca	21.7	159.0	0.006	476	0.511820	6E-06	0.509210	1.4	-16.0	-12.3
ITA-11	Itaoca	24.0	170.0	0.006	476	0.511812	3E-06	0.509112	1.4	-16.1	-12.8
ITA-12	Itaoca	18.5	143.0	0.007	476	0.511809	6E-06	0.509335	1.4	-16.2	-12.1
ITA-13	Itaoca	14.8	105.0	0.01	476	0.511832	7E-06	0.509136	1.4	-15.7	-12.3
ITA-14	Itaoca	14.8	98.7	0.01	476	0.511874	1E-05	0.509006	1.4	-14.9	-12.1
ITA-15	Itaoca	19.9	120.0	0.008	476	0.511885	7E-06	0.508713	1.5	-14.7	-12.8
ITA-16	Itaoca	22.8	157.0	0.006	476	0.511808	2E-06	0.509030	1.4	-16.2	-13.1
ITA-17	Itaoca	23.3	173.0	0.006	476	0.511769	6E-06	0.509193	1.4	-17.0	-13.2
ITA-18	Itaoca	20.9	162.0	0.006	476	0.511793	6E-06	0.509325	1.4	-16.5	-12.4

The Rb-Sr dataset complements these results, highlighting significant differences between the two granites. The Sana Granite shows Rb/Sr ratios from 0.9 to 3.8 and ⁸⁷Sr/⁸⁶Sr_(t) values between 0.7055 and 0.7078 (Figure 3B), indicating a generally radiogenic trend. In contrast, the Itaoca Granite displays greater compositional variability, with Rb/Sr ratios between 0.4 and 2.1 and ⁸⁷Sr/⁸⁶Sr_(t) values ranging from 0.7008 to 0.7077 (Figure 4B), respectively. The Sr-Sr isotopic data are presented in Table 4.

Table 4
Rb-Sr isotopic data for the Sana and Itaoca granites. Concentrations of Rb and Sr are reported in ppm. ⁸⁷Sr/⁸⁶Sr_(t) ratios were calculated at 500 Ma for the Sana Granite and 476 Ma for the Itaoca Granite. 1/Sr values are given in ppm⁻¹. εSr values are calculated relative to CHUR.

Sample	Unit	Rb (ppm)	Sr (ppm)	Rb/Sr	1/Sr (ppm)	87Sr/86Sr	Error	Age (Ma)	87Sr/86Sr(t)	87Sr/86Sr(t,CHUR)	ε (Sr)
SA-01	Sana	274	141	1.9	0.007	0.7533	8.2E-06	500	0.7055	0.7527	-62.6
SA-02	Sana	291	181	1.6	0.006	0.7462	3.5E-06	500	0.7068	0.7456	-52.0
SA-03	Sana	280	205	1.4	0.005	0.7385	3.3E-06	500	0.7051	0.7379	-44.5
SA-04	Sana	248	280	0.9	0.004	0.7273	5.3E-06	500	0.7057	0.7267	-28.9
SA-07	Sana	240	197	1.2	0.005	0.7358	5.9E-06	500	0.7061	0.7352	-39.7
SA-08	Sana	319	85	3.8	0.012	0.8012	7.1E-06	500	0.7078	0.8006	-116.0
ITA-01	Itaoca	277	229	1.2	0.004	0.7352	8.2E-06	476	0.7070	0.7346	-37.5
ITA-02	Itaoca	302	197	1.5	0.005	0.7420	8.4E-06	476	0.7063	0.7414	-47.4
ITA-03	Itaoca	298	198	1.5	0.005	0.7427	7.8E-06	476	0.7076	0.7421	-46.5
ITA-04	Itaoca	296	191	1.5	0.005	0.7405	3.6E-06	476	0.7044	0.7399	-48.0
ITA-05	Itaoca	314	204	1.5	0.005	0.7413	2.5E-06	476	0.7054	0.7407	-47.6
ITA-06	Itaoca	329	178	1.8	0.006	0.7475	3.3E-06	476	0.7043	0.7469	-57.0
ITA-07	Itaoca	290	201	1.4	0.005	0.7405	1.0E-05	476	0.7069	0.7399	-44.6
ITA-08	Itaoca	307	203	1.5	0.005	0.7408	3.0E-06	476	0.7055	0.7402	-46.8
ITA-09	Itaoca	328	183	1.8	0.005	0.7461	1.0E-05	476	0.7043	0.7456	-55.3
ITA-10	Itaoca	228	625	0.4	0.002	0.7160	7.0E-06	476	0.7076	0.7155	-11.0
ITA-11	Itaoca	253	609	0.4	0.002	0.7173	5.0E-06	476	0.7077	0.7167	-12.6
ITA-12	Itaoca	332	249	1.3	0.004	0.7356	5.0E-06	476	0.7046	0.7350	-41.4
ITA-13	Itaoca	307	221	1.4	0.005	0.7377	4.0E-06	476	0.7053	0.7371	-43.1
ITA-14	Itaoca	315	203	1.6	0.005	0.7402	6.0E-06	476	0.7041	0.7397	-48.1
ITA-15	Itaoca	282	407	0.7	0.002	0.7225	1.0E-05	476	0.7064	0.7219	-21.4
ITA-16	Itaoca	354	178	2.0	0.006	0.7472	7.0E-06	476	0.7008	0.7466	-61.4
ITA-17	Itaoca	343	160	2.1	0.006	0.7519	1.0E-05	476	0.7018	0.7513	-65.9
ITA-18	Itaoca	338	222	1.5	0.005	0.7396	5.0E-06	476	0.7042	0.7390	-47.2

Figure 5 illustrates the variation of ⁸⁷Sr/⁸⁶Sr versus 1/Sr and ¹⁴³Nd/¹⁴⁴Nd versus 1/Nd for the Sana and Itaoca granites. Both plutons display strong linear correlations in the Sr system, with coefficients of determination (R²) of 0.9876 for Sana and 0.9863 for Itaoca, indicating robust internal isotopic consistency. In contrast, the Nd system shows moderate dispersion in the Sana Granite (R² = 0.5766) and a weak linear trend in the Itaoca Granite (R² = 0.3608), reflecting greater isotopic heterogeneity for this element, particularly in the Itaoca samples. Notably, sample SA-08 from the Sana granite plots as a clear outlier in the Sr diagram, with ⁸⁷Sr/⁸⁶Sr_(t) of 0.7078 and a Sr content of 319 ppm.

Figure 5
Binary diagrams ⁸⁷Sr/⁸⁶Sr ratios vs 1/Sr and ¹⁴³Nd/¹⁴⁴Nd ratios vs 1/Nd for the rocks of Sana and Itaoca granites. A) ⁸⁷Sr/⁸⁶Sr ratios vs 1/Sr for the rocks of Sana Granite. B) ⁸⁷Sr/⁸⁶Sr ratios vs 1/Sr for the rocks of Itaoca Granite. C) ¹⁴³Nd/¹⁴⁴Nd ratios vs 1/Nd for the rocks of Sana Granite. D) ¹⁴³Nd/¹⁴⁴Nd ratios vs 1/Nd for the rocks of Itaoca Granite. The measured isotopic ratios were used, without recalculation to initial ratios.

4.4 Isotopic mixing models

Figures 6 and 7 illustrate Nd isotopic mixing models for the Sana and Itaoca granites and Figure 8 a binary mixing model for the São Fidélis Group. For the Itaoca Granite, the selected end-members are mafic and high-K rocks of the Rio Negro Magmatic Arc and rocks of the São Fidélis Group, with proportions of 21–43%, 18–52%, and 5–61%, respectively. For the Sana Granite, the chosen end-members are the rocks of the Búzios-Palmital Sequence, high-K rocks of the Rio Negro Magmatic Arc, and the rocks of the São Fidélis Group, with estimated proportions of 6–14%, 15–66%, and 12–84%, respectively.

Figure 6
Nd isotopic mixing models for the Itaoca Granite. (A) Reference fields of potential source rocks, including the Rio Negro Magmatic Arc (Tupinambá et al., 2012b), Serra da Prata Magmatic Arc (Peixoto et al., 2017), Búzios-Palmital Sequence (Schmitt et al., 2008), Juiz de Fora Complex (Araujo et al., 2019), and São Fidélis Group (Fernandes et al., 2015). (B–E) Binary mixing tests between: (B) mafic and high-K rocks of the Rio Negro Magmatic Arc; (C) mafic rocks of the Rio Negro Magmatic Arc and Juiz de Fora Complex; (D) Serra da Prata Magmatic Arc and high-K rocks of the Rio Negro Magmatic Arc; and (E) Búzios-Palmital Sequence and high-K rocks of the Rio Negro Magmatic Arc. The three-component mixing model in (B) includes mafic rocks (end-member A), high-K rocks (end-member B) of the Rio Negro Magmatic Arc, and the São Fidélis Group (end-member C), with mixing proportions of 21–43%, 18–52%, and 5–61%, respectively.

Figure 7
Nd isotopic mixing models for the Sana Granite. (A) Reference fields of potential source rocks as in Figure 6. (B–E) Binary mixing tests between: (B) Búzios-Palmital Sequence and high-K rocks of the Rio Negro Magmatic Arc; (C) medium-K rocks of the Rio Negro Magmatic Arc and Juiz de Fora Complex; (D) Serra da Prata Magmatic Arc and high-K rocks of the Rio Negro Magmatic Arc; and (E) medium-K and high-K rocks of the Rio Negro Magmatic Arc. The three-component model in (B) incorporates the Búzios-Palmital Sequence (end-member A), high-K rocks of the Rio Negro Magmatic Arc (end-member B), and the São Fidélis Group (end-member C), with proportions of 6–14%, 15–66%, and 12–84%, respectively.

Figure 8
Binary mixing model for rocks of the São Fidélis Group, represented as a mixture of medium-K (70–90%) and high-K (10–30%) rocks of the Rio Negro Magmatic Arc.

5. DISCUSSION

The Sana and Itaoca granites are post-collisional plutons emplaced in the Oriental Terrane of the Ribeira Belt, an orogenic system that records multiple accretionary and collisional events during the Neoproterozoic to Early Paleozoic (Heilbron et al., 2020). Both granites are undeformed, emplaced at ca. 500 Ma (Sana) and ca. 480 Ma (Itaoca), and have been traditionally grouped within the Nova Friburgo Suite (Valeriano et al., 2011, 2016; Tupinambá et al., 2012a). This classification emphasized their shared geochronological and structural context and their granitic and leucocratic character. However, recent detailed studies have highlighted significant petrogenetic differences between these plutons, leading to a re-evaluation of their classification and tectonomagmatic significance (Potratz & Valeriano, 2017; Potratz et al., 2021).

The Itaoca Granite displays all the hallmarks of an I-type granite as originally defined by Chappell and White (1974). It is metaluminous to slightly peraluminous, contains biotite as the sole primary mica, includes abundant surmicaceous enclaves, and hosts accessory minerals such as titanite, allanite, and monazite (Potratz & Valeriano, 2017). In contrast, the Sana Granite is strongly peraluminous and contains both magmatic muscovite and biotite, with mineralogical and isotopic evidence for derivation from metasedimentary protoliths (Potratz et al., 2021), supporting its classification as an S-type granite.

An important observation, however, is the occurrence of titanite in the Sana Granite, albeit in amounts of less than 1%. Titanite (CaTiSiO₅) is typically abundant in I-type granites, where its stability reflects the relatively low alumina saturation index (ASI < 1.1) and availability of calcium, favoring incorporation of Ti into titanite rather than into ilmenite, rutile, or biotite (Erdmann et al., 2019; Uher et al., 2019; Chappell & White, 1992). In contrast, strongly peraluminous S-type granites (ASI > 1.1), derived from metasedimentary sources, generally lack titanite because Ti preferentially partitions into Al-rich phases such as ilmenite, rutile, or biotite/muscovite with elevated Al-Ti substitution (Brown, 2013; Broska & Kubis, 2018; Angiboust & Harlov, 2017). The presence of titanite in the Sana Granite, even in trace amounts, therefore, deviates from the expected mineralogical pattern of strongly peraluminous S-type magmas. This feature may indicate a hybrid origin involving a minor contribution from arc-derived or orthogneissic sources, consistent with isotopic mixing models (Figures 6–7), which suggest participation by rocks from the Rio Negro Magmatic Arc.

This observation also aligns with global studies, which show that titanite occurrence is a robust discriminant against source and petrogenetic conditions (Brown, 2013; Broska & Kubis, 2018; Angiboust & Harlov, 2017). The limited occurrence of titanite in the Sana Granite suggests localized zones with lower peraluminosity or Ca enrichment, where titanite crystallization was favored despite the overall sedimentary heritage of the magma. This mineralogical nuance reconciles earlier classifications, such as Tupinambá et al. (2012a), which grouped both Sana and Itaoca granites into the Nova Friburgo Suite and described them as titanite-bearing I-types. By explicitly recognizing titanite in the Sana Granite, this study strengthens the interpretation of a S-type pluton with minor I-type mineralogical contributions (titanite), reinforcing the hybrid nature inferred from isotopic evidence.

5.1 Isotopic patterns and mixing constraints

The Sr and Nd isotopic datasets provide a detailed picture of source mixing and magmatic evolution for the Sana and Itaoca granites. Correlation diagrams of ⁸⁷Sr/⁸⁶Sr versus 1/Sr and ¹⁴³Nd/¹⁴⁴Nd versus 1/Nd (Figure 5) show linear relationships in the Sr system (R² > 0.98 for both plutons), indicating closed-system behavior during crystallization and supporting the use of Sr ratios as robust source tracers. These correlations also imply binary or near-binary mixing between isotopically distinct end-members, a scenario consistent with the Nd-based models (Figures 6–8). In contrast, the Nd isotopic system exhibits greater scatter, particularly in the Itaoca Granite (R² = 0.3608), reflecting complex isotopic heterogeneity and likely open-system processes, including magma mixing and localized crustal assimilation.

The integration of petrographic and isotopic evidence reinforces the interpretation that both granites record hybrid petrogenetic processes. The Itaoca Granite exhibits metaluminous character, titanite-rich assemblage, and Nd isotopic patterns point to a dominant contribution from arc-related orthogneissic sources, whereas the Sana Granite, though strongly peraluminous and isotopically compatible with partial melting of metasedimentary protoliths, shows mineralogical and isotopic features similar to I-type granites such as the presence of titanite and intermediate ε_Nd(t) values.

5.2 Critical evaluation of model limitations

Although the isotopic mixing models provide a useful framework for interpreting the genesis of the Sana and Itaoca granites, their applicability is constrained by the absence of Sr isotopic data for several key source units, particularly the Búzios-Palmital Sequence and the São Fidélis Group. This limitation prevents joint Sr–Nd modeling and reduces the confidence of interpretations based exclusively on Nd isotopes. Consequently, the mixing diagrams shown in Figures 6 and 7 should be regarded as exploratory models, representing plausible scenarios rather than definitive reconstructions of magma sources.

This uncertainty is critical because Sr isotopes play a central role in distinguishing between I-type, S-type, and hybrid signatures, as well as in quantifying crustal versus mantle contributions. The lack of Sr data for important lithologies forces reliance on partial datasets and literature values, which may not fully capture the isotopic variability of these terranes. However, even within these constraints, the models are consistent with petrographic and mineralogical observations, such as the limited presence of titanite in the Sana Granite and the clear metaluminous character of the Itaoca Granite. These converging lines of evidence underscore that, while exploratory, the isotopic models provide valuable insight into the hybrid petrogenetic nature of these plutons and offer a solid foundation for future targeted geochemical and isotopic studies.

Sample SA-08 from the Sana Granite provides an important case study for understanding the compositional variability within this pluton. This monzogranite sample stands out in the Sr correlation diagram (Figure 5) as an outlier, with a high ⁸⁷Sr/⁸⁶Sr_(t) ratio of 0.7078 and an elevated Sr content of 319 ppm. Petrographic observations reveal a higher modal abundance of plagioclase, which likely explains the elevated Sr concentrations, as Sr preferentially partitions into plagioclase during crystallization. Its distinctive isotopic signature may also indicate localized assimilation or partial melting of Búzios-Palmital rocks, supporting the ternary mixing models (Figure 7B) that predict a minor but measurable contribution (6–14%) from this unit to the Sana Granite’s source.

5.3 Regional isotopic context

Figure 9 places the Sana and Itaoca granites in a global isotopic framework, comparing their ⁸⁷Sr/⁸⁶Sr, ¹⁴³Nd/¹⁴⁴Nd, and ε_Nd signatures with key mantle and crustal reservoirs (Rollinson & Pease, 2021). Both plutons plot near the fields defined for continental crust and overlap significantly with the Rio Negro Magmatic Arc (Tupinambá et al., 2012b) and São Fidélis metasedimentary rocks (Capistrano et al., 2017), highlighting their strong genetic link to lithologies of the Oriental Terrane.

Figure 9
⁸⁷Sr/⁸⁶Sr versus ¹⁴³Nd/¹⁴⁴Nd versus ε_Nd diagram showing reservoirs for the Itaoca and Sana granites. Fields: depleted mantle (DM), bulk silicate earth (BE), enriched mantle (EM1, EM2), high-μ (U/Pb) (HIMU), prevalent mantle (PREMA), middle ocean ridge basalts (MORB), some island arc trends, continental crust and the Rio Negro Magmatic Arc. Adapted from Rollinson & Pease (2021) and the field of the rocks of the Rio Negro Magmatic arc was obtained from Tupinambá et al. (2012b).

Similar behaviors for the Rb-Sr and Sm-Nd isotopic systems have been observed in granites in other parts of the world. Initial ⁸⁷Sr/⁸⁶Sr ratios around 0.706 were obtained for two S-type granitic suites by Flood & Shaw (1977). Jung et al. (2001) obtained ε_Nd(i) values between -3 and -7 and initial ⁸⁷Sr/⁸⁶Sr values around 0.716 for granites generated by partially melting of metasedimentary rocks in a magmatic arc environment.

Wu et al. (2021) presented initial ⁸⁷Sr/⁸⁶Sr ratios ranging from 0.704 to 0.729 and ε_Nd(i) values ranging from -3.2 to -6.1 in weakly to strongly peraluminous granites. Gholipour et al. (2022) obtained initial ⁸⁷Sr/⁸⁶Sr ratios ranging from 0.705 to 0.720 for rocks generated by partial melting at high temperatures of metagraywackes, psammites, and schists. Finally, McCulloch & Chappell (1982) highlighted that S-type granites exhibit a wide range of ⁸⁷Sr/⁸⁶Sr_(i) ratios and a narrow range of ε_Nd(i), while I-type granites show opposite behavior regarding ⁸⁷Sr/⁸⁶Sr_(i) ratios and variable values of ε_Nd(i).

Figure 10 synthesizes the Sr and Nd isotopic evolution of these units, showing that the Sana and Itaoca granites share compositional trends with the rocks of the Rio Negro Magmatic Arc and São Fidélis Group. In the Rb-Sr system, the granites display initial ⁸⁷Sr/⁸⁶Sr ratios between 0.7008 and 0.7078, clustering around values typical of the arc-related sources, while the Sm-Nd system reveals consistently negative ε_Nd(t) values, indicating the dominance of evolved crustal material. Boxplots (Figure 10E–F) illustrate that both plutons have similar ranges of ε_Nd(i), despite their contrasting petrographic and geochemical classifications, reinforcing the idea of overlapping isotopic reservoirs within the Oriental Terrane.

Figure 10
Evolution diagrams for the isotopic systems Rb-Sr and Sm-Nd, where the initial ratios were calculated from the crystallization ages of the respective granites. Figures A to B represent, respectively, the Sana and Itaoca granites, compared with the Rb-Sr data presented by Tupinambá et al. (2012b) for the Rio Negro Magmatic Arc. Figures C and D show the evolution curves of the mantle chondritic (CHUR) and depleted (DM) reservoirs with samples from the Itaoca Granite and its enclaves, based on the evolution of the mantle proposed by De Paolo (1981). Figures C and D plot the Nd data presented by Capistrano et al. (2017) for the São Fidélis Group and by Tupinambá et al. (2012b) for the Rio Negro Magmatic Arc.

Together, Figures 9 and 10 emphasize that the isotopic fields of the granites, arc lithologies, and metasedimentary sequences are tightly grouped, reflecting the restricted tectonic evolution of this portion of the Ribeira Belt, where limited external input and recycling of older crustal material produced isotopic convergence. This integrative view demonstrates that, although the Sana Granite is dominantly derived from metasedimentary protoliths and the Itaoca Granite from arc-related orthogneissic sources, their isotopic compositions reflect a common tectonic heritage rooted in the Rio Negro Magmatic Arc.

6. CONCLUSIONS

• Distinct classification with hybrid features: The Itaoca Granite is an I-type granite, metaluminous, titanite-rich, and derived largely from partial melting of mafic and high-K orthogneissic of the Rio Negro Magmatic Arc. The Sana Granite is strongly peraluminous and predominantly S-type, derived mainly from metasedimentary sources, though the occurrence of titanite (< 1%) indicates a secondary contribution from arc-derived sources.

• Inferred magmatic sources: Isotopic mixing models suggest that the Sana Granite originated primarily from partial melting of São Fidélis Group rocks, with a minor contribution from the rocks of Búzios-Palmital Sequence and orthogneisses of the Rio Negro Arc. The Itaoca Granite is interpreted as being derived mostly from partial melting of mafic and high-K orthogneisses of the Rio Negro Magmatic Arc, with variable assimilation of São Fidélis Group metasedimentary rocks.

• Our data reinforce that the Sana and Itaoca granites should not be grouped within the same magmatic suite, as they originated from distinct source rocks. The Sana Granite is interpreted as a product of partial melting of metasedimentary rocks from the São Fidélis Group, whereas the Itaoca Granite resulted from the partial melting of orthoderived rocks associated with the Rio Negro Magmatic Arc. Consequently, the Itaoca Granite is best classified within the Nova Friburgo Suite, while the Sana Granite belongs to the suite that bears its name, the Sana Suite.

• Evidence of internal heterogeneity: Sample SA-08, a monzogranite, is an outlier in correlation diagrams, with high Sr content (319 ppm) and ⁸⁷Sr/⁸⁶Sr_(t)=0.7078. Its elevated Sr is consistent with a higher modal abundance of plagioclase, while its isotopic signature may reflect localized assimilation or mixing with melts from the Búzios-Palmital Sequence, revealing intra-pluton compositional variability in the Sana Granite.

• Exploratory models and need for new data: The absence of Sr isotopic data for key source units (São Fidélis Group and Búzios-Palmital Sequence) limits the robustness of the models; therefore, the proposed mixing proportions should be treated as exploratory. New Sr isotope determinations for these potential sources are essential for validation.

• Regional isotopic convergence: Evolution diagrams show significant overlap between the fields of both granites, the Rio Negro Magmatic Arc, and the rocks of São Fidélis Group, reflecting intense crustal recycling and the restricted tectonic evolution of the Oriental Terrane.

• Tectonic significance: The Sana (S-type) and Itaoca (I-type) Granites represent contrasting products of Cambrian–Ordovician post-collisional magmatism in the Ribeira Belt. Their contrasting origins highlight the complexity of the Oriental Terrane and underscore the need for integrated isotopic, petrographic, and structural data to reconstruct post-collisional magmatism.

Supplementary Material

Supplementary material accompanies this paper.

Figure S1

Geological map of the Sana Granite with the positioning of the sample collection points.

Figure S2

QAP diagram with Sana and Itaoca granite samples.

Figure S3

Geological map of the Itaoca Granite with the positioning of the sample collection points.

This material is available as part of the online article from https://doi.org/10.1590/2317-4889e20250041

ACKNOWLEDGEMENTS

The authors would like to thank the funding agencies. Guilherme Loriato Potratz would like to thank Fundação Carlos Chagas Filho de Amparo à Pesquisa do Estado do Rio de Janeiro for his postdoctoral scholarship, process number E26-204.530/2021 and E26-204.531/2021. Claudio de Morisson Valeriano thanks FAPERJ (E-26-200.410-2023) and CNPq (PQ 310585/2021-0) for financial support and scholarships. The authors thank Amanda Lira Porto, Larissa Lago Neves and Gabriel Paravidini for their help in sample collection and petrographic description.

• Manuscript ID: BJGEO-2024-0048.R3.
• How to cite:
  Potratz, G. L., Valeriano, C. M., & Aguiar Neto, C. C. Challenges in classifying I- and S-type granites: insights from the Sana and Itaoca plutons. Braz. J. Geol. (2026), 56:e20250041. https://doi.org/10.1590/2317-4889e20250041
• Financial support:
  scholarship, process number E26-204.530/2021 and E26-204.531/2021 – FAPERJ.
• Data availability statement:
  Data is available as supplementary material to this manuscript.

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Edited by

• SCIENTIFIC EDITOR:
  Carlos H. Grohmann https://orcid.org/0000-0001-5073-5572

• ASSOCIATE EDITOR:
  Valderez Pinto Ferreira https://orcid.org/0000-0003-3220-7113

Data availability

Data is available as supplementary material to this manuscript.

Publication Dates

• Publication in this collection
  09 Feb 2026
• Date of issue
  2026

History

• Received
  20 Aug 2024
• Accepted
  10 Nov 2025