Rhyacian magmatic arc rocks with sanukitoid geochemical signature from the Juiz de Fora Complex, Minas-Bahia Orogenic System (SE-Brazil)

Abstract

Sanukitoid rocks make up a complete magmatic series with distinct geochemical characteristics of TTG suites and granitoids from modern magmatic arcs and are regarded as markers of the transition from typically Archean geodynamics to modern plate tectonics. Although most known sanukitoid suites formed during the Neoarchean and Mesoarchean, numerous papers have characterized Paleoproterozoic magmatic arc granitoid rocks showing affinity with the sanukitoid series. This work presents new data from field, lithogeochemistry, zircon U-Pb geochronology, and Sm-Nd and Sr isotopic studies on granodioritic granulites with sanukitoid signatures from the Juiz de Fora Complex (JFC), one of the Paleoproterozoic tectonic components of the Minas-Bahia Orogenic System (MBOS), southern São Francisco Paleocontinent (southeastern Brazil). These rocks crystallized at ~2175 Ma and present values of εNd_t between −4.0 and +0.5, T_DM between 2.57 and 2.12 Ga, and ⁸⁷Sr/⁸⁶Sr_i between 0.6937 and 0.7137. We interpret these rocks as the result of crystallization of magmas from a hybrid mantle source extensively contaminated by crustal material during protracted subduction. In southeastern São Francisco Paleocontinent, the association of sanukitoid rocks with other magmatic arc rocks points to a complex and prolonged Rhyacian accretionary system similar to modern plate tectonics.

Keywords:
sanukitoid rocks; granodioritic granulites; zircon U-Pb geochronology; Sm-Nd and Sr isotopes; Rhyacian

INTRODUCTION

The growth of continental masses throughout the Earth’s history occurred through the addition of mantle-derived magma to the continental crust (Cawood et al. 2009, Niu and O’Hara 2009, Hawkesworth et al. 2010). Conditioned by global tectonic evolution, such magmatism gave rise to three principal products, namely the typical Archean tonalite-trondhjemite-granodiorite associations (TTG; Condie 2005, Martin et al. 2005, Moyen and Martin 2012, Laurent et al. 2014, Moyen and Laurent 2018), the modern basalt-andesite-dacite-rhyolite association (the BADR suites; Foley et al. 2002, Martin et al. 2010), and the sanukitoid rocks, a subordinate component, with chemical and isotopic characteristics distinct from TTG and BADR suites (Stern et al. 1989, Stern and Hanson 1991, Martin et al. 2005, 2010, Heilimo et al. 2010, Laurent et al. 2013, 2014).

The sanukitoid rocks make up a magmatic series that includes rocks of intermediate to acidic composition, high Sr, Ba, Ni, Cr, and MgO, high Mg#, high (La/Yb)_N, moderate to low Na₂O/K₂O ratios, and high enrichment in light rare earth elements (LREE) (Stern et al. 1989, Stern and Hanson 1991, Martin et al. 2005, 2010, Heilimo et al. 2010, Laurent et al. 2013, 2014). It is understood that sanukitoids were generated from the partial melting of peridotite mantle rocks that were previously enriched by the incorporation or addition of fluids or melts from subducted hydrated metabasaltic crust (Stern et al. 1989, Stern and Hanson 1991, Martin et al. 2010, Laurent et al. 2013, 2014, Semprich et al. 2015). In that context, these rocks have been interpreted as representing the transition from typical Archean geodynamics to Paleoproterozoic modern plate tectonics (Martin et al. 2005, 2010, Heilimo et al. 2010, Bruno et al. 2020). Although most of the known sanukitoid suites were formed in the Neoarchean and Mesoarchean (e.g., Oliveira et al. 2009, 2010, Martin et al. 2010, Heilimo et al. 2010, Laurent et al. 2014, Sun et al. 2020, Valeriano et al. 2022), numerous works have characterized Proterozoic and Phanerozoic magmatic arc granitoid rocks with affinity with the sanukitoid series (e.g., Fowler and Rollinson 2012, Seixas et al. 2013, Moreira et al. 2018, Bruno et al. 2020, 2021b, Raza et al. 2021, Zhang et al. 2021). Therefore, the investigation of sanukitoid rocks has direct implications for a better understanding of when and how stable and long-lived subduction settings.

The southeastern region of Brazil records a complex geotectonic evolution involving the accretion and collage of several crustal terranes/blocks during at least two orogenic events: the Paleoproterozoic of the Minas-Bahia Orogenic System (MBOS), culminating with the formation of the São Francisco Paleocontinent (Heilbron et al. 2010, 2017, Alkmim and Teixeira 2017, Degler et al. 2018, Bruno et al. 2020, 2021a, 2021b); and the Neoproterozoic Brasiliano/Pan-African orogenies that resulted in the amalgamation of the Western Gondwana (Pedrosa-Soares et al. 2001, Noce et al. 2007, Tupinambá et al. 2012, Heilbron et al. 2017, 2020a, 2020b, Caxito et al. 2022). The Brasiliano orogenic event reworked the margins of the São Francisco Paleocontinent and was responsible for the inversion of Mesoproterozoic to Neoproterozoic sedimentary basins and the generation of widespread pre-, syn-, late-, and post-collisional magmatic suites (Heilbron et al. 2010, 2020a). Thus, the preserved regional structure is complex, with Paleoproterozoic basement inliers (e.g., Juiz de Fora and Mantiqueira complexes), tectonically juxtaposed with Neoproterozoic supracrustal units (e.g., Raposos/Andrelândia Group; Paciullo et al. 2000, Heilbron et al. 2020a), both metamorphosed up to granulite facies and intruded by multiple Brasiliano granitoid rocks (Heilbron et al. 2010, 2017, 2020a, 2020b).

The Juiz de Fora Complex (JFC) comprises granitoid rocks metamorphosed under granulite facies with a wide compositional variation, which are interpreted to have been formed in an intraoceanic magmatic arc environment during the Siderian (Duarte et al. 1997, 2000, Heilbron et al. 1998, 2010, 2013, Degler et al. 2018, Araújo et al. 2021), with isotopic evidence of Mesoarchean crust reworking (Almeida et al. 2022). The JFC rocks were agglutinated along with the other components of the MBOS during the formation of the São Francisco Paleocontinent during the early Orosirian and were intensively reworked during the Neoproterozoic by the Brasiliano/Pan-African orogeny (Heilbron et al. 2010, 2017, Alkmim and Teixeira 2017, Araújo et al. 2021, Almeida et al. 2022). Considering that the JFC has ca. 400 km in length, the present work focuses on its northern segment. Combining Sm-Nd and Sr isotopes, together with whole-rock geochemistry, petrography, and field observations, magmatic arc rocks with sanukitoid signatures were characterized, and their ages were determined by U-Pb geochronology. The new data are compared with a compilation of other Paleoproterozoic sanukitoid suites from the southern Brazil, which allowed important insights regarding the petrogenesis of sanukitoid rocks and the geodynamic evolution of the São Francisco Paleocontinent.

TECTONIC FRAMEWORK

The São Francisco Paleocontinent

The São Francisco Paleocontinent is the precursor of the present São Francisco Craton, cropping out in the southeastern and northeastern regions of Brazil (Fig. 1A). It was agglutinated from the collage of several Archean crustal blocks (e.g., Gavião, Jequié, Piedade, Belo Horizonte, and Bonfin) during the Paleoproterozoic, with the formation of several orogenic belts (such as the MBOS) during the Siderian and Orosirian periods (Fig. 1B; Teixeira et al. 2015, 2017, Alkmim and Teixeira 2017, Barbosa and Barbosa 2017). During the development of the Neoproterozoic Brasiliano/Pan-African orogenic system, the São Francisco Paleocontinent had its margins variably reworked (Fig. 1B). Some of its constituents, such as the JFC, the Guanhães Block, and the Mantiqueira Complex, crop out as reworked inliers within the Neoproterozoic orogens (Heilbron et al. 1998, 2010, Silva et al. 2002, Noce et al. 2007, Novo et al. 2011, Degler et al. 2018, Araújo et al. 2021, Grochowski et al. 2021, Almeida et al. 2022). This Paleoproterozoic orogenic system is preserved in two sectors of the São Francisco Craton: one to the north, in Bahia state (the Bahia Segment), and the other one to further south, in Minas Gerais state (the Minas Segment of the MBOS; Fig. 1B).

Figure 1.
Tectonic framework of the São Francisco Paleocontinent: (A) Geological compartments of Brazil (modified from Heilbron et al. 2017) and (B) Archean blocks and Paleoproterozoic magmatic arcs of the Minas-Bahia Orogenic System in the São Francisco Paleocontinent (modified from Alkmim and Teixeira 2017, Barbosa and Barbosa 2017, Degler et al. 2018, Bersan et al. 2020, Bruno et al. 2021b).

In the southernmost sector of the São Francisco Paleocontinent, Archean blocks are bounded by Siderian-Rhyacian-Orosirian orogenic belts in the Minas Segment of the MBOS (Ávila et al. 2010, 2014, Seixas et al. 2013, Barbosa et al. 2015, Teixeira et al. 2015, 2017, Alkmim and Teixeira 2017, Moreira et al. 2018, Bruno et al. 2020, 2021a, 2021b). The Archean exposures are represented by greenstone belt remnants (Pimhuí, Rio das Velhas, and Pitangui) and several metamorphic complexes (e.g., Bonfim, Belo Horizonte, Campo Belo, and Piedade complexes) comprising gneisses, migmatites, and granitoid rocks. These crustal complexes/blocks acquired stability by the late-Neoarchean, establishing the core of the São Francisco Paleocontinent, which was further amalgamated with other Archean blocks (Piedade and others) between the Siderian and Early Orosirian, resulting in the formation of the Minas segment of the MBOS (Barbosa et al. 2015, Teixeira et al. 2015, 2017, Alkmim and Teixeira 2017, Bruno et al. 2020, 2021b).

The Minas Segment of the MBOS

The Minas segment comprises the Mineiro Belt and the Mantiqueira and Juiz de Fora complexes. The Mineiro Belt, with TTG suites, sanukitoid and granitoid rocks, diorites, gabbros, and supracrustal sequences, corresponds to juvenile to mature magmatic arcs built between 2.45 and 2.10 Ga, resulting from the westward accretion of the Piedade Block to the core of the São Francisco Paleocontinent (Fig. 1B; Noce et al. 2000, Ávila et al. 2010, 2014, Barbosa et al. 2015, Seixas et al. 2012, 2013, Teixeira et al. 2015, 2017, Alkmim and Teixeira 2017, Moreira et al. 2018, Bruno et al. 2020, 2021b).

To the east of the Piedade Block, the Mantiqueira Complex comprises TTG suites and biotite-hornblende gneisses with continental to mantle-derived signatures. They were intruded by late to post-collisional basic rocks (Duarte et al. 2004, Teixeira et al. 2017, Bruno et al. 2020). The Mantiqueira Complex has been interpreted as a reworked Archean microcontinent accreted to the Piedade Block between 2.10 and 2.00 Ga, and reworked during the Neoproterozoic as a result of the development of the Araçuaí-Ribeira Orogenic System (Duarte et al. 2004, Noce et al. 2007, Heilbron et al. 2010, Degler et al. 2018, Kuribara et al. 2019, Cutts et al. 2020, Bruno et al. 2020, 2021a, 2021b).

The Juiz de Fora Complex

The JFC orthogranulites protoliths comprise magmatic arc calc-alkaline granitoid rocks, TTG, and sanukitoid suites, associated with mafic rocks of different geochemical signatures (mid-oceanic ridge basalt [MORB], island arc tholeiite [IAT], and post-collision alkaline basalts) with crystallization ages ranging from 2.40 to 1.90 Ga (Table 1; Heilbron et al. 1998, 2010, 2013, Silva et al. 2002, André et al. 2009, Degler et al. 2018, Araújo et al. 2019, 2021, Kuribara et al. 2019, Almeida et al. 2022, Faria et al. 2022). While previous works have interpreted the JFC as an initially juvenile intraoceanic magmatic arc that evolved into a more mature one (Duarte et al. 1997, 2000, Heilbron et al. 1998, 2010, 2013, Araújo et al. 2019, 2021), recent works have shown some evidence of reworking of some older Mesoarchean crust within this complex (Araújo et al. 2021, Almeida et al. 2022). The JFC represents the last magmatic arc to be accreted onto the southern margin of the São Francisco Paleocontinent, having collided with the Mantiqueira Complex during the early Orosirian (between 2.03 and 2.02 Ga; Heilbron et al. 1998, 2010, Noce et al. 2007, Degler et al. 2018, Araújo et al. 2019, 2021, Bruno et al. 2020, 2021a, 2021b, Almeida et al. 2022).

Table 1.
Compilation of Juiz de Fora Complex zircon U-Pb geochronology data.

Sample	Lithotype	Tectonic classification	Method	Age (Ma)			References
				Inherited	Magmatic	Metamorphic
5B	Felsic granulite	-	TIMS	-	2134	579	Machado et al. (1996)
LC-17	Enderbitic granulite	-	SHRIMP	-	2985 ± 17	808 ± 360	Silva et al. (2002)
LC-17	Enderbitic granulite	-	SHRIMP	-	2985 ± 17	2856 ± 10	Silva et al. (2002)
LC-32	Charnokitic granulite	-	SHRIMP	-	2195 ± 15	587 ± 9	Silva et al. (2002)
1070	Mafic granulite	E-MORB	LA-MC-ICP-MS		2427 ± 9	654 ± 12	Heilbron et al. (2010)
1076	Enderbitic granulite	-	LA-MC-ICP-MS		1966 ± 38	587 ± 15	Heilbron et al. (2010)
1065	Charnokitic granulite	-	LA-MC-ICP-MS		2199 ± 17	633 ± 140	Heilbron et al. (2010)
CJE-44	Mafic granulite	-	LA-MC-ICP-MS		1765 ± 34	586 ± 14	Heilbron et al. (2010)
1062	Charno-enderbitic granulite	-	LA-MC-ICP-MS		1656 ± 69	590 ± 5	Heilbron et al. (2010)
LC-66	Norite	-	SHRIMP		2119 ± 16	579 ± 5	Noce et al. (2007)
UB-1	Enderbite	-	SHRIMP		2084 ± 13	594 ± 37	Noce et al. (2007)
IV-48	Granodioritic orthogneiss	-	SHRIMP		2107 ± 71	580 ± 19	Degler et al. (2018)
M-03	Tonalitic orthogneiss	-	LA-MC-ICP-MS		2110 ± 12	-	Degler et al. (2018)
LC-07	Tonalitic orthogneiss	-	SHRIMP		2122 ± 11	565 ± 7	Degler et al. (2018)
RC-101	Enderbitic orthogneiss	-	SHRIMP		2144 ± 13	-	Degler et al. (2018)
RC-103	Enderbitic orthogneiss	-	SHRIMP		2143 ± 21	-	Degler et al. (2018)
VA-LM-07B	Enderbitic granulite	Low-K tholeiite	SHRIMP	-	2446 ± 10	-	Araújo et al. (2019, 2021)
RP-LM-04	Charnokitic granulite	Sanukitoid	SHRIMP	-	2182 ± 13	561 ± 41	Araújo et al. (2019, 2021)
RP-LM-04	Charnokitic granulite	Sanukitoid	SHRIMP		2182 ± 13	2021 ± 29	Araújo et al. (2019, 2021)
BP-LM-13	Charno-enderbitic granulite	Sanukitoid	SHRIMP	-	2200 ± 7	-	Araújo et al. (2019, 2021)
BP-LM-12	Charno-enderbitic granulite	TTG	SHRIMP	2364 ± 16	2197 ± 13	588 ± 18	Araújo et al. (2019, 2021)
BP-CM-151	Mafic orthogranulite	Tholeiite	LA-MC-ICP-MS	2395 ± 19	2134 ± 43	544 ± 19	Araújo et al. (2019, 2021)
RB13A	Charnokite	-	LA-MC-ICP-MS	-	2039 ± 22	589 ± 6	Kuribara et al. (2019)
MAJF26	Enderbitic orthogranulite	TTG	LA-ICP-MS	2380 ± 19	2085 ± 24	591 ± 10	Almeida et al. (2022)
CTVC 8D	Mafic orthogranulite	IAT	LA-ICP-MS	-	2101 ± 12	-	Almeida et al. (2022)
ADVC 241A	Enderbitic orthogranulite	Sanukitoid	LA-ICP-MS	-	2067 ± 6	-	Almeida et al. (2022)
SJVC 72A	Mafic orthogranulite	E-MORB	LA-ICP-MS	-	2038 ± 5	512 ± 11	Almeida et al. (2022)
MRVC 23A	Charnokitic orthogranulite	Hybrid granitoid	LA-ICP-MS	-	2019 ± 16	636 ± 39	Almeida et al. (2022)
MAJF 14	Charno-enderbitic granulite	Hybrid granitoid	LA-ICP-MS	2730 ± 19	1982 ± 18	600 ± 41	Almeida et al. (2022)
CPR-03	Granulitic orthogneiss	-	LA-MC-ICP-MS	-	2209 ± 22	596 ± 20	Faria et al. (2022)
CPR-04	Granulitic orthogneiss	-	LA-MC-ICP-MS	-	2199 ± 21	603 ± 20	Faria et al. (2022)
CPR-08	Granulitic orthogneiss	-	LA-MC-ICP-MS	-	2104 ± 16	622 ± 46	Faria et al. (2022)
CPR-10	Granulitic orthogneiss	-	LA-MC-ICP-MS	-	2196 ± 14	633 ± 22	Faria et al. (2022)
CPR-13	Migmatitic orthogneiss	-	LA-MC-ICP-MS	-	2176 ± 26	600 ± 18	Faria et al. (2022)
CPR-18	Migmatitic orthogneiss	-	LA-MC-ICP-MS	-	2160 ± 39	584 ± 29	Faria et al. (2022)
CPR-20	Migmatitic orthogneiss	-	LA-MC-ICP-MS	-	2121 ± 18	596 ± 16	Faria et al. (2022)

Previous tectonic models for the evolution of the JFC suggest an early evolutionary stage with moderately juvenile tholeiitic magmatism at 2.44 Ga, followed by moderately juvenile to evolved TTG-sanukitoid magmatic pulses between 2.20–2.18 and 2.07 Ga, and moderately juvenile tholeiitic magmatic pulses at 2.13 Ga (Araújo et al. 2019, 2021, Almeida et al. 2022). The JFC rocks record two high-grade metamorphic events: one in the beginning of the Orosirian (~2.03–2.02 Ga), interpreted as resulting from the collision of the JFC with the Mantiqueira Complex during the terminal phases of the São Francisco Paleocontinent amalgamation (Araújo et al. 2021), and another one in the Ediacaran (around 600–580 Ma), interpreted as the reworking of the continental margin by the Brasiliano/Pan-African orogenic system (Machado et al. 1996, Heilbron et al. 1998, 2010, 2020a, Kuribara et al. 2019, Cutts et al. 2020, Araújo et al. 2021, Almeida et al. 2022, Faria et al. 2022).

MATERIALS AND METHODS

The development of the present work involved field survey, petrographic descriptions, lithogeochemical analyses, whole-rock Sm-Nd and Sr isotopic analyses, and zircon U-Pb geochronology by a laser ablation multi-collector inductively coupled plasma source mass spectrometer (LA-MC-ICP-MS). Seven samples were pulverized at the Laboratório Geológico de Preparação de Amostras (LGPA/UERJ) and sent to Activation Laboratories Ltd. (Actlabs, Ancaster, Canada) for lithogeochemical analyses. For the Sm-Nd and Sr whole-rock isotope analysis, four samples were pulverized in the LGPA (UERJ) and sent to the Laboratório de Geocronologia e Isótopos Radiogênicos (LAGIR/UERJ), where the chemical separation of Sm, Nd, and Sr was carried out in cleanrooms and measurement of isotopic ratios was performed using a TRITON (Thermo Scientific) thermal ionization mass spectrometer (TIMS). For zircon U-Pb geochronology, two samples were analyzed at the Laboratório Multiusuário de Meio Ambiente e Materiais (MultiLab/UERJ) with an LA-MC-ICP-MS Neptune Plus mass spectrometer. Further details of the sample preparation routine, the analytical techniques, and equipment used, as well as the treatment of lithogeochemistry, Sm-Nd and Sr isotopes, and zircon U-Pb geochronology data, are provided in Supplementary Material A.

RESULTS

Field relationships and petrography

The JFC Paleoproterozoic rocks occur in razed anticline cores and as thrust slices interleaved with Neoproterozoic paragneiss and migmatitic paragneisses from the Raposos/Andrelândia Group and Neoproterozoic anatectic I-type granitoids from the Salvaterra Suite (Fig. 2). The contacts between JFC rocks and Neoproterozoic units are tectonic (faults, thrust zones, and shear zones). The main metamorphic foliation has an NNE-SSW strike and moderate to steep dips toward SE, and its distribution reflects large regional folds with vergence to W or NW (refer to geological cross section in Fig. 2).

Figure 2.
Map and geological section of the study area, with field stations and sampling locations for lithogeochemistry, Sm-Nd and Sr isotopes, and U-Pb geochronology data.

The rocks of the JFC are granodioritic granulites ranging from bluish-gray to deep gray color (Figs. 3A-3C) and display medium grain size with predominant granoblastic (Fig. 3B) and subordinate nematoblastic textures defined by oriented orthopyroxene grains (Fig. 3D). Millimeter to centimeter compositional banding characterized by light and dark gray tones is locally observed (Fig. 3A). The main mineralogy of the rocks is defined by plagioclase (34–55%), quartz (9–29%), K-feldspar (9–28%), and orthopyroxene (8–14%). Biotite (4–7%) occurs as either main or accessory phase. Clinopyroxene (0–3%), opaque minerals (0–2%), apatite (< 0.1%), zircon (< 0.2%), and titanite (0–0.1%) constitute the accessory phases.

Figure 3.
Field and petrographic aspects of the Juiz de Fora Complex granodioritic granulites in the Pedra Dourada region (MG): (A) compositional banding of light gray and medium grey granodioritic granulites; (B) detail of the granodioritic granulite with pyroxene porphyroblasts (dark spots); (C) detail of a dark gray granulite; (D) photomicrograph in plane-polarized light showing nematoblastic texture with oriented orthopyroxene (Opx) grains; (E) photomicrograph in cross-polarized light showing myrmekite within K-feldspar (Kfs) and Plagioclase (Pl) crystals; and (F) photomicrograph in plane-polarized light showing orthopyroxene (Opx) and opaque minerals (Op) grains partially replaced by retrometamorphic hornblende (Hbl) and biotite (Bt).

Orthopyroxene crystals are xenoblastic (Fig. 3B) and often surrounded by retrometamorphic hornblende and biotite (Fig. 3F). Plagioclase (without twinning) occurs as equigranular aggregates, whereas K-feldspar crystals are microperthitic and quartz usually shows amoeboid to interlobed contacts. Myrmekitic intergrowth of quartz between plagioclase and K-feldspar (Fig. 3E) is a common feature. Sub-idioblastic to idioblastic biotite flake aggregates without preferential orientation (decussate texture) are also observed.

Two distinct mineral parageneses can be distinguished: one with plagioclase + quartz + K-feldspar + orthopyroxene ± clinopyroxene + opaque minerals ± titanite, with metamorphic peak characteristics and another with hornblende + biotite, of retrometamorphic origin, partially replacing orthopyroxene, clinopyroxene, and opaque minerals.

Whole-rock geochemistry

The whole-rock lithogeochemical data (Suppl. Mat. B) obtained for seven granodioritic granulites show that the investigated samples share many compositional affinities, allowing their characterization as a single igneous suite. They display intermediate SiO₂ contents (58.4 to 65.8 wt.%), moderate to high Mg# values (0.44 to 0.54), and plot in the diorite-granodiorite fields of the TAS diagram (Fig. 4A). The granodioritic granulites are calcic, calc-alkaline, and alkali-calcic (Fig. 4B) and share a typical magnesian and dominantly metaluminous affinity, with A/CNK ratios between 0.81 and 1.01 (Figs. 4C and 4D). They also have moderate to high Ba (between 489 and 1,389 ppm) and Sr (377 to 624 ppm) contents (Fig. 4E). Other important geochemical characteristics are the Na₂O/K₂O ratios between 0.71 and 2.34 and Cr and Ni contents between 40–110 ppm and < 50 ppm, respectively. In the ternary diagrams proposed by Laurent et al. (2014), the samples plot in the sanukitoid and high-K mafic sources fields (Figs. 4F and 4G).

Figure 4.
Lithogeochemical classification diagrams and tectonic setting for the Juiz de Fora Complex granodioritic granulites: (A) TAS diagram by Cox et al. (1979); (B) Na₂O + K₂O + CaO vs. SiO₂ diagram from Frost et al. (2001); (C) FeO_t/(FeO_t + MgO) vs. SiO₂ diagram by Frost et al. (2001); (D) A/NK vs. A/CNK diagram by Shand (1943); (E) triangular diagram Rb-Ba-Sr with the field for high Ba-Sr granites from Tarney and Jones (1994); (F) source diagram by Laurent et al. (2014); (G) ternary classification diagram for late-Archean granitoids by Laurent et al. (2014).

The chondrite-normalized REE diagrams (Fig. 5A) show moderate fractionation between light and heavy REE, with (La/Yb)_N ratios ranging between 9.55 and 15.15. Eu anomalies are absent to weakly negative or positive. In the primitive mantle normalized diagrams (Fig. 5B), the samples show enrichment of Ba, K, Pb, Nd, and Dy, as well as depletion of Th, Nb, P, Zr, and Ti.

Figure 5.
REE patterns for the Juiz de Fora Complex granodioritic granulites: (A) chondrite-normalized to REE diagrams (Boynton 1984) and (B) primitive mantle-normalized REE diagrams (Sun and McDonough 1989).

Zircon U-Pb geochronology data

Zircon grains from samples CA-14 and CA-17 were analyzed by LA-MC-ICP-MS U-Pb techniques. The morphology and internal textures of the grains are shown in Fig. 6. The full analytical data set is shown in Suppl. Mat. B. The relationship between the U-Pb ages and Th/U ratios obtained for the different textural domains identified in the zircon grains for each of the analyzed samples is presented in Table 2.

Figure 6.
U-Pb concordia diagrams and cathodoluminescence images of representative zircon grains from the Juiz de Fora Complex granodioritic granulites: (A and B) sample CA-14; (C and D) sample CA-17.

Table 2.
Relationships between zircon U-Pb ages and Th/U ratios obtained for the different zircon domains of the analyzed samples (CA-14 and CA-17).

Sample	Domain	Age (Ma)	Th/U	Interpretation
CA-14	Core	2176 ± 7	0.15-1.22	Crystallization age
	Rimm	581 ± 12	0.19-0.61	Metamorphism age
CA-17	Core	2175 ± 12	0.25-1.02	Crystallization age
	Rimm	605 ± 26	0.45-1.85	Metamorphism age

Zircon grains from sample CA-14 are colorless and transparent, and display euhedral and subordinately subhedral morphology. They are mostly prismatic with pyramidal or rounded tips. Grain size ranges from 190 to 350 μm in length with dominant aspect ratios of 3:1, although the ratios of 4:1 and 2:1 are also observed. In the cathodoluminescence (CL) images, most grains show two distinct domains highly luminescent cores, with strong oscillatory zoning, and more homogeneous rims, with weak to no oscillatory zoning (Fig. 6A). The boundary between cores and rims is usually abrupt, with truncation of the oscillatory zoning pattern by the rim, suggesting processes of grain corrosion followed by metamorphic overgrowth. A total of 36 analyses in cores and rims were performed in thirty-two zircon grains, avoiding metamictic crystals and grains with inclusions and fractures. From the analyzed grains, 16 spot data were rejected because of high common Pb contents and/or large uncertainties of their isotopic ratios. Data from 20 spots define a discordia with an upper intercept age of 2176 ± 7 Ma (MSWD = 1.3), interpreted as magmatic crystallization age, and a lower intercept at 581 ± 12 Ma, interpreted to reflect the age of metamorphic overprint (Figs. 6B and Table 2).

In sample CA-17, the zircon grains are predominantly subhedral to euhedral, prismatic with a pyramidal to rounded tips, and also colorless and transparent. Inclusions, although not very abundant, are also observed. Zircon grains have lengths ranging between 210 and 360 μm and aspect ratios of 3:1 and 4:1, with subordinate ratios of 2:1 and 3:2. CL textures are relatively complex. Most of the grains exhibit strongly luminescent cores with oscillatory zoning (typical of igneous zircons) surrounded by more homogeneous and weakly zoned rims (Fig. 6C). As in the previous sample, the boundary between these two domains is commonly abrupt. A total of 36 analyses in cores and rims were performed in twenty-seven zircon grains.Notably, 21 spots were discarded using the same criteria described for sample CA-14. The data from 15 spots were used to construct a discordia with upper intercept age of 2175 ± 12 Ma (MSWD = 2.4) and lower intercept age of 605 ± 26 Ma, interpreted, respectively, as the magmatic crystallization and as the metamorphic ages (Fig. 6D and Table 2).

Sm-Nd and Sr isotopes

Four samples were selected for the determination of ID-TIMS Sm-Nd and natural Sr isotopic compositions (Table 3). The Nd and Sr isotope ratios were calculated to initial values according to the U-Pb crystallization ages obtained from samples CA-14 and CA-17 (2176 and 2175 Ma, respectively).

Table 3.
Petrogenetic parameters and model age (T_CHUR and T_DM) calculated from isotopic analyzes of Sm-Nd and Sr in whole rock of the granodioritic granulites from the Juiz de Fora Complex.

Sample	CA-02	CA-14	CA-17	CA-22
SmID	5.6	7.5	4.5	10.2
NdID	28.0	35.5	25.7	54.2
Rb*	39.0	28.0	157.0	71.0
Sr*	624.0	542.0	414.0	377.0
143Nd/144Nd(m)	0.511355	0.511573	0.511377	0.511444
Std. Err. Abs (2s)	0.000006	0.000004	0.000003	0.000006
147Sm/144Nd(m)	0.1215	0.1268	0.1070	0.1132
87Sr/86Sr(m)	0.716290	0.718424	0.728180	0.725007
Std. Err. Abs (2s)	0.000010	0.000011	0.000004	0.000005
Age (Ma)	2.18	2.18	2.18	2.18
fSm/Nd (0 Ma)	-0.38	-0.35	-0.46	-0.42
εNd (t)	-4.0	-1.2	0.5	0.0
εNd (0 Ma)	-25.0	-20.8	-24.6	-23.3
TCHUR (± 0.05 Ga)	2.60	2.32	2.14	2.18
TDM (± 0.05 Ga)	2.59	2.31	2.13	2.17
87Sr/86Sr(i)	0.7106	0.7137	0.6937	0.7079

• ^*
  Values from lithogeochemical data.

Sample CA-02 has the most negative initial εNd (−4.0) and the oldest T_DM (2.57 Ga). Samples CA-14, CA-17, and CA-22, in turn, present the initial near-CHUR εNd values, between −1.2 and 0.5, as well as T_DM ages between 2.30 and 2.12 Ga, which are near or even coincident with the age of magmatic crystallization. The obtained initial ⁸⁷Sr/⁸⁶Sr ratios range from 0.6937 to 0.7137 (Table 3).

DISCUSSION

Petrogenetic implications

The geochemical data strongly suggest that these rocks were generated in a magmatic arc setting: intermediate SiO₂ contents, affinity with the calc-alkaline series, magnesian and metaluminous to weakly peraluminous character, moderate to high Ba, Sr, and LILE contents and low HFSE contents, moderate (La/Yb)_N ratios, and significantly fractionation between LREE and HREE, with slightly positive or negative to absent Eu anomalies (Hawkesworth et al. 1994, Foley et al. 2002, Rustioni et al. 2021). Depletion in Nb and Ti together with Pb enrichment is also the main characteristics of modern magmatic arcs (Kelemen et al. 1993). Moderate to high Mg# is also evidence for mantle melting (Zhang et al. 2019, Zheng 2019) and enrichment in Ba and K suggests the participation of fluids derived from a descending plate as a metasomatic agent (Pearce and Parkinson 1993, Zheng 2019, Nielsen et al. 2020, Rustioni et al. 2021).

Based on the main geochemical characteristics highlighted above, the study rocks are interpreted to have derived from a magma sourced from the peridotitic mantle metasomatized by fluids and melts derived from subducting oceanic crust. In contrast to modern BADR magmatic arc rocks, the studied samples show characteristics which are more similar to those of the sanukite series, as described by Stern et al. (1989), Stern and Hanson (1991), Martin et al. (2005, 2010), and Heilimo et al. (2010): moderate to low Na₂O/K₂O ratios, and moderate to high Mg# and (La/Yb)_N ratios (Table 4).

Table 4.
Comparison of the chemical composition of the granulitic granulites studied in the present work with the typical composition of the sanukitic series, Archean sanukitoids, Paleoproterozoic Sanukitoids, and modern arc granitoids.

	Sanukitic Serie1,2,3	Archean Sanukitoids4 (n = 104)	Archean Sanukitoids of Karelian Province5 (n = 161)	Paleoproterozoic sanukitoids of the Aravalli craton, India6 (n = 20)	Modern arc granitoids4 (n = 250)	Sanukitoids from northern Juiz de Fora Complex (This work)
						Average (n = 7)	CA-11	CA-14	CA-02	CA-22	CA-23	CA-04	CA-17
SiO2	55-73	58.65	55-70	62.01	68.1	62.52	58.41	59.78	60.62	63.50	64.56	64.99	65.79
MgO	5.2-9.17	3.90	1.5-9	1.44	1.55	2.77	2.89	3.48	3.45	2.60	2.98	2.05	1.91
K2O	0.5-4	3.11	1.5-5	5.40	3.4	2.83	3.42	1.69	2.24	2.42	1.72	4.12	4.18
Ba	> 1,000	1,471	706-1613	1,174	715	954.43	1368	509	1197	648	489	1389	1081
Sr	> 500	1,108	513-941	213	316	477.57	455	542	624	377	449	482	414
Cr	≤ 150	104	6-184	16.7	23	67.14	40.0	110.0	90.0	70.0	50.0	50.0	60.0
Ni	90-205	54	8-85	12.6	10.5	35	< 20	50.0	< 20	< 20	< 20	< 20	20.0
Mg#	0.43-0.62	0.53	45-65	0.33	0.41	0.47	43.69	46.07	46.78	43.81	54.02	46.26	46.00
Na2O/K2O	~3	1.38	0.5-3	0.39	1.08	1.18	0.99	2.34	1.53	1.31	1.90	0.71	0.76
Ba+Sr	> 1,500	> 1,466*	> 1,400	1387	1,031	1432	1,823	1,051	1,821	1,025	938	1,871	1,495
(La/Yb)N	-	30.5	14-47	14.95	6.4	12.66	13.7	13.44	9.55	12.18	13.72	15.15	10.85
Rb/Sr	0.01-0.16	0.08	0.10-0.13	0.69	0.35	0.17	0.18	0.05	0.06	0.17	0.16	0.24	0.38

• ¹
  Shirey and Hanson (1984);
• ²
  et al;
• ³
  Stern e Hanson (1991);
• ⁴
  et al;
• ⁵
  et al;
• ⁶
  et al.

Comparing the composition of the studied rocks with that of typical sanukitoid rocks (Table 4), both are magnesian calc-alkaline with intermediate SiO₂, with high Mg#, metaluminous to weakly peraluminous, with high Ba and Sr and low Na₂O/K₂O ratios. Although Cr contents are similar to those of sanukitoids, the Ni contents of the studied samples are comparatively lower, as well as the (La/Yb)_N ratios around 6.0, but significantly higher than those found in the BADRs suites (Table 3; Martin et al. 2005, 2010, Heilimo et al. 2010). Thus, given that the studied rocks present most chemical characteristics in agreement with the values expected for the sanukitic series, their chemical/tectonic classification as sanukitoid is appropriate.

Integrating the zircon U-Pb geochronology with the Sm-Nd and Sr isotopic data, the studied rocks have chondritic to slightly contaminated initial ε_Nd isotopic signatures, between −4.0 and 0.5. Their juvenile character is indicated by the T_DM model ages that are either coincident with, or slightly older than, the magmatic crystallization ages. In contrast, the initial ⁸⁷Sr/⁸⁶Sr ratios point to some significant crustal contribution within its metasomatized mantle source. These data imply that the mantle source of the magmas that generated these rocks features an enriched mantle signature, probably associated with the assimilation of fluids and sediments recycled back to the mantle by descending oceanic plates during protracted events of subduction in modern convergent margin settings, as discussed by Hawkesworth et al. (1994), Chauvel et al. (2008), and Zhang et al. (2019).

Neoproterozoic metamorphic overprint

The metamorphic ages obtained between 581 and 605 Ma are compatible with data presented in previous regional studies (Machado et al. 1996, Heilbron and Machado 2003, Heilbron et al. 2010, 2020a, 2020b, Degler et al. 2018, Kuribara et al. 2019). During the Brasiliano/Pan-African overprint at ~580 Ma, intense deformation and regional metamorphism resulted from the collision stage of the Araçuaí-Ribeira Orogenic System (with the collision between the São Francisco Paleocontinent margin and the Inner Arc System — Rio Doce and Serra da Bolívia magmatic arcs; Heilbron and Machado 2003, Heilbron et al. 2017, 2020a, 2020b). As evidenced by the morphology of the zircon grains and high Th/U ratios, the high metamorphic grade of the rocks is also evidenced by mineral peak metamorphic associations typical of the granulite facies (with orthopyroxene + clinopyroxene + plagioclase) in all study samples.

The Neoproterozoic granulite metamorphism is common in the entire JFC (Duarte et al. 1997, 2000, Heilbron et al. 1998, 2010, Medeiros Júnior et al. 2017) and is also observed in nearby units, such as the paragneisses from the Raposos and Bom Jesus do Itabapoana groups and in the orthogneisses from the Neoproterozoic Serra da Bolivia/Rio Doce magmatic arc (Karniol et al. 2009, Santos et al. 2011, Gouvêa et al. 2020, Marques et al. 2021). In addition, the observation of hornblende and biotite partially substituting orthopyroxene and clinopyroxene in some samples suggests retrometamorphism in conditions of upper amphibolite facies, also in agreement with regional works (Santos et al. 2011, Ferreira et al. 2020, Marques et al. 2021).

Sanukitoid suites in the southern São Francisco Paleocontinent

Several Neoarchean to the late Rhyacian sanukitoid suites related to the accretionary processes that formed the São Francisco Paleocontinent have been previously described in the Minas Segment of the MBOS (Seixas et al. 2013, Moreira et al. 2018, Bruno et al. 2020, 2021a, 2021b, Araújo et al. 2019, 2021, Almeida et al. 2022). The generation of these different sanukitoid suites, mostly following the formation of TTG suites, has been interpreted as evidence of the diachronism on Earth’s geodynamic processes that changes from typical Archean tectonic regimes to tectonic regimes more likely to those currently active (Moreira et al. 2018, 2020, Bruno et al. 2020, 2021a, 2021b). In order to generate more regional interpretations, the dataset obtained was compared with compiled data from different Paleoproterozoic sanukitoid suites from the Minas Segment of the MBOS (Fig. 7 and Table 5), which occur in the southern JFC (Araújo et al. 2019, 2021, Almeida et al. 2022), in the Mantiqueira Complex (Bruno et al. 2020) and in the Mineiro Belt (Seixas et al. 2013, Moreira et al. 2018, Bruno et al. 2021b). The considerations in this topic assume that the sanukitoid suites of each of these compartments have an independent (not cogenetic) evolution.

Figure 7.
Location of sanukitoid occurrences in southern São Francisco Paleocontinent. (A) Regional tectonic-structural compartmentalization and (B) simplified regional geological map and sanukitoid rocks occurrences (with U-Pb and Sm-Nd data).

Table 5.
Comparison of the different Paleoproterozoic sanukitoid suites from the south of the São Francisco Paleocontinent with ages of magmatic crystallization, initial ε_Nd, and T_DM.

Unit	Lithotypes	Age (Ma)	εNd (t)	TDM (Ga) (± 0.05)	References
Juiz de Fora Complex	Granodioritic granulites	2176 to 2175	-4.0 to + 0.5	2.57 to 2.12	This work
	Charno-enderbitic granulite	2200 to 2180	-4.8 to -2.9	2.62 to 2.46	Araújo et al. (2019, 2021)
	Enderbitic orthogranulite	2068	-11.0	3.05	Almeida et al. (2022)
Mantiqueira Complex	Hbl-Bt orthogneiss	2168	-9.7	3.18	Bruno et al. (2020)
Mineiro Belt	Tonalite	2130	-0.8 to + 0.9	2.40 to 2.30	Seixas et al. (2013)
	Bt-Hbl tonalites	2149 to 2135	-	-	Moreira et al. (2018)
	Granodioritic Hbl-Bt orthogneiss	2152 to 2114	-5.0 to + 1.3	2.64 to 2.21	Bruno et al. (2021b)

Regarding the major element compositions, all suites in question are very similar, with a predominance of rocks with intermediate SiO₂ contents and normatively classified as diorites and granodiorites (Fig. 8A). Their calc-alkaline character with high-K mafic rocks sources (Fig. 8B) is expected since they are all classified as sanukitoid rocks (Fig. 8C). When analyzing their REEs patterns (Figs. 9A and 9B), differences begin to become more noticeable. The JFC sanukitoid rocks are quite similar to the other sanukitoid rocks of the southern São Francisco Paleocontinent and, in general, all suites have similar characteristics (fractionation between LREE and HREE; absent, slightly positive, or slightly negative Eu anomalies; enrichment in LILE and depletion in HFSE). However, for the JFC sanukitoid rocks, those described in this work and in Araújo et al. (2021) are noticeably more enriched in LREE than those described by Almeida et al. (2022), where the fractionation between LREE and HREE is less expressive. This implies that these rocks were generated by lower degrees of partial melting or fractionation processes than the others. Moreover, the sanukitoid rocks of the southern JFC described by Almeida et al. (2022) show higher enrichment in fluid-mobile elements (e.g., Ba and Sr; Zheng 2019, Nielsen et al. 2020) and depletion in Th (melt-mobile; Zheng 2019).

Figure 8.
Comparison of major element composition of sanukitoid suites from southern São Francisco Paleocontinent: (A) TAS diagram of Cox et al. (1979); (B) source diagram of Laurent et al. (2014); (C) ternary classification diagram for late-Archean granitoids of Laurent et al. (2014).

Figure 9.
REE patterns of the different sanukitoid suites from southern São Francisco Paleocontinent: (A) chondrite-normalized REE (Boynton 1984) and (B) primitive mantle-normalized REE (Sun and McDonough 1989).

The differences between these different sanukitoid suites become more explicit when their crystallization ages and their Sm-Nd isotopic signatures are compared (Table 5, and Figs. 7 and 10). In general, most of them (the sanukitoid suites of the JFC, Mantiqueira Complex, and Mineiro Belt) have Rhyacian crystallization ages, initial ε_Nd between −5.0 and +1.3 (moderately juvenile), and Neoarchean to Siderian and Rhyacian T_DM Nd model ages. The exceptions are the sanukitoid rocks of the southern CJF (Almeida et al. 2022) and Mantiqueira Complex (Bruno et al. 2020), both with significantly lower initial ε_Nd (−10.98 and −9.7, respectively) and Mesoarchean T_DM ages. In addition, the southern JFC sanukitoid rocks described by Almeida et al. (2022), with a crystallization age of 2068 Ma, are the youngest sanukitoid rocks reported from the southern São Francisco Paleocontinent.

Figure 10.
Initial ε_Nd versus initial ⁸⁷Sr/⁸⁶Sr of the different sanukitoid suites from the southern São Francisco Paleocontinent.

In the regional scenario (Fig. 7), the integration and analysis of these data suggest that the rocks from the Minas segment of the MBOS, in the southern São Francisco Paleocontinent, record at least two stages of sanukitoid generation: the first and more long-lived event, between 2.20 and 2.11 Ga, is coincident with the climax of juvenile crust formation within the Minas Segment of the MBOS and coeval with the generation of different sanukitoid suites (along with TTG suites and granitoid rocks) from the Mineiro Belt (Seixas et al. 2013, Moreira et al. 2018, Bruno et al. 2021b) and the Mantiqueira and JFC complexes (Bruno et al. 2020, Araújo et al. 2021; and this work); the second and younger event, dated at ca. 2.07 Ga, is restricted to the JFC (Almeida et al. 2022) and was emplaced immediately before the regional metamorphism resulting from the diachronic collision of Archean blocks and Paleoproterozoic magmatic arcs during the final stages of São Francisco Paleocontinent amalgamation, as suggested by the emplacement of syn-collisional granitoid rocks and metamorphism ages between 2.05 Ga in Mineiro Belt (Moreira et al. 2018, Bruno et al. 2020, 2021b) and 2.03 Ga in the JFC (Araújo et al. 2021).

Regarding the geodynamic processes responsible for the generation of these rocks, the generation of pre-collisional rocks with a sanukitoid signature in the midst of calc-alkaline granitoid suites, magmatic arc tholeiites, and TTG suites allows the interpretation of a scenario with a complex accretionary system during the Paleoproterozoic in these different compartments (i.e., Mineiro, and the Mantiqueira and Juiz de Fora complexes; Fig. 11). In contrast to the typical sanukites, the sanukitoid magmatic arc signature depicted by the rocks from the Minas Orogen shows a lower fractionation between LREE and HREE, with intermediate (La/Yb)_N ratios between typical Archean sanukitoid and BADR suites from modern magmatic arcs. This difference implies lower degrees of interaction between melts from the subducting plate and the peridotite mantle, limiting the metasomatism of the mantle wedge in the subduction zone almost exclusively by fluids released from the descending plate at depth, in a process that is intermediate between the generation of typical sanukitoids and modern BADR suites, which is possible with an increase in the dip angle of the descending plate, as presented by Martin et al. (2010). Regarding the sources of these rocks, the initial ε_Nd varying between close to 0 and −11 (Table 5 and Fig. 10) attest to the origin of these magmas in a hybrid mantle, significantly modified by the assimilation of crustal material (fluids and melt) from the subducting plate and sediments carried out into the mantle by the descending slab over an extended period of time and/or by earlier subduction processes, as discussed by Hawkesworth et al. (1994), Chauvel et al. (2008), and Zhang et al. (2019).

Figure 11.
The Minas Orogen at about 2.15 Ga: (A) paleogeographic reconstruction of the configuration of the crustal blocks and magmatic arcs of southeastern São Francisco Paleocontinent at ca. from 2.15 Ga (modified from Alkmim and Teixeira 2017, Bruno et al. 2021b) and (B) schematic tectonic cross-section of the generation of mantle-derived rocks (e.g., sanukitoids) in the Mineiro Belt and in the Mantiqueira and Juiz de Fora complexes in ca. of 2.15 Ga (modified from Bruno et al. 2021a).

CONCLUSIONS

The study rocks are granodioritic granulites, with chemical characteristics compatible with those of sanukitoid rocks: they are intermediate SiO₂, with moderate to high Ba, Sr, Mg#, high (La/Yb)_N ratio, and low Na₂O/K₂O ratio. They are crystallized at ca. 2175 Ma and underwent high-grade metamorphism at ca. 605–580 Ma during the Brasiliano orogenic events. In addition, initial εNd between −4.0 and +0.5, T_DM between 2.57 and 2.12 Ga, and initial ⁸⁷Sr/⁸⁶Sr ratios between 0.6937 to 0.7137 are typical of moderately juvenile to slightly evolved (contaminated?) isotope sources and suggest that the genesis of these rocks is related to a hybrid mantle source contaminated with crustal material (fluids, sediments, and melts) during protracted periods of subduction and/or by previous subductions.

In the Paleoproterozoic scenario of the southern São Francisco Paleocontinent, there are at least two periods of generation of magmatic arc rocks with sanukitoid signatures, namely, the first one, between 2.20 and 2.11 Ga, is associated with calc-alkaline granitoid rocks, IAT and TTG rocks in the Mineiro Belt, Mantiqueira, and JFC complexes; and a younger one, restricted to the JFC, with the generation of sanukitoid rocks and calc-alkaline granitoid and TTG rocks at ca. 2.07 Ga. Such rock associations with distinct signatures attest to a complex and enduring accretionary system to the southeast of the São Francisco Paleocontinent during the Rhyacian (within the Minas Segment), very similar to those of modern plate tectonics accretionary settings.

ACKNOWLEDGMENT

The authors thank CAPES for the master’s scholarship granted to the first author (process n° 88887.601073/2021-00), to CNPQ and FAPERJ for funding the activities, and to the technicians and coordinators of MultiLab and LAGIR, for their assistance and commitment in carrying out the geochronological and isotopic analysis, respectively. Here, we also express our gratitude to the professionals from the LGPA (UERJ) and LPA (UFES) for their help with the preparation of the samples, and to Matheus Alves for his help in the field surveys. MH and CMV acknowledge their CNPq-PQ and FAPERJ-CNE grants. The authors also thank the reviewers for their valuable contributions and, the editor, for his dedication in leading the editorial process.

Supplementary data

Supplementary data associated with this article can be found in Supplementary Material A and Supplementary Material B.

ARTICLE INFORMATION

• Manuscript ID: 20220038.
  How to cite: Mauri S., Heilbron M., Bruno H., Marques R.A., Neto C., Valeriano C.M., Bersan S., Romero L.F., Geraldes M.C. Rhyacian magmatic arc rocks with sanukitoid geochemical signature from the Juiz de Fora Complex, Minas-Bahia Orogenic System (SE-Brazil). Brazilian Journal of Geology, 52(4):e20220038. https://doi.org/10.1590/2317-4889202220220038

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Publication Dates

• Publication in this collection
  03 Feb 2023
• Date of issue
  2022

History

• Received
  18 May 2022
• Accepted
  06 Oct 2022