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Magnetic Fabrics and Microstructures of Paleoproterozoic Intrusive Bodies of Piedra Alta Terrane, Río De La Plata Craton, Uruguay: a Reconnaissance Study

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Magnetic Fabrics and Microstructures of Paleoproterozoic Intrusive Bodies of Piedra Alta Terrane, Río De La Plata Craton, Uruguay: a Reconnaissance Study SILEIR RA A D B E E G D E A O D L E O I G C I A O ARTICLE BJGEO S DOI: 10.1590/2317-4889202020200002 Brazilian Journal of Geology D ESDE 1946 Magnetic fabrics and microstructures of Paleoproterozoic intrusive bodies of Piedra Alta Terrane, Río de la Plata Craton, Uruguay: a reconnaissance study Pablo Reinaldo Franceschinis1,2* , Augusto Ernesto Rapalini1,2 , Leda Sánchez Bettucci3 , Carmen Martínez Dopico1,2 , Florencia Nidia Milanese1,2 Abstract Small to medium-sized intrusive bodies with ages between 2.1 and 2.0 Ga characterize Piedra Alta terrane and represent the final stabilization of Río de la Plata Craton. A reconnaissance study of petro- and magnetic fabrics based on microscopic observations, anisotropy of magnetic susceptibility and anhysteretic remanent magnetization, was carried out on 41 sites from 14 intrusive bodies, in order to obtain preliminary information on kinematics of their emplacement, degree of deformation, and regional stress regime during this magmatic event. The mag- netic fabrics coupled with the microstructural analysis are interpreted as generally reflecting magma kinematics near solidus temperature, although few cases of tectonically modified fabrics at local levels have been interpreted. Field evidence and magnetic fabrics in most plutons show subvertical to high angle E-W to NE-SW trending foliations and subvertical lineations. These data suggest that plutons were probably intruded under a regional extensional to transtensional regime, which controlled the magma ascent and distribution of the intrusions. Lack of metamorphism and low to null deformation shown by the study plutons suggest a late-orogenic character for this magmatism, which has been associated with crustal stabilization after accretionary processes that led to the formation of Río de la Plata Craton in the Orosirian. KEYWORDS: Piedra Alta terrane; Río de la Plata craton; anisotropy of magnetic susceptibility. INTRODUCTION main axes (Tarling and Hrouda 1993). The relations between The anisotropy of magnetic susceptibility (AMS) is a tech- these axes provide information about the anisotropy magnitude nique that has been widely applied to infer the rock petrofabric and the ellipsoid shape (Jelinek 1981), which, under certain from the measurement of the magnetic susceptibility ellipsoid conditions, may reflect the petrofabric of the rock under inves- (e.g., Tarling and Hrouda 1993, De Saint-Blanquat et al. 2001, tigation. However, interpretation of AMS results is, in many Martín-Hernández et al. 2004, Raposo et al. 2012, Mondal et al. cases, ambiguous due to the varied minerals that contribute 2018). Its rapidity and simplicity have transformed this tech- to the magnetic susceptibility of each rock. When well-con- nique into a very valuable tool to study the internal structure, strained by microscopic observations and different kinds of and therefore the emplacement kinematics of plutonic bod- mineral identification methods, AMS may result in a powerful ies in virtually all tectonic environments (e.g., Bouchez et al. tool for deciphering the emplacement kinematics of plutonic 1992, López de Luchi et al. 2010, Schöpa et al. 2015, among bodies and their tectonic framework (Fig. 1). others). The AMS has proved to be very useful on numerous During the late Early to Middle Paleoproterozoic occasions to determine the degree and spatial distribution of (ca. 2.2–2.0 Ga), a major crustal forming and stabilization deformation in rocks with low to moderate tectonic distur- event took place in Río de la Plata Craton (Sánchez Bettucci bance (e.g., Rochetteet al . 1992, Borradaile and Henry 1997, et al. 2010, Oyhantçabal et al. 2011; and references therein). Bolle et al. 2018; among others). The AMS ellipsoid is defined This event has been well known since several decades as the by the maximum (K1), intermediate (K2), and minimum (K3) “TransAmazonian” cycle (Almeida et al. 1973). It also affected other cratons, such as Congo-São Francisco (Alkmim and Marshak 1998, Toteu et al. 2001, Aguilar et al. 2017, De Waele 1Universidad de Buenos Aires – Buenos Aires, Argentina. et al. 2008) and Guyana (or proto-Amazonia, Tassinari and E-mails: [email protected], [email protected], Macambira 1999, Delor et al. 2003, McReath and Lins Faraco [email protected], [email protected] 2006). In Piedra Alta terrane (Figs. 1A and 1B), which constitutes 2Consejo Nacional de Investigaciones Científicas y Técnicas – Buenos Aires, Argentina. the “core” of Río de la Plata Craton, this process is recorded by 3Universidad de la República – Montevideo, Uruguay. the presence of large granitic-gneissic areas separated through E-mail: [email protected] supracrustal metamorphic belts (rhyolites, micaschists, basalts, *Corresponding author. turbidites, iron formations, among others) assigned to intra-oce- © 2020 The authors. This is an open access article distributed anic or back-arc environments (San José, Florida and Arroyo under the terms of the Creative Commons license. Grande belts, Sánchez Bettucciet al . 2010). Dominant Sm-Nd 1 Braz. J. Geol. (2020), 50(1): e20200002 and Lu-Hf model ages for Piedra Alta terrane (2.5–2.1 Ga) medium-sized intrusions, dominantly but not exclusively, of strongly suggest major crustal formation processes with little granitic to granodioritic composition (see Rapalini et al. 2015). to negligible recycling of older crusts (Oyhantçabal et al. 2011, Getting information on the petrofabric of these bodies may give Oriolo et al. 2016). Granitic-gneissic terranes are interpreted some clues regarding the mechanisms of magma intrusion in as complexes that record juvenile products of subduction-re- an early Paleoproterozoic crust in the cratonization process, as lated magmatism (Preciozzi and Bourne 1992, Schipilov et al. well as in the general stress regime that affected them. Hence, 1998). By around 2.0 Ga, Río de la Plata Craton was probably we may contribute to a better understanding of the tectonic already a tectonically stable crustal block (Peel and Preciozzi processes that were involved in the final formation stages of a 2006), composed by Piedra Alta terrane and Tandilia System small continent: the Paleoproterozoic Río de la Plata Craton. (see Oyhantçabal et al. 2011, Cingolani 2011). Nico Pérez Rapalini et al. (2015) presented the first magnetic fabric (Preciozzi et al. 1979) and Cuchilla Dionisio terranes in Eastern results on six of such igneous bodies of Piedra Alta terrane. Uruguay (Rapela et al. 2011, Oriolo et al. 2016, among oth- To complement that study and obtain a more representa- ers) were accreted much later, during Neoproterozoic times. tive picture of this major tectono-magmatic process, we car- Crustal stabilization of Piedra Alta terrane is recorded by the ried out a magnetic fabric study by means of measuring the intrusion of Paleoproterozoic magmatic bodies scarcely and AMS on the selected sites of 14 other intrusions (Fig. 1B). only localized deformed. They constitute numerous small to Our analysis was accompanied by microscopic observations A B PLSZ: Paso de Lugo Shear Zone; CSZ: Cufré Shear Zone. Figure 1. (A) Location of Río de la Plata craton and its relationship with other South American terranes and cratons. White box indicates the location of Piedra Alta terrane within Río de La Plata Craton. (B) Intrusives studied in this paper. In italics, the intrusives previously studied by Rapalini et al. (2015). Modified from Sánchez Bettucciet al . (2010), Rapalini et al. (2015) and Franceschinis et al. (2016). 2 Braz. J. Geol. (2020), 50(1): e20200002 and rock-magnetic experiments in order to characterize their considered of Paleoproterozoic age, and a strike-slip sinistral microstructures and to determine the main mineral phases behavior has been proposed (Preciozzi 1993). responsible for the magnetic fabrics. San José Belt is represented by San José, Paso Severino and This is taken as a reconnaissance study, considering that no Montevideo formations (Fig. 1B). San José Formation consists systematic sampling with sufficient density was carried out at of meta-volcanic rocks, both acidic and basic, and a metasedi- each pluton. However, the consistent results obtained in most mentary succession. The Paso Severino formation consists of bodies strongly suggest a general regional pattern. rhyolites, basalts, metapelites, carbonates, and banded iron levels. San José belt is affected by Cufré Shear Zone (CSZ) of possible Paleoproterozoic age, which is of an approximate E-W GEOLOGICAL SETTING orientation and has strike-slip sinistral behavior. It also presents a series of intrusive bodies ranging from granites to gabbros of Piedra Alta terrane around 2.10 and 2.05 Ga that have been classified as late- to Bossi et al. (1993) originally defined three outcropping post-orogenic (Peel and Preciozzi 2006, Hartmann et al. 2008, metamorphic belts in the South-central part of Piedra Alta Oyhantçabal et al. 2018). Several of these bodies were studied terrane. Oyhantçabal et al. (2003) reduced their number to in this paper (Figs. 1 and 2). To the South of Santa Lucia rift, two: Arroyo Grande and San José Belts (Fig. 1B). Both green- the Montevideo Formation is exposed, consisting in amphi- stone belts show an E-W trend. The former is a greenschist bolites, micacites and gneisses (Sánchez Bettucciet al . 2010, facies volcano-sedimentary succession represented by Arroyo Oyhantçabal et al. 2011). Metamorphic grade is higher than Grande Formation (Oyhantçabal et al. 2011). This volca- in the North and reaches amphibolite facies. The Montevideo no-sedimentary sequence consists of quartzite, metapelites, formation is affected by Mosquitos Shear Zone (MSZ), which metasandstones, rare meta-conglomerates, and meta-basalts has been dated as early to middle Orosirian (1909 ± 23 and and metandesites (Sánchez Bettucciet al . 2010, Oyhantçabal 2049 ± 25 Ma) with K-Ar ages of muscovite grains (Oyhantçabal et al. 2011). Arroyo Grande belt is intruded by much less to et al. 2006). This fault zone also shows an approximate E-W virtually undeformed granitoids represented by the ca. 2.10 Ga orientation and a strike-slip sinistral behavior.
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