Provenance of detrital zircons of the canindé group (Parnaíba basin), northeastern Brazil

Accepted Manuscript Provenance of detrital zircons of the canindé group (Parnaíba basin), northeastern Brazil Camila Vilar de Oliveira, CandidoA.V. Moura PII:

S0895-9811(18)30213-X

DOI:

https://doi.org/10.1016/j.jsames.2018.12.009

Reference:

SAMES 2066

To appear in:

Journal of South American Earth Sciences

Received Date: 15 May 2018 Revised Date:

1 November 2018

Accepted Date: 13 December 2018

Please cite this article as: Vilar de Oliveira, C., Moura, C.V., Provenance of detrital zircons of the canindé group (Parnaíba basin), northeastern Brazil, Journal of South American Earth Sciences (2019), doi: https://doi.org/10.1016/j.jsames.2018.12.009. This is a PDF file of an unedited manuscript that has been accepted for publication. As a service to our customers we are providing this early version of the manuscript. The manuscript will undergo copyediting, typesetting, and review of the resulting proof before it is published in its final form. Please note that during the production process errors may be discovered which could affect the content, and all legal disclaimers that apply to the journal pertain.

PROVENANCE OF DETRITAL ZIRCONS OF THE CANINDÉ GROUP (PARNAÍBA ACCEPTED MANUSCRIPT BASIN), NORTHEASTERN BRAZIL Camila Vilar de Oliveira1,2, Candido A V Moura2

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Programa de Pós-Graduação em Geologia e Geoquímica, Instituto de Geociências, Universidade Federal do Pará, Belém, Brazil; 2 Instituto de Geociências, Universidade Federal do Pará, Belém, Brazil; ABSTRACT

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This is the first work focusing on the provenance of Middle Devonian-Early Carboniferous sandstones in the eastern margin of the Parnaíba basin. This sedimentary succession represents the main petroleum system in this basin and is composed, from base to top, of the Itaim, Pimenteiras, Cabeças, Longá and Poti Formations of the Canindé Group. The internal textures and U-Pb analyses of detrital zircons allowed defining potential source areas for the sediments of this group. A global tendency of sea level rise in the Middle Devonian, in the evolutionary context of West Gondwana, resulted in the establishment of epicontinental seas and deposition of transgressive sedimentary sequences. Shales and sandstones of the Pimenteiras Formation represent extensive records of these Devonian seas on this paleocontinent. This succession provides zircon ages from 3443-438 Ma. Detrital zircons with ages of 538-486 Ma are the most abundant, suggesting derivation mainly from nearby younger sources in the Southern subprovince of the Borborema or Tocantins provinces. The transition between the Middle Devonian and Mississippian Periods is marked by progressive retreat of epicontinental seas with minor marine incursions (represented by the Longá Formation) and resulted in the continental deposits of the Cabeças and Poti Formations. Paleocurrent patterns in both formations suggest direct derivation from the Borborema province. The Cabeças, Longá and Poti Formations contain numerous zircons with ages ranging from 999 to 722 Ma. This detrital population indicates derivation from rocks formed during the Cariris Velhos event in the central portion of the Borborema province. The Cabeças Formation also provided an extensive number of zircons with ages ranging from 2034 to 1830 Ma. Further, the studied geologic units, except for the Pimenteiras formation, show detrital contingents with ages of 1.0-1.2 Ga, also suggesting provenance from distal areas. However, as the spectrum of zircon ages of the Canindé Group is similar to that of the Brasiliano belts surrounding the Parnaíba basin, these belts may also be considered candidates to provide sediments for the Middle Devonian-Early Carboniferous deposits.

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Keywords: U-Pb geochronology; Provenance; Detrital zircons; Parnaíba basin; Canindé Group.

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1. INTRODUCTION

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U-Pb geochronology is a powerful technique for extracting source information from detrital zircon grains. Detrital zircon analysis uses the interpreted provenance to propose a geological history for sedimentary basins and their surrounding source regions (Fedo et al. 2003). Detrital zircons may be reworked through multiple sedimentary cycles and therefore are ubiquitous in sandstones; however, the abundance of detrital heavy minerals is controlled by sedimentary facies (Zimmermann et al. 2015). The durability of zircon is a challenge because multicycle sedimentation may be masked, leaving an incorrect interpretation of exclusively primary sources and compromising the interpretation of provenance (Thomas 2011). The highly quantitative and qualitative U-Pb dating of detrital zircons obtained by microanalysis techniques, such as laser ablation inductively coupled plasma mass spectrometry (LA-ICP-MS) and the imaging of the grain with a cathodoluminescence detector attached to a scanning electron microscope (SEM), permit the establishment of a direct link between the ages of hosted zircon grains from a sample and those of the several remaining rocks from multiple

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crystalline sources (Köksal et al.ACCEPTED 2008, Linnemann et al. 2011, Thomas 2011, Linol et al. 2014). MANUSCRIPT Thus, U-Pb dating of detrital zircons from sedimentary deposits allows recognition of the variations and heterogeneities of source areas, contributing to the investigation of paleogeographic and paleoenvironmental changes that affected the petroleum system of a sedimentary basin. The Parnaíba basin, located in the northeast region of Brazil (Goés and Feijó 1994, Góes 1995, Pedreira da Silva et al. 2003, Santos and Carvalho 2004, Vaz et al. 2007), presents the necessary conditions for the generation of hydrocarbons (source rock, reservoir, migration and traps) (Góes et al. 1990). The petroleum system of the basin includes, to a large extent, the Middle Devonian-Mississippian sequence of the Canindé Group. The main source rocks are shales of the Pimenteiras Formation, which are widely distributed and reach thicknesses greater than 500 meters (Góes et al. 1990). The reservoir rocks are the sandstones of the Cabeças Formation, and the seals are represented by shales of the Cabeças and Longá Formations (Rodrigues 1995).

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Fig. 1. The Parnaíba basin (NE Brazil) in a Gondwana paleogeographic reconstruction, showing the location of the study area (modified from Torsvik and Cocks 2013, Arthaud et al. 2015, Uriz et al. 2016).

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At the regional level, both the sedimentary environment of source/seal rocks and the quality of the Cabeças reservoir in this petroleum system have been considered relatively homogeneous. The alternation of sandstones and shales would be representative of transgressive-regressive cycles within a platform environment, influenced by glacial events (Caputo et al. 2006a, 2006b, Vaz et al. 2007). However, although scarce, studies such as those of Santos (2005), Young (2006) and Barbosa et al. (2015) indicate the existence of paleoenvironmental and paleogeographic variations along the basin. Such variations could interfere, for example, with the quality of the reservoirs, as

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well as the distribution of the source rocks. In addition, a provenance study for this specific ACCEPTED MANUSCRIPT sedimentary succession (Canindé Group) has not yet been reported. This work presents U-Pb dating of detrital zircons from the sedimentary successions that form the Middle Devonian-Mississippian petroleum system of the Parnaíba basin. The study was conducted in outcrops of the Canindé Group on the eastern border of the basin (Fig. 1). The geochronological data, along with the morphological and textural description of the detrital zircon grains, are used here to investigate the variations in the source areas and to propose a paleogeographic interpretation for the deposition of this sedimentary succession.

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2. GEOLOGICAL CONTEXT 2.1. PARNAÍBA BASIN

The 600,000 km2 Parnaíba basin is located in the northeastern portion of the South American platform (Fig. 2a), and the erosive limits of this basin are defined by Pan-African/Brasilian tectonic lineaments (Goés 1995). The evolution of the Parnaíba basin is related to the subsidence of the basement during the last pulses of the Brasiliano cycle (~550 Ma). This tectonism allowed the formation of graben structures, generating accommodation spaces filled by immature clastic sediments of the Riachão and Jaibaras Formations, which were overlain by the sediments of the Parnaíba basin (Cunha 1986, Vaz et al. 2007). The sedimentary record of this basin, with a thickness of 3500 m, comprises the following supersequences: Silurian (Serra Grande Group), Middle Devonian-Mississippian (Canindé Group), Pennsylvanian-Lower Triassic (Balsas Group), Jurassic (Pastos Bons Formation) and Cretaceous (Codó, Corda, Grajaú and Itapecuru Formations) (Fig. 2b; Vaz et al. 2007, Ballén et al. 2013).

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Fig. 2. (a) Northeastern portion of the South American platform, showing the vast area of the Parnaíba basin, which covers the states of Pará (PA), Tocantins (TO), Maranhão (MA), Piauí (PI) and Ceará (CE), in NE Brazil; (b) Simplified

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geological map of the Parnaíba basin (modified from Aguiar and Nahass 1969); (c) Geological map of the study area ACCEPTED MANUSCRIPT with sample locations (modified from Barbosa et al. 2015).

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Paleogeographical reconstructions associated with intense seafloor spreading in the evolutionary context of the Gondwana paleocontinent demonstrate that climatic events caused a global trend of rising sea level in the Devonian period, resulting in the formation of epicontinental seas and the deposition of sedimentary sequences with high transgressive trends (Torsvik et al. 2012, Torsvik and Cocks 2013). The Canindé Group of the Parnaíba basin records one of the most important marine incursions in the South American platform (Góes et al.1990, Vaz et al. 2007). The Canindé Group crops out in the east and southwest parts of the Parnaíba basin and comprises the Itaim (not sampled in this work), Pimenteiras, Cabeças, Longá and Poti Formations, constituting a complete transgressive-regressive cycle discordantly deposited on the Silurian sequence of the Serra Grande Group. The sedimentation of the Canindé Group begins with fine to medium sandstones interlayered with bioturbated shales and deposited in a deltaic to platform environment influenced by tide and waves. The sedimentary succession assembled in the Itaim Formation represents a transgressive event whose peak was reached during the deposition of the shales of the Pimenteiras Formation in a shallow platform environment dominated by storm waves (Góes and Feijó 1994). The Cabeças Formation follows the deposition of these basal units and presents, at the base, a depositional environment related to a platform under the action of tidal currents and storms (Della Fávera 1990, Góes and Feijó 1994); however, a fluvio-deltaic system has also been reported (Ponciano and Della Fávera 2009). Glaciogenic diamictites occur at the top of this formation (Kegel 1953, Loboziack et al. 2000, Caputo et al. 2008, Barbosa et al. 2015). This unit is covered by the Longá Formation, which is composed of shales with intercalations of fine sandstones deposited in a platform environment dominated by storm waves (Góes and Feijo 1994). The sedimentary cycle ends with the Poti Formation, presenting medium to fine sandstones with fine layers of siltstone deposited in deltaic to strand plain tidal flat environments under the influence of storm waves. The end of the sedimentation of this Middle Devonian-Mississippian sequence is marked by a disconformity associated with the effects of the Hercynian orogeny (Vaz et al. 2007).

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2.3. GEOLOGY OF SURROUNDING AREAS The surrounding cratonic areas of the Parnaíba basin in the South American platform (see the synthesis of events in Fig. 3) have numerous inliers and Archean blocks. Additionally, Paleoproterozoic crust is found extensively in all domains described above. However, rocks older than 2.3 Ga are not common, except in the Bacajá and Amapá domains and in the Carajás province, all of them in the Amazonian craton (Santos et al. 2006, Rosa-Costa et al. 2006, 2008, Vasquez et al. 2008). Few occurrences of Paleoproterozoic rocks (> 2.3 Ga) in the Borborema province have been reported. In addition, Siderian rock associations occur locally in the northern basement of the Brasília belt and probably extend to the northwestern portion of the São Francisco craton (Brito Neves et al. 2013). Orosirian rocks of the Amazonian craton are related to the Uatumã magmatic event (Klein et al. 2013). Moreover, ages of ~1.9 Ga are reported in the Rio Preto (Caxito et al. 2011) and Sergipano belts (Neves et al. 2006, Brito et al. 2008, 2010), suggesting the existence of an important Orosirian tectono-magmatic event in the northern border of the São Francisco craton (Caxito et al. 2013, 2015).

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2.2. CANINDÉ GROUP

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Older rocks of the SouthACCEPTED American platform reworked during the Pan-African/Brasiliano MANUSCRIPT tectono-thermal cycle are also inserted into the Brasiliano domain, in addition to the rocks formed during this event. However, taphrogenic processes affected these older rocks during the transition between the Late Paleoproterozoic and the Mesoproterozoic, which was characterized by the development of continental rifts and widespread deposition of sedimentary sequences intercalated with volcanic rocks (Brito Neves et al. 2014).

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Fig. 3. Geochronological panorama of the areas surrounding the Parnaíba basin. (1) Nutman and Cordani 1993; (2) Fetter et al. 2000, Silva et al. 2002, Dantas et al. 2004, 2013, Oliveira et al. 2010, and Santos et al. 2015; (3) Santos et al. 2006 and Reis et al. 2006; (4) Caxito et al. 2013; (5,20) Santos et al. 2015; (6) Fetter et al. 2000; (7) Melo et al. 2002, Santos et al. 2008a, and Brito Neves et al. 2013; (8) Fuck et al. 2014; (9,10) Rosa-Costa et al. 2006, 2008 and Vasquez et al. 2008; (11) Cruz et al. 2014; (12) Sá et al. 2002; (13) Neves et al. 2006 and Brito et al. 2008, 2010; (14)

Caxito et al. 2011; (15) Vasquez et al. ACCEPTED 2008, Juliani and MANUSCRIPT Fernandes 2010, Brito Neves 2011, Barreto et al. 2012, and Klein et al. 2013; (16) Sá et al. 1995, 1997 and Hollanda et al. 2011; (17) Santos et al. 2008a; (18) Accioly 2000 and Lages et al. 2013; (19,22,23) Babinski et al. 1999 and Danderfer et al. 2009; (21) van Schmus et al. 1995; (24) Tassinari and Macambira 1999, 2004 and Santos et al. 2008b; (25) Medeiros 2004, Santos et al. 2010, van Schmus et al. 2011, and Guimarães et al. 2012; (26) Aquino and Batista 2011; (27) Brito Neves et al. 2015; (28,33) Ganade de Araújo et al. 2014a; (29) Caxito et al. 2016 and Brito Neves et al. 2015; (30) Brito Neves et al. 2003, Ferreira et al. 2004, and Sial et al. 2008; (31) Laux et al. 2005 and Brito Neves et al. 2014; (32) Campos Neto and Caby 2000 and Dantas et al. 2006; (34) Ferreira et al. 2004 and Sial et al. 2008; (35) Ganade de Araújo et al. 2013.

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Late Mesoproterozoic primary sources are found in the southwestern Amazonian craton, especially in the Sunsás domain (Santos et al. 2008b, Tassinari and Macambira 1999, 2004). In contrast, these younger ages are not extensive or nonexistent in the Borborema province. Tonian terranes of the Borborema province are reported in the Central subprovince, more specifically in the Alto Pajeú terrane and Riacho Gravatá subterrane. These regions are envisaged as type areas of the Cariris Velhos event (Medeiros 2004, Santos et al. 2010, van Schmus et al. 2011, Guimarães et al. 2012). The Brasiliano collage was initiated in the Cryogenian (Brito Neves et al. 2014). However, superimposed juvenile magmatic and tectonic processes hamper the recognition of these early events. In the Cryogenian-Ediacaran interval, post-Rodinia or pre-Gondwana, a complex and varied scenario with collision and diachronic accretionary processes occurred in all Neoproterozoic structural provinces of the South American platform (Brito Neves et al. 2015). In a few cases, these processes were followed by intrusions of granitic and syenitic bodies (Ferreira et al. 2004, Sial et al. 2008). In other places (e.g., SE of Brasília belt), the collisional events were limited to the Ediacaran Period.

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The sedimentary successions of the Parnaíba basin were deposited within the paleogeographic context of the West Gondwana paleocontinent; therefore, the ages of the surrounding rock units from cratons and mobile belts presently in the African continent are briefly described (Fig. 1). The southern part of the West African craton (WAC; Fig. 1) consists of the Archean (>2.8 Ga) Kénéma-Man domain (Goujou et al., 1999; Thiéblemont et al., 2001; Camil et al., 1983; Kouamelan et al., 1997; Cocherie et al., 1998), affected by the Leonian (2.9-3.0 Ga) and Liberian (2.7-2.8 Ga) cycles (Mac-Farlane et al., 1981; Camil et al., 1983; Egal et al., 2002). This Archean domain is juxtaposed against the Paleoproterozoic Baoulé-Mossi domain. This Paleoproterozoic domain (>2.0 Ga) is made up of greenstone belts, sedimentary basins and regions of extensive granitoid plutons of tonalite-trondhjemite-granodiorite (TTG) affinity (Davis et al., 1994; Lüdtke et al. 1999; Doumbia et al., 1998; Baratoux et al., 2011; Perrouty et al., 2012, Jessell et al., 2016). The Paleoproterozoic domain was established and structured during the Eburnean (2.2-2.0 Ga) cycle (Bonhomme, 1962; Egal et al., 2002). The Late Neoproterozoic Dahomeyan and Pharusian terranes of the Trans-Saharan orogenic belt define the eastern boundary of the WAC (Black et al., 1979; Black and Liégeois, 1993; Jessell et al., 2016). The Nigerian shield comprises a polycyclic (>2.5 Ga) basement and remnants of metamorphic cover sequences preserved in large synforms and schist belts (Caby 1989; Caby & Boessé, 2001). This shield, exposed east of the Transbrasiliano-Kandi lineament (Arthaud et al 2008), was largely reworked during the multistage Pan-African orogeny (Grant 1978; Mullan 1979; Caby 1989). The Congo craton (CC; Fig. 1) was linked with the São Francisco craton during the Erbunean orogeny to form a single large mass of continental crust, which was later wrapped by

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2.3.1. Adjacent African areas

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The basement of the Parnaíba basin was formed by crustal collisions involving cratonic blocks and includes extensive Neoproterozoic fold belts and concealed (Parnaíba block) basement inliers (Oliveira and Mohriak, 2003; Cordani et al., 2013). Remnant areas of the complex evolution of West Gondwana are found in the Borborema (BP) and Tocantins (TP) provinces (Ganade de Araujo, 2014). However, before the beginning of the tectonic evolution of these provinces during the Neoproterozoic, the older terranes of the BP affected by the Cariris Velhos event and the Parnaíba block were separated from the Amazonian-West African craton by the Gurupi and Araguaia belts (Neves, 2003; Klein et al., 2005; Moura et al., 2008; de Castro et al., 2013). The West Gondwana orogen (WGO) developed along the Transbrasiliano-Kandi lineament as a result of collision of the Amazonian-West African block with the Central African block and the closing of the Pharusian-Goias Ocean in the Early Neoproterozoic (Ganade de Araujo, 2013). The Brasiliano-Pan African orogenic belts that formed during this process (Cordani et al., 2013) permitted the direct interaction between the above mentioned regions. The WGO includes the Trans-Saharan orogen (Hoggar and Dahomey belts), the west limit of the BP (Ceará Central domain) and the north portion of the TP (Brasilia belt). The closure of the Sergipano-Oubanguides Ocean, which separated the PernambucoAlagoas massif from the São Francisco-Congo craton (Oliveira et al., 2010) in the late Neoproterozoic, led to the development of inboard orogenic basins in the southern Borborema province (e.g., van Schmus et al., 2003; Ganade de Araujo et al., 2013; Caxito et al., 2017). As a result, the amalgamation of cratonic fragments and the incorporation of accretionary complexes into mobile belts occurred (Dalziel, 1997; Oliveira and Mohriak, 2003; Cordani et al., 2013). In this context, the Southern subprovince (Rio Preto, Riacho do Pontal and Sergipano fold belts) represents a continental-scale orogenic system that extends along the northern margin of the São Francisco craton (Caxito et al., 2017). The Araguaia suture zone, presently overlain by the allochthonous Araguaia belt, represents the final Neoproterozoic collision between the Amazonian craton and the Parnaíba block (Brito Neves and Fuck, 2014). The Gondwana supercontinent underwent tectono-thermal reactivation during the Ediacaran-Cambrian. In addition, Late Cambrian-Early Ordovician rifting and magmatic episodes occurred in West Gondwana, but they did not result in continental breakup (Cordani et al, 2013). Early Paleozoic cratonic basins, such as the Parnaíba basin, formed along the failed rifts and occupied large regions (de Castro et al., 2016).

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2.3.2. Pan-African/Brasiliano orogens

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Pan-African-Brasiliano orogenic ACCEPTED belts (Trompette 1994, 2000). Archean rock units (3.1-2.7 Ga) in MANUSCRIPT the SW Congo craton are found in the Chaillu and Gabon blocks (Feybesse et al., 1998), followed by (2.8-2.5 Ga) late orogenic granites (Feybesse et al., 1998).

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3. METHODS 3.1. SAMPLING

The studied deposits are located in the eastern border of the Parnaíba basin. They are distributed along the BR-316 and BR-230 interstate roads in the states of Maranhão and Piauí. According to the characterization of architectural, mineralogical and facies attributes of the analyzed sedimentary rocks, six composite columnar sections were constructed (Fig. 4). They represent a siliciclastic succession composed of diamictites, intraformational breccias, fine to coarse sandstones and fine to very fine sandstones, interdigitated with pelites and mudstones. The outcrops are ~3 to 10 m in height and a dozen meters in lateral extent and are representative of the

Pimenteiras, Cabeças, Longá andACCEPTED Poti Formations. In total, six sandstone samples of approximately MANUSCRIPT 10 kg each, representative of these lithostratigraphic units, were collected.

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Fig. 4. Columnar sections of the Canindé Group in the eastern border of the Parnaíba basin and sample locations for UPb zircon analysis (profile 3* after Barbosa et al. 2015).

Sample CC04 (-7,07758; -41,4838333) corresponds to the offshore-shoreface middle deposit (Af1 association) of the Pimenteiras Formation. This succession is exposed in the eastern part of the

study area near the cities of Pimenteiras and Picos and is representative of terrigenous platforms ACCEPTED MANUSCRIPT with bars (offshore bars) dominated by storms (Fig. 5a; Santos and Carvalho 2004).

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Fig. 5. (a) Tempestite deposit of the Pimenteiras Formation, Picos City; (b) Subglacial deposit (3) intercalated with and of erosive character in relation to the deltaic front (1) of the Cabeças Formation, Oeiras City; (c) Deposit of deltaic front of the Longá Formation near Nazaré do Piauí City; and (d) Deposit of channel bars of the Poti Formation, Barão do Grajaú City.

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Samples CC06 (-6,34525; -41,6087222) and CC03 (-7,01706; -42,1489958) are from the Cabeças Formation. Sample CC06 was collected near Valença do Piauí City, where the deposits exhibit more proximal features indicated by the large thickness of sigmoidal lobes (Af4 association). Sample CC03 was collected near Oeiras City in a distal deltaic front deposit (Af3 association). Subglacial deposits (Af2 association) are intercalated, with erosive character, in the Af3 association (Fig. 5b). The Af4, Af3 and Af2 associations correspond to a glacio-deltaic system (Barbosa et al. 2015).

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Sample preparation and U-Pb dating of 6 sandstones were performed at the Isotope Geology Laboratory (Pará-Iso) of the Geoscience Institute of the Federal University of Pará (IG-UFPA). The samples were fragmented, disaggregated and wet-sieved at 250-125 µm intervals (medium to fine sand), following the methods described by Lawrence et al. (2011). The samples were then panned, washed with 10% HCl and dried in an oven. The heavy minerals were concentrated with bromoform. The detrital zircons were identified and separated by handpicking under a binocular microscope and mounted in epoxy resin (~100 grains in each mount). After the zircon grains were polished, SEM cathodoluminescence (SEM-CL) images were obtained at the laboratory facility of the Brazilian Geological Survey (CPRM-Belém) and at the Microanalyses Laboratory of IG-UFPA. Information about internal textures allows the identification and classification of zircon populations, improving the control of the geochronological data of several crystal domains (Morton et al. 1996, Corfu et al. 2003, Kosler and Sylvester 2003). Additionally, information from SEM-CL images (zoning, recrystallization, metamictization, alteration, etc.) allows the identification of both magmatic textures, such as oscillatory zoning produced by alternation of U-rich and U-poor halos (low and high luminescence, respectively), and metamorphic zircons with nonoscillatory zoning and homogeneous internal textures, caused by destruction of former igneous textures (Corfu et al. 2003).

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3.2. SAMPLE PREPARATION

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In the study area, the Longá Formation isMANUSCRIPT restricted to the surroundings of Nazaré do Piauí ACCEPTED City. Sample CC02 (-6,98328; -42,5235083) was collected from an outcrop featuring offshoreshoreface deposits (Fig. 5c; Af5 association). Correlations with other units suggest a shallow marine environment for the Longá Formation (Santos and Carvalho 2004). From the Poti Formation, samples CC05 (-6,10481; -42,2120278) and CC01 (-6,68773; 43,2582308) were collected. The former was sampled in the surroundings of Elesbão Veloso City from an exposure with characteristics of offshore-shoreface marine deposits (Af6 association). Sample CC01 was collected in channel bar deposits (Fig. 5d; Af7 association) near the city of Barão Grajaú (MA). The Af6 association represents the basal portion of the Poti Formation and has been interpreted as a shallow-water depositional environment in the shoreface zone with storm wave activity (Goés 1995). In contrast, the Af7 association represents sandy bars of a braided fluvial system belonging to the top of the Poti Formation.

3.3. ZIRCON GEOCHRONOLOGY

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All U-Pb isotope analyses were performed using a high-resolution Neptune Thermo Finnigan multicollector inductively coupled plasma mass spectrometer (MC-ICP-MS) equipped with a Nd: YAG 213 nm LSX-213 G2 CETAC laser ablation (LA) microprobe at the Pará-Iso. The methodology applied essentially follows that described by Dias et al. (2017) and Milhomem Neto et al. (2017). U-Pb dating of detrital zircons from the Canindé Group furnished 39-98 measurements, following the suggestion of Andersen (2005). This researcher indicated that the potential information contained in detrital zircons should be extracted from a random fraction comprising 3570 grains or more, depending on the complexity of the age distribution. The operating conditions and instrument settings of MC-ICP-MS and laser ablation system during analytical sessions are listed in Dias et al. (2017, see Table 1 from this author). All data were acquired with single spot analyses on individual zircon grains using a 25 µm spot size. Spot analyses were performed in groups with 10 determinations interspersed with standard GJ-1 (608.5 ± 1.5 Ma; Jackson et al.

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U-Pb analyses by LA-MC-ICP-MS were performed on 543 grains (see supplementary data file). Concordant U-Pb ages (90% to 110%) were obtained in 394 zircon grains. Frequency histograms combined with curves of the relative probability of 207Pb/206Pb ages of the concordant grains are shown in Figures 6 and 7. Internal structures revealed by SEM-CL of some concordant zircon grains are shown in Figure 8.

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4. RESULTS 4.1. U-Pb AGES AND INTERNAL STRUCTURES

4.1.1. Pimenteiras Formation

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2004). Blank values were acquired after analyses of each standard + sample block. Common lead ACCEPTED MANUSCRIPT 204 ( Pb) interference and background correction is normally carried out by monitoring the 202Hg and 204 (Hg + Pb) masses during analytical sessions and using a model Pb composition (Stacey and Kramers 1975). After blank and common Pb corrections, the ratios and their absolute errors (onesigma level) of 206Pb/238U, 232Th/238U, and 207Pb/206Pb were calculated using an Excel spreadsheet (Chemale Jr. et al. 2012). Age calculations and the presentation of isotopic results were performed using the Isoplot/Ex software (Ludwig 2003). Analyses with 90-110% concordance are considered concordant for the interpretation of zircon data. A large proportion of the zircons analyzed yielded discordant results. In a number of cases, this discordance resulted in meaninglessly low 206Pb/238U ages; therefore, we report our data as 207Pb/206Pb ages that are considered minimum ages for discordant analyses (Kalsbeek et al. 2008). The results are shown in age probability diagrams combined with frequency histograms produced using Age Display (Sircombe 2004). The K-S test was applied to a set of radiometric data using all 207Pb/206Pb ages, with the software made available by the Geochronological Center of Arizona University (Guynn and Gehrels 2010). The age patterns of concordant analyses are not significantly different from the age patterns of all analyses, suggesting that the 207Pb/206Pb ages can be used with confidence to constrain the sedimentary provenance and stratigraphic context of the studied rocks (Fernandez-Suarés et al. 2013).

U-Pb dating of 143 grains from the CC-04 sample furnished 98 concordant ages between 3443 Ma and 438 Ma (Fig. 6a). Zircons with Cambrian ages (538-486 Ma) are the most abundant, with 20% concordant grains. In the Neoproterozoic, two groups are predominant: Tonian zircons (15%) with ages of 955-722 Ma and Ediacaran zircons (14%) with ages from 624 Ma to 547 Ma. Paleoproterozoic zircons (2428-1672 Ma) may also be assembled into two main groups: Rhyacian ages (10%) between 2299 Ma and 2067 Ma and Orosirian ages (12%; 2042-1820 Ma). Archean (6%; 3443-2530 Ma), Mesoproterozoic (7%; 1597-1089 Ma) and Ordovician-Silurian (3 grains only; 486 Ma, 478 Ma and 438 Ma) zircons were also found. Plots in diagrams of relative probability illustrate a major peak at 520 Ma and three smaller peaks at 800 Ma, 2000-2050 Ma and 2410 Ma (Fig. 7a). SEM-CL images of Siderian grains reveal internal parts partially obliterated by recrystallization or metamictization and locally irregular shapes highlighted by CL bright lines but preserved faint growth zoning (H3 and E7*). The internal parts of Rhyacian grains have been almost completely obliterated by metamictization (A5) or form a homogeneous unzoned core (D5) surrounded by a large CL-bright rim (Fig. 8a). Occasionally, these grains show a faint and broad zoning locally overprinted by zones of metamictization (I2). The Orosirian grains exhibit internal parts entirely (E8*) or partially obliterated by recrystallization or/and metamictization with

AC C

302 303 304 305 306 307 308 309 310 311 312 313 314 315 316 317 318 319 320

pronounced fractures; however, ACCEPTED they preserved MANUSCRIPT a faint oscillatory concentric (F3) or broad (H2) zoning. Cryogenian grains show predominantly weak diffuse zoning completely obliterated by recrystallization and locally overprinted by zones of metamictization (D4*, H8, and E2). Ediacaran grains display recrystallization patches that emphasize the loss of growth zoning (F6* and J5); occasionally, the internal part preserves a faint oscillatory concentric zoning (G1*). Cambrian grains show diverse contingent internal shapes, with typically magmatic growth zoning (C1 and G4), and display cores obliterated by metamictization surrounded by thick CL-bright rims (I8) or with variation in the growth zoning (D2).

354 355 356

357 358 359 360 361 362

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346 347 348 349 350 351 352 353

Fig. 6. Frequency histograms and probability curves of detrital zircon ages obtained by LA-MC-ICP-MS from sandstone samples of the Canindé Group.

4.1.2. Cabeças Formation The samples CC06 and CC03 (50 and 69 zircon grains) present 39 grains (2558-537 Ma) and 46 grains (2784-478 Ma), respectively, with concordant ages (Fig. 6b-c). Zircons with Orosirian ages (2034-1830 Ma) are the most abundant, accounting for 28% of the concordant grains. In the Mesoproterozoic, only Stenian zircons (15%), with ages of 1121-1013 Ma, are found. Tonian ages between 977 Ma and 750 Ma (15%) are predominant among the Neoproterozoic

zircons. Neoarchean (8%; 2784-2558 Ma), Cambrian (537 Ma and 522 Ma; 2 grains only) and ACCEPTED MANUSCRIPT Ordovician (478 Ma; only one grain) zircons are also present in these samples. Both samples show important Stenian, Tonian and Orosirian detrital zircon contributions. Sample CC06 exhibits dominantly Orosirian grains and a significant presence of CryogenianEdiacaran zircons. However, sample CC03 exhibits dominantly Stenian-Tonian grains with noteworthy Ediacaran contributions. The diagram of the relative probability for the Cabeças Formation shows a major peak at 1030 Ma and three smaller peaks at 547-575 Ma, 967 Ma and 1884 Ma (Fig. 7b).

371

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363 364 365 366 367 368 369 370

Fig. 7. Paleoenvironment, morphology, frequency histograms and probability curves of detrital zircon ages from the Pimenteiras, Cabeças, Longá and Poti Formations (age and system boundaries after the IUGS International Stratigraphic Chart).

375 376 377 378 379 380 381 382 383 384 385 386 387

Orosirian grains exhibit internal parts partially obliterated by recrystallization or metamictization (Fig. 8b). However, preserved oscillatory concentric zoning, occasionally surrounded by thick CL-bright intensity rims (D9 and E1) or covered by an extremely thin CL-dark rim (F3 and K2), is observed. Stenian grains show diverse contingent internal shapes, displaying preserved oscillatory concentric zoning locally overprinted by zones of recrystallization. Inclusions commonly appear (K8). Very irregular concentric zoning, almost entirely overprinted by zones of recrystallization (I10), is present. Sometimes, this zoning is completely obliterated by recrystallization or metamictization, forming a homogeneous unzoned zircon (I5). Tonian grains are partially obliterated by recrystallization or metamictization. However, they preserve growth zoning (J7), occasionally surrounded by thin CL-bright rims (G5). Cryogenian grains show predominant weak diffuse zoning completely obliterated by recrystallization, locally overprinted by zones of metamictization (G2). Xenocrystic cores surrounded by homogeneous unzoned rims (F7°) are rare. Ediacaran grains show typical magmatic growth zoning with faint oscillatory concentric zoning.

AC C

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372 373 374

390

4.1.3. Longá Formation The U-Pb data of 75 zircons from CC02 show 54 concordant ages between 2682 Ma and 415 Ma (Fig. 8d). Paleoproterozoic (2002-1670 Ma) and Neoproterozoic (999-542 Ma) zircon grains are predominant at 26% and 39%, respectively. Subordinate Stenian grains (12%) with ages of 1190-1003 Ma are identified. Two Neoarchean (2682 Ma and 2515 Ma), two Cambrian (502 Ma and 492 Ma), three Ordovician (473 Ma, 473 Ma and 458 Ma) and one Lower Devonian (415 Ma) zircon grains are also present. Plots in the relative probability diagram (Fig. 9c) show major peaks at 1005 Ma, subordinate peaks at 473 Ma, and minor peaks at 662 Ma, 1754 Ma and 1845 Ma.

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391 392 393 394 395 396 397

The internal parts also present inclusions (F1) and broad zoning with pronounced parallel partitions ACCEPTED MANUSCRIPT (J10).

RI PT

388 389

398

Fig. 8. Cathodoluminescence images of representative analyzed zircon grains from sandstones of the Canindé Group. Circles mark spots (25 µm in size) analyzed by LA-MC-ICP-MS.

401 402 403 404 405 406 407 408 409 410 411

SEM-CL imaging reveals that the Orosirian grains show a complex history of development (Fig. 8c). They display recrystallization patches, which emphasize the loss of growth zoning (J5), locally overprinted by zones of metamictization and occasionally surrounded by CLbright rims (F8). Statherian grains exhibit internal parts that are almost completely obliterated by recrystallization or metamictization, forming homogeneous an unzoned core (G3) overlain by an extremely thin CL-dark rim or a large metamictic core (xenocrystic core) and strongly fractured rim (E4). Stenian grains have partially preserved growth zoning that is penetrated by zones of recrystallization. Locally, these grains have irregular shapes accentuated by CL-bright lines (E9), patchy texture (G1), and large CL-dark rims surrounding metamict corroded layers. Cryogenian grains are very fractured (E3) and show a predominant weak diffuse zoning completely obliterated by metamictization; however, they seldom exhibit typically magmatic broad growth zoning (C3).

412

AC C

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399 400

4.1.4. Poti Formation

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440 441 442 443 444 445 446 447 448 449 450 451 452 453 454 455 456 457

4.2. PROVENANCE PATTERNS

U-Pb ages obtained in the detrital spectrum of the Canindé Group, diagrams of density distribution (probability), percentage discriminated in pie diagrams and applications of the Kolmogorov-Smirnov test (K-S; Fig. 9) allow the comparison and/or differentiation of specific provenance patterns. In addition, the K-S test is applied to establish the degree of similarity among the studied lithostratigraphic units. This test compares the age distributions of detrital zircons of two samples from different geological formations in order to identify whether both were drawn from the same population (de Graaff-Surpless et al. 2003). The studied zircon populations demonstrate a heterogeneous distribution, with a predominance of Paleoproterozoic sources (especially Orosirian) in relation to Archean sources. On the other hand, the Mesoproterozoic (especially Stenian), Neoproterozoic (mainly Tonian and Ediacaran) and Cambrian contingents participate in different proportions in the studied units. The CC02 sample (Longá Formation) has a wide detrital spectrum, with ages ranging from Cambrian to Archean, and the P values of the K-S test show that this sample is not significantly different from samples CC01 and CC05 (Poti Formation), CC06 (Cabeças Formation) and CC04 (Pimenteiras Formation) (Fig. 9a). In turn, sample CC-06 is not significantly different from sample CC05. Sample CC03 (Cabeças Formation) is significantly different from the other samples but not significantly different from sample CC-06 (same geological unit). In sample CC03, there is a lack of Cryogenian and Late Tonian zircon grains. Sample CC04 is significantly different from the other

EP

439

Samples CC05 and CC01 (85 and 89 zircon grains, respectively) show concordant ages in ACCEPTED MANUSCRIPT 80 grains (2771 Ma and 485 Ma) and 77 grains (2740 Ma and 429 Ma), respectively (Fig. 6e-f). These two samples have dominant zircon populations with Stenian ages (22%) between 1187 and 1000 Ma and Neoproterozoic grains with mainly Tonian (26%; 999-722 Ma) and Ediacaran (12%; 628-542 Ma) ages. Paleoproterozoic zircons with Orosirian (8%; 2037-1815 Ma) and Statherian (7%; 1776-1638 Ma) ages also occur. Cambrian zircons (8%; 540-485 Ma) and one Silurian grain (429 Ma) are also present. In addition, Neoarchean (4%; 2771-2.518 Ma) grains are found. Both samples show important Stenian-Tonian detrital contributions. However, sample CC01 has a significant Ediacaran contribution not shown in sample CC05. The probability diagram for the Poti Formation samples reveals a major peak at 1033 Ma and, subordinately, 3 minor peaks at 536 Ma, 600-627 Ma and 900 Ma (Fig. 7d). SEM-CL images (Fig. 8d) show that Orosirian zircons preserved growth zoning (C4° and G5°). Locally, the grains are penetrated by zones of recrystallization and/or metamictization and occasionally exhibit core-rim texture (D2°). Some zircon grains may also present an internal CLbright core with concentric zoning truncated by an outer CL-dark rim with an irregular broad oscillatory zone (D2º). Stenian grains have partially preserved growth zoning that is penetrated by zones of recrystallization, locally overprinted by zones of metamictization (J8°, D7°, and C9°). They also exhibit internal parts completely obliterated by recrystallization, forming chaotic zones (F6*). Unzoned grains locally appear with irregular dashed shapes from CL-bright lines and micro veining (J2). Tonian grains are partially obliterated by recrystallization or metamictization, with slightly preserved growth zoning (C7). They also display recrystallization patches that emphasize the loss of growth zoning (F5°) and chaotic zoning core surrounded by an intense CL-bright oscillatory zoning rim (A3). Cryogenian grains show predominantly weak oscillatory zoning obliterated by recrystallization, locally overprinted by zones of metamictization (K4°), and abundant fractures (B2°). Ediacaran grains display recrystallization patches that emphasize the loss of growth zoning (H7), locally overprinted by broad zones of metamictization (I3).

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413 414 415 416 417 418 419 420 421 422 423 424 425 426 427 428 429 430 431 432 433 434 435 436 437 438

samples but not enough significantly different from samples of the Poti and Cabeças Formations. ACCEPTED MANUSCRIPT Despite the large numbers of Ediacaran-Cambrian and/or Tonian detrital zircon ages in the CC04, CC05 and CC01 samples, Neoproterozoic sources are commonly found in all analyzed samples. Considering the lithostratigraphic units, in general, the Longá Formation is not significantly different from the Poti and Pimenteiras Formations. Additionally, there is not enough significant difference between the Pimenteiras and Poti Formations (Fig. 9b). However, these two units are significantly different from the Cabeças Formation, which in turn is not significantly different from the Longá Formation (P-values in Fig. 9c-d).

AC C

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458 459 460 461 462 463 464 465

466

Fig. 9. (A) Probability p of two samplesACCEPTED being derived from the same population. (B) Probability p of two formations MANUSCRIPT showing similar populations. (C-D) Tables with results of the Kolmogorov–Smirnov test applied to the U-Pb ages of detrital zircons from the Middle Devonian-Mississippian sandstones of this study (Parnaíba basin). Barbeau et al. (2009) suggested a p value of 0.05 for provenance studies with a 95% confidence interval.

471 472 473 474 475 476 477 478 479 480 481 482 483 484 485

The predominance of Cambrian ages in the Pimenteiras Formation suggests a main contribution from rocks of this age to this sedimentary succession. In addition, zircon populations of Paleoproterozoic and Mesoproterozoic ages are present in similar proportions in this unit. Particularly, this formation has rare Paleo- and Mesoarchean grains, and among the studied units, is the only one that presents few Stenian zircon grains. The Cabeças Formation, which succeeds the Pimenteiras Formation, presents a zircon population of Siderian age, which is also identified in this last unit. However, in the Cabeças Formation, zircons of Paleoproterozoic age predominate, and there is a considerable increase in Stenian and Tonian zircon grains. Furthermore, the Archean grains are exclusively of Neoarchean age, as in the Longá and Poti Formations. The zircon populations of Neoproterozoic and Paleoproterozoic ages in the Longá Formation are equivalent in proportion. The number of Cambrian zircon grains is smaller than those in the Pimenteiras and Cabeças Formations. In turn, the Statherian zircon population is much higher. The Poti Formation shows a predominance of Neoproterozoic over Paleoproterozoic zircon populations, as well as an important contribution of Stenian and a significant increase in Cambrian grains.

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The history of the sag Parnaíba basin (Fig. 10a) involves long-term accumulation of terrestrial and shallow-water marine sediments starting at the end of the Brasiliano collage that resulted in the formation of the Gondwana supercontinent. The Araguaia belt and the mega shear zone known as the Transbrasiliano lineament (TBL) played important roles in this collisional scenario (Neves, 2015, de Castro et al., 2016). The amalgamation of West Gondwana involved continental subduction at mantle depths and the formation of mountain chains along the TBL in the Late Ediacaran (Ganade de Araujo et al., 2014). Additionally, during the Cryogenian-Early Ediacaran, Brito Neves et al., (2016) and Neves (2018) suggested a magmatic arc in the Central subprovince. Postorogenic tectonic inversion occurred during the Late Neoproterozoic and Early Paleozoic, forming a set of troughs and sag-related deposits on a failed rift system (de Castro et al., 2016). East of the TBL (Fig. 8b), the rifting process was mainly controlled by NE-SW ruptile structures associated with this lineament, primarily along the crustal boundary between the Parnaíba block and the Neoproterozoic Borborema province (de Castro et al., 2016). Large parts of these orogens were already deeply eroded and even flattened at the onset of Silurian-Devonian postorogenic sedimentation. Destro et al. (1994) suggested that late orogenic molassic deposits (Ediacaran-Cambrian) formed in a narrow graben. Oliveira and Mohriak (2003) interpreted this structure as a post-Brasiliano orogeny aborted rift before the sag subsidence of the intracratonic Parnaíba basin in the Silurian. The TBL controlled the main depositional axis of the Parnaíba basin between the Silurian and Mississippian Periods (Góes 1995). A relationship between the sedimentation of the basal sequences of the Parnaíba basin (Serra Grande Group and base of the Canindé Group) and the detrital fragments inherited from these Neoproterozoic belts has already been suggested (Ganade de

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488 489 490 491 492 493 494 495 496 497 498 499 500 501 502 503 504 505 506 507 508 509 510

5. DISCUSSION 5.1. TECTONIC CONTROL

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467 468 469 470

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Araújo et al., 2012, Maia and Bezerra, 2014). However, the influence of the Brasiliano structures in ACCEPTED MANUSCRIPT the paleolandscape of the Borborema province is only indirect (Peulvast and Betard 2015). In the eastern border of the Parnaíba basin (Serra da Ibiapaba and many regions of Ceará State), the Silurian Serra Grande Group overlies a set of Cambrian-Ordovician grabens related to reactivation along the Sobral shear zone (Oliveira and Mohriak 2003; de Castro et al., 2014), which is the northern segment of the TBL. These deposits represent part of the geographically and stratigraphically discontinuous sedimentary cover of Borborema province (Peulvast and Bétard 2015). Menzies et al. (2018) showed an important Brasiliano age detrital zircon population (~550 Ma) for the Serra Grande Group in the eastern portion of the Parnaíba basin. This population suggests a nearby source that might have been exposed during late orogenic or prerift movements (Martill 1993).

AC C

511 512 513 514 515 516 517 518 519 520 521

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ACCEPTED MANUSCRIPT

522 523 524 525 526 527 528 529

Fig. 10. (a) Geochronological overview of the areas surrounding the Parnaíba basin (Hasui, 2012); (b) Eastern portion of the Parnaíba basin highlighting the surrounding terranes of the Borborema province and the São Francisco craton. (van Schmus et al. 1995, 2011, Sá et al. 1995,1997, Fetter et al. 2000, Medeiros 2004, Neves et al. 2006, Brito et al. 2008, Santos et al. 2010, Guimarães et al. 2012, Brito Neves 2013, Caxito et al. 2014, Santos et al. 2015). (1a) Northern subprovince: Médio Coreaú domain (MC); Ceará Central domain-Acaraú terrane (AC) and Cearense terrane (CE); Rio Grande do Norte domain-Jaguaribeano-Encanto belt (JE), Rio Piranhas massif (RP), Seridó belt (SB) and São José do Campestre massif (JC); (1b) - Central subprovince: Piacó-Alto Brígida terrane (PB), Alto Pajeú terrane (AP),

Alto Moxotó terrane (AM) and Rio Capibaribe terrane (RC); and (1c) - Southern subprovince: Sergipano belt (SFB), ACCEPTED MANUSCRIPT Pernambuco-Alagoas massif (PEAL) and Riacho do Pontal belt (RPF).

532 533 534 535 536 537 538 539 540 541 542 543 544 545 546 547 548 549 550 551 552 553 554 555 556

Silva et al. (2014) suggested reactivation of TBL during the Lower Devonian, resulting in the establishment of grabens in the Borborema province. The abrupt change in the zircon age distribution curves between the Pimenteiras and the base of the Cabeças deposits (Fig. 6) may be associated with this episodic and restricted tectonic activity. With the reduction of tectonic activity during the Middle Devonian (post-Pimenteiras Formation), the sedimentation was controlled mainly by glacio-eustatic dynamics associated with the migration of glaciation centers in the continental portions of Gondwana (Torvisk and Cocks 2013). The fluvial and deltaic facies paleocurrent patterns are better observed in the Serra Grande, Cabeças and Poti Formations (Goes 1995; Barbosa et al., 2015, Hollanda et al., 2014, Linol et al., 2016, Menzies et al., 2018 and this work). On the eastern edge of the Parnaíba basin, the main paleofluxes trend NNW; however, along the TBL, the paleofluxes trend NE and SE (Fig. 10b). Thus, as indicated by the paleocurrents, the source area of the studied sedimentary deposits (Fig. 4) was the Borborema province, with a slight contribution from the Tocantins province. Comparison of the age spectra of the dated samples shows a clear shift in provenance during the deposition of the studied units. The Pimenteiras Formation displays an essentially unimodal pattern, suggesting derivation mostly from nearby young sources in the Borborema province. The rock units of this province were also available throughout the deposition of the Cabeças Formation, but the appearance of 1.9 Ga and 1.0 Ga age components suggests the contribution of distal sources in the Amazonian craton and Central-Southern subprovinces of Borborema. Alternatively, the reworking of the orogenic system (Fig. 11a) of the Southern subprovince (including the Rio Preto belt interpreted by Caxito et al., 2017) would explain the presence of this Orosirian zircon population. However, the U-Pb methodology employed does not allow the identification of sedimentary recycling mechanisms (Hollanda et al., 2014). During the sedimentation of the fluvial deposits of the Poti Formation, there was dominant input of sediments from the younger Neoproterozoic rock units, suggesting another possible reactivation.

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The age distribution of the zircon population in the Canindé Group suggests minor Archean but important Neoproterozoic and Mesoproterozoic (except Pimenteiras formation) detrital zircon contributions. However, it is difficult to infer direct sources for the sediments of this group, since the different textures identified in the zircon grains indicate possible mixing of magmatic and metamorphic origin. In addition, the transitional depositional environment of the Pimenteiras and Longá Formations (offshore-shoreface) most likely induced the mixing of distal and proximal sources on the terrigenous platform (Fig. 7). According to evolutionary models of marine transgression in the South American platform during the Middle Devonian (Almeida and Carneiro 2004, Torvisk and Crock 2013), the Borborema province was almost completely flooded, with the exception of a small exposed portion to the east and south of the Parnaíba basin. Therefore, the main contributions of proximal Archean and Paleoproterozoic zircons (3.4-2.0 Ga) for the Pimenteiras Formation came from the northwestern part of São Francisco craton and the external area of the Riacho do Pontal belt (3.2- 2.0 Ga; Angelin 2001, Barbosa et al. 2003, Dantas et al. 2010), with possible inputs from the southern portion of the Sergipano belt (3.4-2.8 Ga; Oliveira et al. 2006). However, distal sources (3.0-1.8 Ga) located in the east-central portion of the Amazonian craton (Tassinari and Macambira 2004, Santos et al. 2006, Reis et al. 2006, Vasquez and Rosa-Costa 2008, Juliani and Fernandes 2010, Brito Neves 2011,

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558 559 560 561 562 563 564 565 566 567 568 569 570 571 572 573 574

5.2. POTENTIAL SOURCE AREAS

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557

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530 531

Barreto et al. 2012, Klein et al. 2013) and the Western African craton (Lemoine et al. 2006) were ACCEPTED MANUSCRIPT also available.

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575 576

577

Fig. 11. (a) Main cratonic blocks and mobile belts of West Gondwana, with the location of the north-northeastern portion of the South American platform; (b) Comparative distribution curves of U-Pb ages of the Canindé Group and possible source areas (*van Schmus et al. 2003, 2011, Nascimento 2005, Neves et al. 2006, 2009, 2012, Ganade de Araújo et al., 2010, 2012, Guimarães et al. 2012, Caxito et al., 2011, 2014a,2014b, Kalsbeek et al. 2013, Cruz et al. 2014, Da Silva Filho et al. 2014, Garcia et al. 2014, Neves et al., 2015a, 2015b, Brito Neves et al. 2015).

583 584 585 586 587 588 589 590 591 592 593 594 595 596 597 598 599

The most extensive events of crustal formation in the areas surrounding the Borborema province occurred in the Rhyacian (2.2-2.0 Ga), related to the Transamazonian (Amazonian craton) and Eburnian (Western African craton) orogenies (Ganade de Araújo et al. 2012). Despite the extensive Orosirian magmatism (1.9-1.8 Ga) in the Amazonian craton (Klein et al. 2013), zircon ages of approximately 1.9 Ga in the basement rocks of the surrounding belts of the São Francisco craton (Sergipano and Rio Preto belts) suggest the existence of an Orosirian tectono-magmatic event in the northern border of the São Francisco craton (Caxito et al. 2013, 2015). This event would support the contribution of Orosirian zircons in the Pimenteiras Formation. However, distal source areas from the Amazonian and/or African domains cannot be discarded (Fig. 12.1) The rocks of the Monte Orebe complex in the Riacho do Pontal belt have been dated between 819 Ma and 792 Ma (Brito Neves et al. 2015); thus, these areas may have provided the Late Tonian zircons for the Pimenteiras Formation. The lack of obvious proximal sources may suggest distal sources related to the Trans-Saharan belt, within which Neoproterozoic terranes (870700 Ma) have been widely reported for the segment from Hoggar to Dahomeyan (Caby 2003, Berger et al. 2011). The significant Neoproterozoic and Cambrian populations between 620 and 500 Ma in the Pimenteiras Formation and the typical magmatic textures of the zircon grains identified by SEM-CL

AC C

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578 579 580 581 582

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images suggest a source relatedACCEPTED to the Brasiliano domains. In such cases, there is a possible MANUSCRIPT relationship with the outer zone of the Riacho do Pontal belt, which is composed of metasedimentary rocks (Casa Nova Group) intruded by multiple syn- to post-Brasiliano granitic to syenitic rocks (Jardim de Sá et al. 1988, 1996, Santos and Silva Filho 1990, Caxito et al. 2017). The transition between the Middle Devonian and Mississippian Periods is marked by progressive retreat of epicontinental seas (Góes 1995) with minor marine incursions (related to the Longá Formation), resulting in the continental deposits of the Cabeças and Poti Formations (Fig. 12.2-4). The paleocurrent patterns of the fluvial sandstones of the Poti Formation (Góes 1995) and the unimodal deltaic sigmoid of the Cabeças Formation (Barbosa et al. 2015) in the eastern border of the Parnaíba basin indicate that the source areas of these geologic units were situated to the south-southeast of this basin. In this case, the siliciclastic contribution found in the sedimentary piles subsequent to the Pimenteiras Formation came mainly from the central-southern portion of the Borborema province. Metasedimentary rocks of the Borborema province (Fig. 11b) related to different tectonosedimentary environments show considerable peak intervals of 2.25-1.95 Ga, 1.8-1.6 Ga and 1.00.9 Ga, compatible with the main detrital contingents of the post-Pimenteiras formations (2.2-2.0 Ga, 1.9-1.7 Ga and 1.1-0.9 Ga). The younger detrital population (1.1-0.9 Ga) in the metasediments has been frequently related to rocks formed during the Cariris Velhos cycle/event (Neves 2015). However, this age pattern is also reported in the northern portions of both the São Francisco (Una Group; Santos et al. 2012) and Congo (de Wit et al. 2005, 2011) cratons. In addition, the MesoNeoproterozoic Namaqua-Natal Belt, which has been correlated to South American Tonian terranes (Neves 2015), could be another possible candidate to provide these 1.0-0.9 Ga zircon grains for the metasedimentary rocks. Thus, the age pattern mentioned above for the post-Pimenteiras units suggests recycling of the metasedimentary units of the Borborema province. This interpretation is supported by the absence or rare occurrence of 1.5-1.3 Ga zircon grains in both metasedimentary rocks (Neves et al., 2009) and post-Pimenteiras units, which are common in the other possible source areas mentioned. The Stenian zircon populations (1.1-1.0 Ga) are significantly large in these post-Pimenteiras units, and it would be doubtful to relate them only to the narrow terranes of Alto Pajeú and Riacho Gravata (Cariris Velhos event, stricto sensu) in the Central subprovince. The record of Grenvillian age detrital zircons has been overlooked in the Borborema province, despite not being an isolated fact since it has been reported in other areas surrounding the Parnaíba basin by Valeriano et al. (2004), Klein and Moura (2008), Moura et al. (2008) and Caxito et al(2017). Brito Neves et al. (2015) and Caxito et al. (2014a) described large Stenian detrital occurrences in the Riacho do Pontal belt. The major age peaks identified in both the Cabeças (2.0-1.8 Ga, 1.1-1.0 Ga and 650-540 Ma) and Longá (1.9-1.8 Ga, 1.1-1.0 Ga and 650-540 Ma) Formations are consistent with the erosion of rocks from the Riacho do Pontal belt. Other domains of the South subprovince in the Borborema province (Carvalho 2005, Brito et al., 2008, Cruz and Accioly 2013) and syn- to postcollisional and transcurrent magmatic bodies (615-520 Ma) emplaced during the Brasiliano collage (800-500 Ma; Gandade de Araújo et al. 2013, Brito Neves et al. 2014) have also contributed as source areas for both formations, especially the Stenian sources. Contributions from the São Francisco craton may also be considered. The main detrital spectrum of the Poti Formation (2.0-1.8 Ga, 1.0-0.92 Ga and 720-540 Ma) is similar to that of the rocks of the Central subprovince (possibly the Alto Pajeú and Moxotó terranes; Santos et al., 2015) and Brasiliano plutons that are widespread in this region, with minor

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contributions from the Ceará Central and westernMANUSCRIPT Rio Grande do Norte domains (Ganade de Araújo ACCEPTED et al., 2013, Brito Neves et al., 2014).

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Fig. 12. Suggested panorama of main proximal source areas of sedimentary supply in the eastern border of the Parnaíba basin. (A) São Francisco craton; (B) Cratonic covers; (C-E) Borborema province – (C) Northern, (D) Central and (E) Southern subprovinces; (F) Phanerozoic covers; (G) Sea; (H) Tempestite; (I) Delta; (J) Fluvial bars; (K-L) Marine transgression and regression.

6. CONCLUSIONS

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The identification of source areas for detrital zircons in a sedimentary basin is complex. The provenance patterns identified in the Canindé Group suggest a nonstatic paleoenvironment that was repeatedly dislocated due to marine transgression and regression that occurred between the Middle Devonian and Middle Mississippian Periods. These results suggest the following stages:

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(1) The offshore-shoreface environment of the Pimenteiras Formation was a “filter”, capturing sediments from the contact region between the São Francisco craton and the Riacho do Pontal (outer zone) and Sergipano (Central-southern portion, subordinately) marginal belts. Later, the sediments were intensely reworked by coastal currents, dispersed toward the platform and mixed by storm waves (with possible inputs of distal sources from the Amazonian and Western African cratons). (2) Progressive retreat of the epicontinental sea exposed previously submerged regions in the Southern subprovince, mainly in the internal and central zones of the Riacho do Pontal belt and

to a lesser extent in other areas ACCEPTED (Sergipano beltMANUSCRIPT and Pernambuco-Alagoas massif), as well as the extreme northern part of the São Francisco craton. The detrital sediments (predominantly Stenian sediments with ages of 1.2-1.0 Ga) were transported by Cabeças delta toward the sedimentary basin. The contribution of sediments from the northern portions of Borborema province (Ceará Central and western Rio Grande do Norte domains) was on a smaller scale. (3) Marine incursions (Longá Formation) were less pronounced in the South American platform at the end of the Middle Devonian. However, the deposits exhibited distal characteristics, which were also reworked and mixed with allochthonous sources by storm waves. In this case, proximal metasedimentary sources were probably similar to those of the Cabeças Formation. (4) The Mississippian Period is marked by the beginning of continentalization. More distal and central zones of Borborema province (possibly the Alto Moxotó and Alto Pajeú terranes) furnished sediments to fluvial-deltaic systems of the Poti Formation. This process explains the influence of 1.0-0.92 Ga zircons correlated with the Cariris Velhos event and the increasing Statherian zircon population (1.7-1.6 Ga). The contributions of sediments from the Northern and Southern subprovinces should also be considered. However, we suggest a lack of influence from the São Francisco craton on the sedimentation of the Poti Formation.

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The evolution of geologic research in the Parnaíba basin and new geochronological data in Borborema province will allow us to clarify the real contribution of the Stenian-Tonian terranes of this province to the sedimentary succession of the Parnaíba basin. Specific knowledge about provenance patterns of the zircons will help to explain whether the sources, to date directly related to the Cariris Velhos event, may actually represent recycled sediments that were previously stored during the Brasiliano collage. In this case, sediments could also originate from distinct sources, such as the Sunsás belt and/or beyond the South American platform in the African Central block (Irumide, Kilbaran and Namaqua-Natal belts), where extensive Mesoproterozoic orogenic belts occur.

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ACKNOWLEDGMENTS

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We acknowledge the Coordenação de Aperfeiçoamento de Pessoal de Nível Superior (CAPES) for the research scholarship granted to the first author. We also thank the Isotope Geology Laboratory of the Federal University of Pará (Pará-Iso) for the U-Pb analyses. The acknowledgments extend to the Pará-Iso staff and to professor Marco Antonio Galarza Toro for helping with the U-Pb data processing. The authors are grateful to CPRM-Belém for the CL-SEM images of zircons. We are thankful to the reviewers for the suggestions and criticism of the manuscript. This research was supported by Processo CNPq nº 473215/2013-6.

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Nov 01, 2018

Dr. Reinhardt Fuck Regional Editor of the Journal of South American Earth Science Universidade de Brasília, Brasília, Brazil Re: Higlights. Manuscript “PROVENANCE OF DETRITAL ZIRCONS OF THE CANINDÉ GROUP (PARNAÍBA BASIN), NORTHEASTERN BRAZIL”. SAMES_2018_188

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Dear Editor,

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We have forwarded the following highlights: - In eastern edge of the Parnaíba basin the main paleofluxes trend NNW; - The Brasiliano belts of southern Borborema subprovince, may be considered the mainly candidates to provide sediments for the Middle Devonian-Early Carboniferous deposits; - Pimenteiras Formation displays an essentially unimodal pattern, suggesting derivation also from Tocantins province (Brasilia belts) or reworking of the cratonic basins of the São Francisco craton; - Did the Cariris-Velhos event effectively contribute to the extensive StenianTonian zircon age spectra found in the Parnaíba basin? Sincerely.

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Camila Vilar de Oliveira PhD Student Programa de Pós-Graduação em Geologia e Geoquímica – PPGG Instituto de Geociências, Universidade Federal do Pará – UFPA