The paths and timing of late Paleozoic ice revisited: New stratigraphic and paleo-ice flow interpretations from a glacial succession in the upper Itararé Group (Paraná Basin, Brazil)

Accepted Manuscript The paths and timing of late Paleozoic ice revisited: New stratigraphic and paleo-ice flow interpretations from a glacial succession in the upper Itararé Group (Paraná Basin, Brazil)

Thammy Ellin Mottin, Fernando Farias Vesely, Mérolyn Camila Naves de Lima Rodrigues, Felipe Kipper, Paulo Alves de Souza PII: DOI: Reference:

S0031-0182(17)30707-1 doi:10.1016/j.palaeo.2017.11.031 PALAEO 8533

To appear in:

Palaeogeography, Palaeoclimatology, Palaeoecology

Received date: Revised date: Accepted date:

28 June 2017 7 November 2017 12 November 2017

Please cite this article as: Thammy Ellin Mottin, Fernando Farias Vesely, Mérolyn Camila Naves de Lima Rodrigues, Felipe Kipper, Paulo Alves de Souza , The paths and timing of late Paleozoic ice revisited: New stratigraphic and paleo-ice flow interpretations from a glacial succession in the upper Itararé Group (Paraná Basin, Brazil). The address for the corresponding author was captured as affiliation for all authors. Please check if appropriate. Palaeo(2017), doi:10.1016/j.palaeo.2017.11.031

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ACCEPTED MANUSCRIPT The paths and timing of late Paleozoic ice revisited: new stratigraphic and paleo-ice flow interpretations from a glacial succession in the upper Itararé Group (Paraná Basin, Brazil)

Thammy Ellin Mottin1,*, Fernando Farias Vesely1, Mérolyn Camila Naves de

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Lima Rodrigues1, Felipe Kipper2, Paulo Alves de Souza2

1

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Programa de Pós-Graduação em Geologia, Departamento de Geologia,

Universidade Federal do Paraná, Caixa Postal 19001, CEP 81531-980,

2

Programa

de

Pós-Graduação

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Curitiba, PR, Brazil em

Geociências,

Departamento

de

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Paleontologia e Estratigrafia, Instituto de Geociências, Universidade Federal do Rio Grande do Sul, Caixa Postal 15001, CEP 91501-970, Porto Alegre, RS,

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Brazil

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*Corresponding author

Email addresses: [email protected] (T.E. Mottin), [email protected] (F.F. [email protected]

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Vesely),

(M.C.N

de

Lima

Rodrigues),

[email protected] (F. Kipper), [email protected] (P.A. Souza).

ACCEPTED MANUSCRIPT Abstract This paper examines a glacial diamictite-bearing succession from the upper Itararé Group (Taciba Formation) in eastern Paraná Basin, Brazil. The object of study provides the opportunity to investigate in detail the late stages of glacial sedimentation during the Late Paleozoic Ice Age (LPIA) in this sector of SW

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Gondwana, with implications for glacial cyclicity and regional paleo-ice flow

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reconstructions. Sedimentology, geological mapping and palynological analysis

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allowed the recognition of four facies associations, comprising subaqueous outwash, mass-transport, tide-influenced delta-front, and tide-influenced delta

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plain deposits. The succession records at least two episodes of ice-margin advance and retreat into a marine-influenced environment and can be placed in

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the earliest Permian based on the palynomorph assemblage. Cross stratification in outwash facies and deltaic deposits indicate sediment transport

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to the SW, the same revealed by deformational structures in mass-transport

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diamictites derived from downslope resedimentation of glaciomarine sediments during deglaciation. A glacial source to NE is therefore indicated and is in

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agreement with paleo-ice flow directions obtained from previously studied localities to the north. This north-derived early Permian glaciation contrasts with

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glacial sources to the SE recognized in the lower and middle intervals of the Itararé Group. The scenario suggests a geometric reconfiguration of the Paraná Basin during the LPIA and the migration of ice centers with time during the Late Paleozoic Ice Age in SW Gondwana.

Keywords: Gondwana, Late Paleozoic Ice Age, glacial stratigraphy, glacial paleogeography, mass-transport diamictite

ACCEPTED MANUSCRIPT 1. INTRODUCTION The Late Paleozoic Ice Age (LPIA) is considered the longest and most geographically widespread ice age in the Phanerozoic (Eyles, 1993; LópezGamundí and Buatois, 2010). According to recent research, multiple glacial events 1 to 8 My-long alternated with nonglacial periods are recognized in

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Gondwana deposits from the Visean (Mississippian) to the earliest-middle- Late Permian, which were presumably controlled by diachronous ice-spreading

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centers on topographic paleohighs (Isbell et al., 2003; 2012; Fielding et al.,

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2008; Gulbranson et al., 2010; Limarino et al., 2014; Vesely et al., 2015;

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Fallgatter and Paim, 2017). Currently, this view seems to have gained more acceptance than the traditional concept of continental-scale ice sheets

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continuously waxing and waning across Gondwana for up to 100 My (e.g. Veevers and Powell, 1987; Frakes and Francis, 1988; Frakes et al., 1992;

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Scotese et al., 1999).

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The paleoflow directions, size, spatial distribution and geometric configuration of ice masses are major unresolved problems of the LPIA in SW

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Gondwana. The late Paleozoic Itararé Group (Paraná Basin, southern Brazil) contains several glacial landforms and deposits that are useful for paleo-ice flow

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and paleogeographic reconstructions (Almeida, 1948; Bigarella et al., 1967; Rocha-Campos et al., 1988; Caetano-Chang et al., 1990; Tomazelli and Soliani, 1997; Riccomini and Velásquez, 1999; Gesicki et al., 2002; Trosdtorf et al. 2005; Fallgatter and Paim, 2017). The most confident indicators of ice flow are streamlined landforms and striated pavements sculptured on the basement and subglacially plowed surfaces on soft beds that are preserved few meters above the basal boundary of the Itararé Group (e.g. Rosa et al., 2016). These features suggest that multiple ice lobes reached the eastern Paraná Basin flowing to the

ACCEPTED MANUSCRIPT NW and to the N (Fig. 1). One main source of ice would be an ice sheet/cap located in highlands of Namibia, SE Africa (Windhoek highlands; Visser et al., 1987; Santos et al., 1996). An ice center located west of the Paraná Basin (Asunción Arch) is still controversial (Frakes and Crowell, 1969; França and Potter, 1988; Gesicki et al., 2002; Limarino et al., 2014; Aquino et al., 2016;

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Rosa et al., 2016), mainly because of the lack of confident paleo-ice flow

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indicators in the western side of the basin.

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Paleocurrents derived from cross-stratified sandstones from the lower and middle levels of the Itararé Group (Lagoa Azul and Campo Mourão

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formations) show predominant sediment transport towards the NW, N and NE (Fig. 1; Bigarella and Salamuni, 1967; Vesely and Assine, 2006; Vesely et al.,

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2015; Aquino et al., 2016; Carvalho and Vesely, 2017), pointing to a coincidence between paleo-ice flow and clastic input during the Pennsylvanian.

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On the other hand, paleo-ice flow and sediment transport directions in the

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youngest glacial succession (Taciba Formation), are poorly constrained and based on a relatively small amount of kinematic indicators (e.g. Rocha-Campos

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et al., 2000), hampering reliable paleogeographic reconstructions for latest LPIA and the glacial-post glacial transition.

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In this paper we investigate in detail the uppermost late Paleozoic glacial deposits of the Itararé Group (Taciba Formation) and their bounding relationships with the postglacial, coal-bearing Rio Bonito Formation in a sector of eastern Paraná Basin (Fig. 1). By combining sedimentology, sequence stratigraphy, biostratigraphy and paleocurrent analysis, the main goal of this paper is to document the stratigraphic evolution of the final stages of the LPIA in

ACCEPTED MANUSCRIPT this sector of SW Gondwana as well as to discuss implications for paleo-ice flow patterns and glacial to postglacial paleogeography.

2. GEOLOGICAL SETTING The late Bashkirian to lower Sakmarian Itararé Group, object of the

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present study, contains the records of multiple glacial cycles materialized as

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unconformity-bounded sequences (e.g. França and Potter, 1991; Souza, 2006; Vesely and Assine, 2006; Holz et al., 2010). An Early Permian age for the upper

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part of the Itararé Group (Taciba Formation) and the lower part of the

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postglacial Guatá Group (Rio Bonito Formation) has been indicated by distinct fossil groups like palynomorphs (e.g. Souza and Marques-Toigo, 2003; 2005)

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and invertebrates (e.g. Simões et al., 2012; Neves et al., 2014; Taboada et al., 2016) observed in different localities across the eastern outcrop belt. However,

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recent U-Pb dating of volcanic layers in glacial and postglacial strata exclusively

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from the southernmost portion of the basin (Rio Grande do Sul state) place the upper Itararé Group in the Pennsylvanian and constrain the glaciation to the

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Carboniferous in that area (Cagliari et al., 2016; Griffis et al., 2017a). This apparent inconsistency has been the object of continuing research to determine

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if biozones need calibration or if glacial to postglacial transition was truly diachronous in the Paraná Basin. The glacial to postglacial transition in the central-northern sector of the Paraná Basin coincides with a significant change in sediment dispersal patterns. While the main paleocurrent direction in the Itararé Group is towards the north (e.g. França et al., 1996; Vesely and Assine, 2006; Carvalho and Vesely, 2017), the post-glacial Rio Bonito Formation has fluvial and deltaic

ACCEPTED MANUSCRIPT paleocurrents trending SW (Assine et al., 2003; Zacharias, 2004; Zacharias and Assine, 2005). This change has been associated with depocenter migration to the south due to tectonic readjustments (e.g. Milani, 1997). The stratigraphic interval studied herein is well exposed in the Ibaiti region (NE Paraná State), southern Brazil (Fig. 1), and corresponds to the

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Taciba Formation (França and Potter, 1988) and the youngest of the five

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deglaciation sequences defined by Vesely and Assine (2006). In this area, the

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Taciba Formation comprises a thick succession of sandstones at the base, overlain by two distinct diamictite units separated by a rhythmite-sandstone

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interval (Vesely and Assine, 2004; 2006). This succession is capped by postglacial deposits by means of a subaerial unconformity with incised valleys filled

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with fluvial-estuarine facies of the lower Rio Bonito Formation (Zacharias and

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Assine, 2005).

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3. METHODS

This study is based on the investigation of outcrops in an area covering

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300 km² around the Ibaiti region, NE Paraná State (Fig. 1). A number of 110 outcrops were described in road cuts, abandoned quarries and natural

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exposures (supplementary material; Appendix A). Five stratigraphic sections were measured to document vertical facies successions. Biostratigraphic control was obtained using palynomorphs retrieved from two diamictite samples (RE-01 and RE-02) and one muddy rhythmite sample (RE-03) and taking into account the biozonation proposed by Souza and Marques-Toigo (2005) and Souza (2006). Paleocurrent data (726 readings) were taken from trough and planar cross-stratification in sandstones and current ripples in sandy rhythmites. The orientation of mass transport-related deformational structures (bedding, fold

ACCEPTED MANUSCRIPT axes, axial planes, and sandy injectites) were also collected. Kinematic analysis of mass transport deposits was based on the following methods: mean bedding strike (MBSM; Sharman et al., 2015), mean axis (MAM; Woodcock, 1979; Alsop and Marco, 2012; Sharman et al., 2015); mean axial plane strike (MAPS; Alsop and Marco, 2012), axial-planar intersection (AIM; Alsop and Marco, 2012), fold

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facing (Alsop and Marco, 2012), and downslope average axis (DAM;

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Woodcock, 1979).

4. RESULTS Facies associations

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4.1.

In the study area the Taciba Formation can be subdivided into five

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lithostratigraphic units (units 1 to 5 in stratigraphic order) in which eighteen facies and four genetic facies associations were identified. Detailed descriptions

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regarding individual facies, their interpreted formative processes and facies

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associations are presented as supplementary data (Appendix B) and illustrated in figures 3 to 6. In the following subsections we only present a brief explanation

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of the four facies associations with a focus on their correspondent interpreted

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depositional settings.

4.1.1. Subaqueous outwash deposits This facies association is recorded in unit 1 as a 50 m-thick, sandygravelly interval in the lower Taciba Formation. It comprises an alternation of poorly- (dominant) to well-sorted sandstones and conglomerates, ranging from structureless to well stratified, often plastically deformed, and arranged in multiple 2 to 15 m-thick, sharp-based, finning-upward cycles (Figs. 2 and 3). Gravel

within

coarser-grained

facies

(Appendix

B)

displays

similar

ACCEPTED MANUSCRIPT compositional and textural characteristics, ranging from subangular to rounded granules to boulders (up to 30 cm) mainly of granite and quartzite. Clasts are rarely faceted and striated (Fig. 3A) and locally display long-axis imbrication (Fig. 3C). Lonestones where identified mainly at the base of unit 1 and consist of oversized clasts of crystalline rocks within laminated, coarse-grained

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sandstones (Figs. 2 and 3D).

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The complex association of stratified, massive/graded and deformed

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facies (Appendix B) suggests rheologically variable depositional processes, including bedload-dominated currents, concentrated to hyperconcentrated

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density flows and slumps. The intercalation of different facies indicates cyclic changes in flow conditions with time. These characteristics and the

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interfingering with diamictite facies upsection (Fig. 2) are inconsistent with deposition in subaerial, fluvial settings and, conversely, point to a subaquatic

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origin. A subaqueous outwash-fan/apron environment is thus interpreted based

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on the observation of: (i) recurrence and aggradation of coarse-grained deposits and rapid vertical facies changes (e.g. McCabe and Eyles, 1988; Lajeunesse

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and Allard, 2002; Russell and Arnott, 2003); (ii) striated/faceted clasts pointing to a glacial source; (iii) plastically deformed (slumped) beds, consistent with

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instability on the foresets of outwash fans/aprons (Lønne, 1995; Henry et al., 2012; Aquino et al., 2016); (iv) sandy facies that grade laterally into diamictite and mudstone (e.g. Visser et al., 1987; Isbell et al., 2008; Koch and Isbell, 2012); (v) soft-sediment deformation which is commonly described from proximal glaciomarine/glaciolacustrine environments characterized by high sedimentation rates and water-rich, unstable substrates (Powell and Domack, 2002; Henry et al., 2012).

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4.1.2. Mass-transport deposits This facies association occurs in two different stratigraphic positions in the Taciba Formation (units 2 and 5; Fig. 2), forming up to 25 m thick diamictite packages composed of both homogeneous and heterogeneous facies,

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commonly with allochthonous sandstone blocks (F1a to F1d; Appendix B and

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Fig. 4). Diamictites of unit 2 rest conformably on the subaqueous outwash facies association and are sharply overlain by delta-front rhythmites of unit 3.

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Diamictites of unit 5 rest sharply on the delta plain facies association and are

deposits of the Rio Bonito Formation.

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cut on top by the subaerial unconformity that predates the postglacial fluvial

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In general, diamictites have angular to rounded, polymictic clasts immersed in a muddy to muddy-sandy matrix (Appendix B; Fig. 4D). They are

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mainly clast-poor (< 5% clasts; sensu Hambrey & Glasser, 2012) and the

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maximum clast size is 120 cm. Clasts are predominantly composed of granite, quartzite, quartz and sandstone. Faceted, striated (Fig. 4E) and bullet-shaped

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clasts are abundant. Coarse-grained layers and allochthonous blocks (up to 100 m large) are compositionally and texturally similar to facies from the underlying

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units. In the larger blocks (Fig. 4F-G) cross-stratification equivalent to that observed in units 1 and 4 can be easily recognized. The top of unit 5 exhibits a well-developed, up to 10 m-thick paleosol horizon few meters below the base of the postglacial Rio Bonito Formation (Fig. 4H). The presence of unsorted (diamictite) and plastically deformed facies, (e.g. folds, faults, shear planes, sand injectites, deformed blocks) and the occurrence of algal species of marine affinity (see Section 4.2) suggests a

ACCEPTED MANUSCRIPT subaqueous, mass-flow origin for this facies association. Internal structures are consistent with resedimentation due to slumping (Shanmugam, 2006; Posamentier and Martinsen, 2011) where blocks of previously deposited sediment can be incorporated either from slope collapse and basal scouring. Glacially-transported striated/faceted clasts were probably emplaced originally

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as ice-rafted debris and subsequently embraced in the mass flows.

4.1.3. Tide-influenced delta-front deposits

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Unit 3 (Figs. 2 and 5) is composed of a coarsening/thickening upward, 7

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to 20 m thick succession of current-rippled rhythmites (F3) and sandstones with flaser bedding that pass upward into sandstones of unit 4. Asymmetrical ripples

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with foreset dip reversals (Fig. 5A) and submillimeter-thick mud drapes on ripple foresets (Fig. 5C) are quite common. The upper, sandier interval of the

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rhythmite succession exhibits larger composite bedforms consisting of

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downstream accretion, sigmoidal-shaped macroforms with down-current, cross laminated intrasets (Fig. 5D). Scattered granules to pebbles of granite and

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quartzite deforming lamination below (dropstones) occur locally and decrease in abundance upwards (Figs. 2 and 5E).

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This facies association resulted from deposition under hydrodynamic underflows associated with suspension fallout. The occurrence of dropstones points to the presence of floating ice. The coarsening-upward trend (Fig. 2) is interpreted as a result of progradation. In this sense, the rhythmites of unit 3 can be ascribed to a delta front region. A tide-influenced delta front is suggested by: (i) ripples with bidirectional paleocurrents (flow reversal; e.g. Willis et al., 1999; Nichols, 2009); (ii) mud drapes on ripple foresets that indicate slack water

ACCEPTED MANUSCRIPT periods between reversing tidal currents (e.g. Boyd et al., 2006); (iii) presence of heterolithic stratification (e.g. Tänavsuu-Milkeviciene and Plink-Bjorklund, 2009); (iv) occurrence of sigmoidal bedding probably corresponding to tidal bundles (Nio and Yang, 1991; Kreisa and Moiola, 1986). Trace

fossils

of

Helminthoidichnites

tenuis

(Fitch,

1850),

a

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nonspecialized grazing trail (Buatois et al., 2006), occurs locally in sand-rich

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rhythmites (Fig. 5F) and would indicate a shallow freshwater environment

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(Buatois and Mángano, 1993; Buatois et al., 1998; Netto et al., 2009). On the other hand, the presence of Tasmanites sp., Deusilites tenuistriatus,

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Leiosphaeridia sp. and Navifusa variabilis in muddy rhythmites from the lower unit 3 points to a marine influence. The depositional environment can thus be

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interpreted as a marginal marine environment with high input of freshwater,

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corroborating the facies interpretation of a deltaic setting.

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4.1.4. Tide-influenced delta-plain deposits Unit 4 is a 15 to 20 m-thick and laterally extensive sandstone-dominated

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interval conformably overlying delta-front deposits of unit 3. Typical facies include trough and planar cross-stratified, medium to very coarse-grained

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sandstones (Appendix B; Fig. 6) often disposed as channelized and lenticular bodies. Subordinate facies include thin, massive mudstones, sandstones with flaser bedding, plane-parallel laminated sandstones, trough cross-stratified pebbly sandstones and mud-draped rippled sandstones. This facies association, which is a continuation of the underlying deltafront facies in the form of a well-developed coarsening-upward stacking pattern, is interpreted as a delta plain environment occasionally influenced by tidal

ACCEPTED MANUSCRIPT currents. A braided fluvial style is supported by the predominance of coarsegrained facies, several fining-upward cycles and the low mud content, which suggest poorly developed floodplains (Miall, 1977; Coleman and Prior, 1982; Liangqing and Galloway, 1991). Cross-stratified sandstones formed by dune migration under bedload-dominated currents are interpreted as channel-fill

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deposits (e.g. Bridge and Lunt, 2006). Tide influence is suggested by mud

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drapes on ripple foresets and flaser bedding, which is more frequent in the

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lower part of unit 4. In this association tidal reworking is less common and of minor intensity than that described from the underlying delta-front association

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(unit 3). This characteristic would define the whole system as a tide-influenced instead of tide-dominated delta (e.g. Storms et al. 2005; Tänavsuu-Milkeviciene

Palynology

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4.2.

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and Plink-Björklund, 2009).

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Palynological analysis was performed in two samples retrieved from diamictites of unit 2 (samples RE-1 and RE-2) and one sample from muddy

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rhythmite of lower unit 3 (sample RE-3) in the Ribeirão do Engano region (outcrop locality 11; Appendix A). Their stratigraphic position is indicated in the

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composite vertical log of figure 2. The samples revealed rich palynological assemblages in which spores and pollen grains are dominant, followed by few microplankton elements, mainly related to Chlorophyta algae. The complete list of the palynomorphs is presented in table 1. The most abundant taxa are cingulizonate (Vallatisporites and Cristatisporites) and apiculate spores (Horriditriletes), polyplicate pollen grains (Vittatina), appart from taeniate bisaccate

pollen grains

(Protohaploxypinus and Illinites). Monosaccate

ACCEPTED MANUSCRIPT (Cannanaropolis and Plicatipollenites) and non-taeniate bisaccate pollen grains (Limitisporites) are subordinate. Photomicrographs of selected palynomorphs are presented in figure 7. The recognized species are correlated with the basal Protohaploxypinus goraiensis Subzone of the Vittatina costabilis Interval Zone (VcZ), that

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encompasses the uppermost deposits of the Itararé Group and the base of the

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postglacial deposits of the Rio Bonito Formation (Souza and Marques-Toigo,

Cisuralian).

Diagnostic

species

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2005; Souza, 2006). This subzone is attributed to the early Permian (Early identified

in

this

study

include

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Protohaploxypinus limpidus, Illinites unicus and Vittatina subsaccata. The occurrence of the algae Tasmanites sp., Deusilites tenuistriatus, Leiosphaeridia

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sp. and Navifusa variabilis in the units 2 and 3 supports a marine-influenced

Sediment transport patterns

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4.3.

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environment (e.g. Kane, 1968; Revill et al.,1994; Souza, 2006; Telnova, 2012).

4.3.1. Paleocurrent records

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A total of 726 paleocurrent measurements were obtained from the leeside dip azimuth of cross stratification and current ripples in sandstones and

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sandy rhythmites of units 1 (subaqueous outwash), 3 (delta front) and 4 (delta plain). The results are presented in figure 8 as rose diagrams for individual facies associations and a synoptic diagram encompassing all paleocurrent data. The latter shows a main SSW paleocurrent direction (203 mean azimuth). Trough cross-stratified, coarse-grained facies in subaqueous outwash deposits (209 readings) present oblique bimodal paleocurrent pattern to SSE and W, with a mean vector to SSW (Fig. 8). The bimodality is probably a result

ACCEPTED MANUSCRIPT of data acquisition from trough cross strata instead of the presence of two distinct flow directions. The results indicate that meltwater streams emanating from a stable to retreating glacier flowed roughly to the SW, which would suggest an ice margin to the NE during deposition of unit 1. In the delta-front facies association (218 readings), current ripples and

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sigmoidal bedding show an asymmetric bipolar pattern, with mean vectors

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trending SW and NE. According to field observations (Fig. 5A), this bimodality is

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associated with flow reversals, where finer-grained, superimposed ripples migrated in the opposite direction in relation to coarser-grained ripples and

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larger host bedforms. This indicates the coexistence of at least two opposite currents of different intensities (dominant and subordinate) formed by

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alternating onshore- and offshore-directed flows (e.g. Herbert et al., 2005). Paleocurrent records from the delta-plain facies association (299

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readings) exhibit a higher degree of dispersion and variable orientation relative

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to the hierarchy of sedimentary structure (Fig. 8). The flow direction indicated by mid to large scale trough and planar cross stratification is towards SW (230

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mean azimuth) while paleocurrents from current ripples are mainly towards NE (41 mean azimuth). According to field observations and facies interpretation, the

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SW trend corresponds to the direction of dune migration in fluvial distributary channels whereas the NE-directed ripples can be explained by the influence of weak flood tidal currents acting in the lower delta plain. The higher degree of dispersion can be a result of the distributary or avulsive channel networks typical of delta-plain and fan-shaped systems (e.g. North and Warwick, 2007; Cain and Mountney, 2009).

ACCEPTED MANUSCRIPT The dominant NE to SW sediment-transport direction observed in three different facies associations of the Taciba Formation is similar to that indicated by Zacharias (2004) and Zacharias and Assine (2005) in the cross-stratified fluvial sandstones of the lowermost, postglacial Rio Bonito Formation (Fig. 1).

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4.3.2. Mass-transport paleoslope

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Slump-generated deformational structures in stratified, heterogeneous

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diamictites were analyzed in outcrop localities 3 and 109 (Appendix A) to infer paleoslope dip azimuth associated with mass-transport (Figs. 9 and 10). A total

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of 121 measurements from the orientation of bedding, fold axes, axial planes and sandy injectites were collected and stereographically analyzed. The results

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indicate a maximum slump-related stress axis trending NE-SW and, consequently, a paleoslope strike oriented NW-SE (Figs. 9 and 10).

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In both analyzed outcrops, the observed and stereographically calculated

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folds vergence constrains mass flows towards SW, assuming that folds verge in the downslope direction (e.g. Woodcock, 1979). This is parallel to the sediment

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transport direction indicated by paleocurrents from outwash and deltaic deposits and tells that glacially-derived debris (striated clasts within MTD) were sourced

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from the NE and resedimented on a depositional slope dipping to the southwest.

5. DISCUSSION 5.1.

Depositional history and ice-margin fluctuations

Based on the nature of facies associations and fossil content, it can be assumed that the studied succession accumulated in subaerial to relatively deep subaquatic environments. Within this broad depositional setting the

ACCEPTED MANUSCRIPT influence of glaciers was only indirect as supported by: 1) subaqueous masstransport deposits holding faceted/striated clasts, 2) dropstones in different stratigraphic levels and 3) concentrated to hyperconcentrated-flow deposits attributed to subaqueous outwash. Furthermore, the occurrence of the chlorophyta algae Tasmanites sp., Deusilites tenuistriatus and Leiosphaeridia

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sp. and sedimentological indicators of tides show that deposition occurred in a

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marine-influenced environment (e.g. Kane, 1968; Revill et al., 1994; Souza,

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2006; Telnova, 2012). The entire succession was probably deposited in the earliest Permian (Early Cisuralian) because of a palynological assemblage

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correlated to the Protohaploxypinus goraiensis Subzone of the Vittatina costabilis Interval Zone (Souza and Marques-Toigo, 2005; Souza, 2006).

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Through the recognition of the stratigraphic stacking of the four facies associations, it is possible to reconstruct the local depositional history and to

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infer its relationship with ice-margin fluctuations and base-level changes in a

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much higher resolution than previously described (e.g. Vesely and Assine, 2006). Thus, eight evolutionary stages are here recognized, each marked by

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variable depositional trends and different degrees of glacial influence on deposition (Fig. 11).

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Stage I comprises subaqueous outwash deposits of unit 1 that accumulated in front of a grounded tidewater glacier, and records a moment during which the ice margin was relatively close to the depositional site. A stagnant to retreating ice margin is corroborated by the absence of ice-push structures or any apparent ice-contact zone deposit (e.g. Kneller et al., 2004). This phase is dominated by conglomerates and poorly sorted sandstones derived from meltwater jets (e.g. Powell and Cooper, 2002). Massive diamictites

ACCEPTED MANUSCRIPT and mudstones were formed via rapid settling from buoyant meltwater plumes along with the introduction of ice-rafted debris (Powell, 1990; Henry et al., 2012; Koch and Isbell, 2012; Fig. 11). Subaqueous outwash or grounding-line fan deposits have been reported from several late Paleozoic gondwanic successions in both unconfined and

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confined (valley) glacial settings (e.g. Visser et al., 1987; von Brunn, 1996;

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Kneller et al., 2004; Vesely and Assine, 2006; Henry et al., 2012; Koch and

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Isbell, 2012; Aquino et al., 2016). In such ice-proximal glaciomarine environments, isostatic subsidence promoted by ice loading was probably of

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primary importance in increasing accommodation in the ice marginal zone (e.g. Boulton, 1990; Brookfield and Martini, 1999) in order to build a thick succession

MA

of outwash deposits.

With ice retreat, isostatic rebound can outpace deglacial eustatic rise

D

causing a rapid relative sea-level fall as modelled by Boulton (1990) and Powell

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and Cooper (2002) and inferred from several study cases (e.g. Nemec et al., 1999; Massari et al., 1999; El-ghali, 2005; Cummings et al., 2011; Nutz et al.,

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2015; Dietrich et al., 2017). These predicted isostatically-driven tectonic forces and associated base-level fall may have led the previously accumulated

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outwash and rainout deposits to become unstable, causing remobilization via slumps and debris flows and forming, during stage II, mass-transport diamictites with allochthonous blocks of sandstones (Fig. 11). Studies on Quaternary mass-transport deposits have also recognized the connection between retreating ice margins and mass failure (e.g. Laberg et al., 2006; Twichell et al., 2009). The isostatic readjustment of landmasses due to the ice melting can induce earthquakes of different intensities. These

ACCEPTED MANUSCRIPT movements, in turn, can start mass movements from sediment previously destabilized by other mechanisms such as excess pore pressure, gas hydrate dissociation and others. Sea-level fall has also been regarded as an important trigger mechanism for mass failure in continental margins and delta-front slopes once it causes a drop in wave base leading to shelf-margin instabilization (e.g.

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Rothwell et al., 1998; Catuneanu, 2006; Berton and Vesely, 2016; Guan et al.

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2016).

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A relatively thin level of dropstone-bearing shale sharply overlies the mass-transport diamictites of unit 2. It is interpreted as a maximum flooding

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zone (stage III) reflecting an increase in water depth that happened probably because positive glacio-eustacy overcame the rapid effect of glacio-isostatic,

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rebound causing relative sea-level rise (e.g. Boulton, 1990; Dietrich et al., 2017). In stage IV, following the maximum transgression, sediment supply

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outpaced relative sea-level rise causing highstand deltaic progradation towards

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the SW. A normal instead of forced regression is suggested by the conformable stacking pattern from delta-front to delta-plain deposits (e.g. Catuneanu, 2006).

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From the maximum flooding (stage III) to the climax of delta progradation (late stage IV) a progressive diminishing in the amount of dropstones is observed,

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suggesting that highstand progradation proceeded during late deglacial to postglacial conditions. The fact a delta plain has been developed indicates an ice-free shoreline that probably prevented the entrainment of ice-rafted debris in the basin. The subaerial deltaic deposits formed during late stage IV are sharply succeeded by a new unit of subaqueous mass-transport diamictite (unit 5). The emplacement of this diamictite requires a considerable increase in water depth

ACCEPTED MANUSCRIPT in order to submerge the delta and create space to accommodate a masstransport deposit up to 25 m thick. Considering that the underlying delta was deposited during a glacial minimum and that the mass-transport diamictites above hold abundant glacially-derived faceted/striated clasts, it seems likely that the required water-depth increase was in some extent genetically related to

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a new phase of glaciation (stage V). The advance of a glacier can promote

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glacio-isostatic subsidence in the proglacial zone several tens of kilometers

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beyond the ice margin (e.g. Boulton, 1990; Brookfield and Martini, 1999; Bennett and Glasser, 2009). Crustal depressions up to 100 m and as fast as 7

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m/Ka have been estimated for areas formerly affected by the Laurentide Ice Sheet in the Quaternary (e.g. Rémillard et al., 2017).

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Direct evidence (subglacial deposition, erosion or deformation) of a new glacier advance during stage V is not preserved in the study area, but

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glaciotectonic deformations described by Rocha-Campos et al. (2000) few

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meters below the Rio Bonito Formation 350 km northeastward (Cerquilho locality) can be associated with this event. According to the kinematic analysis

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of folds and shear planes performed by Rocha-Campos et al. (2000), paleo-ice flow was towards the SW, matching our paleocurrent database. Considering the

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lack of subglacial and ice-marginal features in the study area in this stratigraphic position, it can be interpreted that the ice margin did not reach Ibaiti during stage V. Instead, this area probably experienced very low glaciomarine sedimentation rates during this stage, consisting of fine-grained sediment and ice-rafted debris that were subsequently remobilized by mass flows.

ACCEPTED MANUSCRIPT The emplacement of thick mass-flow diamictites of unit 5 can be ascribed to similar controlling factors than those interpreted for unit 2. A new phase of ice-margin retreat thus led to a new phase of isostatic rebound and base-level fall (stage VI), causing slope instability and resedimentation of previously accumulated glaciomarine sediments. The presence of rhythmite and

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sandstone blocks derived from units 3 and 4 and incorporated in the mass-

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transport diamictites suggests strong basal scouring/plucking and assimilation

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of these facies in the diamictite matrix during flow runnout (e.g. Moscardelli et al., 2005; Lamarche et al., 2008; Suss et al., 2014; Buso et al., 2015).

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A transgressive episode subsequent to stage VI is not recorded in the study area and this is a marked difference compared to the deglaciation pattern

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of underlying units (see stages I to III; Fig. 11). In contrast, the next recorded evolutionary stage (stage VII) comprises an important base-level fall that led to

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paleosol (root traces and peds) development on top of unit 5. Root traces are

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evidence that the diamictite was subaerially exposed and colonized by plants (Retallack, 1988). It also indicates climatic amelioration favoring the

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development of vegetated land. The subaerial unconformity with incised valleys that delineate the contact between the Taciba and Rio Bonito formations can be

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also attributed to this stage as proposed by Zacharias and Assine (2005). As the gap involved in the Taciba-Rio Bonito unconformity is unknown, a considerable thickness of strata could have been removed from the upper Taciba Formation due to subaerial erosion, making it impossible to accurately reconstruct the geological history at the glacial-postglacial transition. The relative sea-level fall that produced the subaerial unconformity underlying the Rio Bonito Formation has been attributed to tectonic uplifting in

ACCEPTED MANUSCRIPT the northern sector of the Paraná Basin (Milani, 1997; Milani and Ramos, 1998; Zacharias and Assine, 2005). A subsequent sea-level rise (stage VIII) allowed the infilling of the incised valleys by the coal-bearing fluvial and tidal-plain facies associations that correspond to the basal portion of the Rio Bonito Formation

Implications for paleo-ice flow directions

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5.2.

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(Zacharias and Assine, 2005).

With very few exceptions, confident information relative to paleo-ice flow

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directions in the Paraná Basin is restricted to subglacial landforms on the

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preglacial substrate and soft-sediment grooving within Pennsylvanian strata (see Gesicki et al., 2002 and Rosa et al., 2016 for recent reviews and Fallgatter

MA

and Paim, 2017 for new findings). These data show consistent trends to the N and to the NW throughout the eastern and southern borders of the basin,

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pointing to Carboniferous ice sources located to the southeast and to the south

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(Fig. 1).

Results from the present study, however, show an important change in

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sediment dispersion patterns in the upper Itararé Group, which would indicate a distinct paleo-ice flow direction at the end of the LPIA in the Paraná Basin. The

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outwash systems at the base of the Taciba Formation were built in the opposite direction of ice retreat. Cross stratification in outwash facies indicates that meltwater streams flowed from NE to SW, suggesting thus an ice margin located to the north instead of to the SE as indicated by paleoflow records from underlying stratigraphic intervals. Deltaic deposits also show predominant fluvial paleocurrents towards the SW, implying in a catchment area located to the NE. Moreover, the paleocurrents presented here have the same direction than those

ACCEPTED MANUSCRIPT obtained from postglacial fluvial facies of the lowermost Rio Bonito Formation (Zacharias and Assine, 2005). In addition to paleocurrents, slump-related penecontemporaneous deformational structures in diamictites genetically related to the outwash and deltaic deposits indicate paleo-mass transport to the SW, pointing to a

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paleoslope dipping in that direction during the deposition of the Taciba

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Formation. Mass-transport deposits of units 2 and 5 exhibit faceted and striated

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clasts that suggest a glaciogenic protolith located to the NE prior to resedimentation. Therefore, the group of evidence strongly suggests an ice

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source to the NE and paleo-ice flow to the SW (Fig. 12). Some pieces of information from previous work give additional support to

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the idea of an ice source located somewhere to the north. In the Cerquilho region, 350 km northeast from the study area, Santos et al. (1996) and Rocha-

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Campos et al. (2000) reported soft-sediment deformation (recumbent and drag

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folds, shear surfaces, faults and shear lamination) below subglacial tillites and interpreted them as glaciotectonic in origin. The deformational structures show

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a predominant vergence to SSW and, according to the authors, are related to the advance of glacier on soft sediments. The stratigraphic level from which the

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glaciotectonic structures were described corresponds to the upper part of the Itararé Group, less than 20 m beneath its contact with the postglacial Tatuí (Rio Bonito) Formation. The palynological assemblage described by Souza (2000) in the Cerquilho locality is attributed to the Early Permian, mainly because of the occurrence of Vittatina sp. On the basis of its stratigraphic position and kinematics, the Cerquilho structures are considered here as part of the same glacial episode that gave rise to the upper diamictite unit described in the

ACCEPTED MANUSCRIPT present paper (stages V and VI; Fig. 11). Considering the inferredpaleo-ice flow direction, the study area would thus be placed in a more distal setting in relation to the Cerquilho locality. The

San

Franciscana

Basin,

located

in

central-eastern

Brazil,

approximately 400 km NE from the northern edge of the Paraná Basin, contains

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late Paleozoic glacial facies belonging to the Santa Fé Group (Campos and

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Dardenne, 1994). In this unit, diamictites with faceted clasts and dropstone-

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bearing rhythmites are found covering glacially striated pavements on Neoproterozoic rocks of the Três Marias Formation (Bambuí Group). The

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precise age of the Santa Fé glacial facies is unknown, but the typical trace-fossil assemblage allows placing it in the Upper Paleozoic (Campos and Dardenne,

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1994). In one of the glacial pavements, crescentic fractures were reported (Campos and Dardenne, 2002) and revealed a SSW paleo-ice flow towards the

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Paraná Basin, which would require an ice source located even farther to the

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north.

Late Paleozoic glacial deposits and landforms have been also

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documented in the Sergipe-Alagoas basin and the Santa Brígida graben (Curituba and Batinga formations), NE Brazil (Viviani et al., 2000; Anderson and

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Cotter, 2005). In these units, reported glacial features include striations on Precambrian basement, diamictite with striated/faceted clasts, rhythmites with dropstones and intraformational grooves interpreted as iceberg keel marks (Viviani et al., 2000). Although no confident paleo-ice flow kinematic indicators have been published, the deposits and associated landforms are indisputable evidence for mid-latitude late Paleozoic glaciation in NE Brazil.

ACCEPTED MANUSCRIPT A northern source for diamictites of the Taciba Formation is also corroborated by basin-scale lithofacies distribution as described by França and Potter (1988) and Eyles et al. (1993) based on exploration wells. In the subsurface the diamictite-bearing, upper interval of the Taciba Formation (Chapéu do Sol Member; França and Potter, 1988) is a blanked-like unit up to

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200 m thick that extends horizontally for more than 700.000 km 2 in the central-

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northern sector of the basin (Eyles et al., 1993). To the south (Santa Catarina

SC

state) this unit passes laterally into a shale/rhythmite-dominated succession with scattered ice-rafted debris (Rio do Sul Member; França and Potter, 1988).

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This horizontal facies change would be suggestive of a depocenter in the south and a north to south downdip transition from ice-proximal to ice-distal

MA

glaciomarine environments (e.g. Eyles et al., 1985; Boulton, 1990). The scenario described above seems to be consistent with recent results

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of U-Pb dating of detrital zircon presented by Griffis et al. (2017b) based on

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samples collected from diamictites in the lower (Lagoa Azul Fm.) and upper (Taciba Fm.) levels of the Itararé Group. These authors demonstrated a change

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from more proximal to more distal sources towards the top of the succession, a similar pattern detected in other time-equivalent South American and African

AC

late Paleozoic units.

On what extent the SE-derived Pennsylvanian ice lobes were still active during deposition of the uppermost Itararé Group (e.g. Eyles et al., 1993; Santos et al., 1996) is still an open matter for debate as is the external controls on glaciation. At least in the study area sedimentological evidence favoring ice and sediment sourced from the SE was not identified. Thus, the overall paleogeographic setting indicated by our results plus previously published

ACCEPTED MANUSCRIPT information discussed herein suggests relocation of ice-spreading centers with time during the LPIA in the western sector of Gondwana.

6. Conclusions The analysis of glacial deposits from the uppermost interval of the Itararé

PT

Group (Paraná Basin) provides a number of relevant conclusions concerning



RI

the final stages of the LPIA in this region of SW Gondwana:

The stratigraphic stacking of the upper Itararé Group (Taciba Formation)

SC

in the study area records at least two phases of ice-margin advance

Although some aspects of diamictites point to a glacial affinity (e.g. bullet-shaped

and

striated

clasts),

MA



NU

separated by an interglacial deltaic phase.

no

evidence

for

subglacial

deposition/deformation could be found in the study area. The diamictites

D

consist mainly of mass-transport facies resulted from the resedimentation



PT E

of glacially-derived debris and previously accumulated sediments. The depositional history interpreted for the studied succession highlights

CE

the importance of glacioisostatic forces in creating accommodation in the proglacial zone and as trigger for slope instability and the emplacement



AC

of mass-transport deposits. Paleocurrent indicators and kinematics of slump-related deformational structures indicate a general paleoflow to the SW, which is similar to the postglacial fluvial facies of the Rio Bonito Formation but markedly different from the lower levels of the Itararé Group.

ACCEPTED MANUSCRIPT 

The group of evidence indicates a glacial source to the north during the deposition of the Taciba Formation, which is supported by results from previous research in and outside the Paraná Basin. An important paleogeographic change happened in the Paraná Basin still during the glacial phase and not only in postglacial times as previously

CE

PT E

D

MA

NU

SC

RI

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suggested.

AC



ACCEPTED MANUSCRIPT Acknowledgments This contribution is part of MSc research performed by the first author in the Postgraduate Program in Geology at UFPR. The authors thank CNPq for financial support to F. F. Vesely and P. A. Souza (grants 461650/2014-2 and 461628/2014-7) and CAPES for providing scholarships to T. E. Mottin and M. C.

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N. L. Rodrigues. We thank the three anonymous reviewers and editor Isabel

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Montañez for comments and suggestions that improved the quality of the

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CE

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MA

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SC

manuscript.

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do Paraná. Revista Brasileira de Geociências 35(4), 573-583.

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Table 1 - List of palynomorphs identified in the Taciba Formation in the Ibaiti region.

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FIGURE CAPTIONS

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Fig. 1 - Geological setting: (A) Location of the study area in the eastern border of the Paraná Basin. Blue arrows indicate reliable paleo-ice flow directions

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obtained from subglacial landforms (Rosa et al., 2016). Abbreviation for Brazilian states: MT, Mato Grosso; GO, Goiás; MS, Mato Grosso do Sul; MG,

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Minas Gerais; SP, São Paulo; PR, Paraná; SC, Santa Catarina; RS, Rio Grande do Sul. (B) Stratigraphic position of the study interval with respect to the

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deglaciation sequences described by Vesely and Assine (2006) in northern

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Paraná state.

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Fig. 2 - Composite vertical log (A) and measured stratigraphic columns of the

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five units recognized in the Taciba Formation (B).

Fig. 3 - Facies characteristics of the subaqueous outwash facies association. (A) Striated subangular quartzite clast from pebbly sadnstone. (B) Matrixsupported, faintly stratified conglomerate (F16). (C) Gravelly sandstone with moderate long-axis clast imbrication (F13). (D) Detail of a granite dropstone within F18 (note downwarped lamination). (E) Flat mudstone clasts in through cross-stratified sandstone of F10. (F) Normally-graded sandstone with granules

ACCEPTED MANUSCRIPT and pebbles at the base (F9). (G) Load structure and deformed stratification (F6); (H) Metric-scale slump folds in pebbly sandstone (F7).

Fig. 4 - Facies characteristics of mass-transport deposits facies association. (A) Sheared diamictite displaying sub-horizontal shear planes (F1b) indicated by

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arrows. (B-C) Compositional bands and sandy injectites (sills and dykes) in

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heterogeneous diamictite (F1c). (D) Massive diamictite (F1a) with polymictic

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clasts ranging from pebbles to cobbles. (E) Example of a well striated clast found in diamictite of F1d. (F-G) Diamictites with allochthonous, m-scale

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sandstone blocks (F1d). (H) Purple colored paleosol horizon developed on top

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of the upper diamictite (unit 5).

Fig. 5 - Facies characteristics of the tide-influenced delta front facies

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association. (A) Sand-rich rhythmite (F3) showing current ripples and

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dropstones. Note two opposite paleocurrent directions. (B) Planar lamination within sandy layers in rhythmites (F3). (C) Rippled- rhythmite with mud drapes

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(F3). (D) Sigmoidal composite macroform. (E) Flaser-bedded sandstone with a

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granite dropstone (F4). (F) Bedding plane with Helminthoidichnites tenuis.

Fig. 6 - Facies characteristics of the tide-influenced delta plain facies association.

(A)

Medium-

and

(B)

small-scale

trough

cross-stratified

sandstones. (C) Medium-scale planar cross-stratification in medium-grained sandstone (F11). (D) Plane-parallel stratification in medium-grained sandstone (F12). (E) Trough cross-stratified, pebbly sandstone. Note rip-up mudstone

ACCEPTED MANUSCRIPT clasts indicated by arrows. (F) Trough-like sandstone body with a basal lag of mudstone clasts.

Fig. 7 - Photomicrographs of selected palynomorphs from the Taciba Formation in the Ibaiti region. 1) Punctatisporites gretensis (slide MP-P 12607, coordinate

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England Finder I50); 2) Calamospora hartugiana (12607, R43); 3) Horriditriletes

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uruguaiensis (12606, P48); 4) Vallatisporites ciliaris (12609, H38); 5)

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Vallatisporites vallatus (12607, W43); 6) Cristatisporites sp. cf. C. inconstans (12606, O43); 7) Laevigatosporites vulgaris (12609, N40); 8) Plicatipollenites

(12605,

T51);

11)

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densus (12604); 9) Cananoropollis sp. (12607, I47); 10) Meristocorpus sp. Protohaploxypinus

bharadwajii

(12607,

N47);

12)

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Protohaploxypinus limpidus (12607, K36); 13) Ilinites unicus (12605, T46); 14) Ilinites unicus (12607, V57); 15) Mabuitasaccites crucistriatus (12607, K51); 16)

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Vittatina subsaccata (12604, D43); 17) Vittatina subsaccata (12605, M51); 18)

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Vittatina subsaccata (12604, G54); 19) Striomonosaccites sp. (12605, F31); 20) Tasmanites sp. (12609, L48); 21) Navifusa variabilis (12608, P53); 22)

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Deusilites tenuistriatus (12604, F58); 23) Botryococcus braunii (12608, P48).

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Scale = 20 μm.

Fig. 8 - Rose diagrams representing paleocurrent data collected from different facies associations in the Taciba Formation. Unit 1, outwash deposits; unit 3, delta front; unit 4, delta plain.

ACCEPTED MANUSCRIPT Fig. 9 - Photomosaic and interpreted sketch of mass-transport diamictite showing metric-scale slump folds verging to the SW. Stereograms display slump fold orientations according to the different applied methods.

Fig. 10 - Structural data from mass-transport diamictite of unit 2. (A) Metric

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slump folds verging to the SW. (B) Cm-scale slump folds marked by the sand-

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rich layers of F1c. Stereograms of slump-fold orientations according to the

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different applied methods.

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Fig. 11 - Interpreted paleodepositional settings for the eight recognized

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evolutionary stages.

Fig. 12 - Representation of a north-derived glaciation during the Early Permian

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dispersal patterns.

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in the Paraná Basin based on available paleo-ice flow indicators and sediment

ACCEPTED MANUSCRIPT Table 1 Spores Calamospora hartugiana Wilson and Bentall 1944 Calamospora liquida Kosanke 1950 Calamospora spp. Cristatisporites crassilabratus Archangelsky and Gamerro 1979 Cristatisporites sp. cf . C.inconstans Archangelsky and Gamerro 1979

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Cristatisporites spp. Densosporites sp. Dibolisporites sp.

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Horriditriletes uruguaiensis (Marques-Toigo) Archangelsky & Gamerro 1979

Laevigatosporites vulgaris Ibrahim 1933 Punctatisporites gretensis Balme and Hennelly 1956

Spelaeotriletes sp.

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Punctatisporites spp.

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Horriditriletes spp.

Vallatisporites arcuatus (Marques-Toigo) Archangelsky and Gamerro 1979

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Vallatisporites ciliaris (Luber) Sullivan 1964 Vallatisporites vallatus Hacquebard 1957 Vallatisporites sp.

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Verrucosisporites sp. Pollen grains

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Colpisaccites sp. Cannanoropollis sp. Cycadopites sp. Illinites unicus Kosanke emend. Jansonius and Hills 1976 Limitisporites sp. Mabuitasaccites crucistriatus (Ybert) Playford and Dino 2000 Meristocorpus sp. Plicatipollenites densus (Lele) Bose and Maheshwari 1968 Plicatipollenites malabarensis (Potonié and Sah) Foster 1975 Plicatipollenites spp. Protohaploxypinus limpidus (Balme & Hennelly) Balme and Playford 1967 Protohaploxypinus bharadwajii Foster 1979 Protohaploxypinus spp. Striomonosaccites sp. Vittatina subsaccata Samoilovich 1953 Vittatina spp. Algae (Chlorophyta) Botryococcus braunii Kützing 1849 Deusillites tenuistriatus Gutiérrez, Césari and Archangelsky 1997 Leiosphaeridia sp. Navifusa variabilis Gutiérrez and Limarino Tasmanites sp.

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ACCEPTED MANUSCRIPT Highlights Two glacial episodes recorded in the upper part of the Itararé Group are documented Diamictite units comprise subaqueous, glacially-influenced mass-transport deposits Two events of ice-margin advance are separated by an event of delta progradation

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Mass failure was probably caused by glacioisostatic rebound during early deglaciation

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Paleotransport direction to SW points to an ice source located NE of the study area