Transpressional deformation during Ediacaran accretion of the Paranaguá Terrane, southernmost Ribeira Belt, Western Gondwana

Journal Pre-proof Transpressional deformation during Ediacaran Accretion of the Paranaguá terrane, southernmost Ribeira belt, western Gondwana D. Patias, L.F. Cury, O. Siga, Jr. PII:

S0895-9811(19)30122-1

DOI:

https://doi.org/10.1016/j.jsames.2019.102374

Reference:

SAMES 102374

To appear in:

Journal of South American Earth Sciences

Received Date: 15 April 2019 Revised Date:

1 October 2019

Accepted Date: 1 October 2019

Please cite this article as: Patias, D., Cury, L.F., Siga Jr., , O., Transpressional deformation during Ediacaran Accretion of the Paranaguá terrane, southernmost Ribeira belt, western Gondwana, Journal of South American Earth Sciences (2019), doi: https://doi.org/10.1016/j.jsames.2019.102374. This is a PDF file of an article that has undergone enhancements after acceptance, such as the addition of a cover page and metadata, and formatting for readability, but it is not yet the definitive version of record. This version will undergo additional copyediting, typesetting and review before it is published in its final form, but we are providing this version to give early visibility of the article. 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. © 2019 Published by Elsevier Ltd.

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1

TRANSPRESSIONAL DEFORMATION DURING EDIACARAN ACCRETION

2

OF THE PARANAGUÁ TERRANE, SOUTHERNMOST RIBEIRA BELT,

3

WESTERN GONDWANA

4 5

Abstract

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The Paranaguá Terrane is mainly constituted by an Ediacaran arc-related

7

granitic complex, spread in a NE-SW trending elongated stripe, located in the

8

Southern Ribeira Belt, South-Southeastern Brazil. The basement of these

9

granites occurs as a disrupted folded belt composed of metasedimentary and

10

gneissic-migmatitic rocks. The integration of structural and geophysical (gamma

11

spectrometry and magnetometry) data from the Paranaguá Terrane and the

12

adjacent tectonic units, suggests that the deformation in the study area is

13

partially controlled by the geometry of the Luis Alves Cratonic Block, as well as

14

the northern part of Dom Feliciano Belt. The irregular shape of this cratonic unit

15

associated with N-NW tectonic transport direction caused strain partitioning in

16

the area and the development of two structural domains: southern and northern

17

Paranaguá. The southern part is characterized by sinistral transpressional

18

shear zones, while the northern sector is dominated by thrust shear zones that

19

represent a large frontal collision with oblique components. The hierarchy of the

20

structural and microstructural features in the Paranaguá Terrane associated

21

with geochronologic data suggest two deformational phases (D1 and D2) during

22

a transpressive collisional system. The D1 progressive deformational stage is

23

correlated to the main period of granitic crystallization during the Ediacaran and

24

was divided in two moments: i) early D1 (640 – 610) associated with the

25

regional metamorphism and thrust and folding tectonics with N-NW tectonic

2

26

transport and; ii) late D1 (610-580 Ma) linked to the strain partitioning and

27

development of the southern (simple-shear dominated) and northern (pure-

28

shear dominated) structural domains with sinistral kinematics, granite

29

emplacement and high-temperature mylonites. The D2 deformation stage (540

30

– 500 Ma) is mainly represented by the low-temperature mylonites and

31

deformation under retrograde conditions.

32 33

Key Words: Brasiliano – Pan-African orogeny, Paranaguá Terrane, oblique collision,

34

aerogeophysics, structural analysis, strain partitioning.

35 36

1. Introduction

37

The tectonic evolution of the Western Gondwana continent involved a

38

series of collisional orogens that culminated in the amalgamation of several

39

Precambrian terranes from the late Neoproterozoic until the early Paleozoic

40

(Brito Neves et al., 1999; Campos Neto, 2000; Schmitt et al., 2004; Basei et al.,

41

2008; Heilbron et al., 2008; Faleiros et al., 2011; Brito Neves et al., 2014;

42

Konopásek et al., 2016).

43

The reconstruction of continental margins related to Brasiliano – Pan-

44

African tectonic events depends on how much information we can get from

45

Neoproterozoic granites and metamorphic belts (Trouw et al., 2000; Passchier

46

et al., 2002; Goscombe et al., 2003; Goscombe and Gray, 2007; Heilbron et al.,

47

2008; Siga Jr et al., 2009; Basei et al., 2011). Consequently, the interaction

48

between major tectonic units as cratons, microplates, mobile belts and their

49

respective geometry, plays an important role in the deformational history of

3

50

these orogenic systems (Tikoff and Teyssier, 1994; Teyssier et al., 1995;

51

Fossen et al., 2018).

52

In the southwestern part of Gondwana, the coastal Paranaguá Terrane

53

(study area – Fig. 1), an accretionary to collisional system, was juxtaposed onto

54

the Luis Alves craton and Curitiba Terrane to the Ribeira Belt, during the

55

Ediacaran (Fig. 1). This orogenic cycle (Brasiliano – Pan-African) created

56

distinct structural patterns that provided important clues to understand the

57

deformational history of the Paranaguá Terrane, as well as the interaction

58

between different tectonic units.

59

This study presents the deformational aspects and structural domains of

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the Paranaguá Terrane and its spatial arrangement, allowing the evaluation of

61

the regional expression and the tectonic significance of the geological features

62

observed in outcrops and in micro- and meso-scale. We propose a new model

63

for the deformation history based on field observations and high resolution

64

aerogeophysical data integrated with previous geologic and geochronologic

65

data. This model highlights that boundaries conditions play an important role in

66

the structural pattern of the Paranaguá Terrane and control strain partitioning.

67 68

2. Geological setting

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The study area is located in the southern portion of Ribeira Belt, which is

70

a mobile belt product of the interaction between cratonic blocks (São Francisco,

71

Paranapanema, Luis Alves and Congo) and consumption of the Adamastor

72

Ocean (Silva et al., 2005; Heilbron et al., 2008). The southern Ribeira Belt is

73

formed by Precambrian terranes amalgamated during the Ediacaran and often

74

bounded by thrust or transcurrent shear zones (Basei et al., 1992; Silva et al.,

4

75

2005; Faleiros et al., 2011). The southernmost portion of this belt consists of the

76

Apiaí, Curitiba and Paranaguá Terranes and stands out by the presence of the

77

Luis Alves Cratonic Block separating the Ribeira and the Dom Feliciano Belts

78

(Fig. 1).

79

The Curitiba Terrane (Fig. 1) is bounded by shear zones in the north

80

(Lancinha-Cubatão Shear Zone) and in the south (Piên-Mandirituba and

81

Icapara shear zones) that separate it from the Luis Alves and Paranaguá units,

82

respectively. This block is mainly formed by Paleoproterozoic basement

83

orthogneisses of the Atuba Complex migmatized during the Ediacaran (Siga Jr.

84

et al., 1995; Sato et al., 2003, 2009); Mesoproterozoic (Stenian) and

85

Neoproterozoic (Ediacaran) supracrustal units, represented by the Capiru and

86

Turvo-Cajati Formations, respectively (Siga Jr. et al., 2012; Campanha et al.,

87

2016; Leandro, 2016), and Ediacaran granitic intrusions (Campanha and

88

Sadowski, 1999).

89

The Luis Alves unit (Fig. 1) is considered a cratonic block, mainly formed

90

by Archean to Paleoproterozoic orthogneisses, migmatites and granites with

91

TTG affinities (Hartmann et al., 2000; Basei et al., 2009). This cratonic fragment

92

played an important role in the evolution and deformation of the Southern

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Ribeira Belt during the Ediacaran, such as: i) being the continental block for the

94

emplacement of Rio Piên magmatic arc (Harara, 2001) and part of the A-type

95

anorogenic granites from Serra do Mar Suite (Vlach et al., 2011; Vilalva et al.,

96

2019); ii) represents the basement of extensional Ediacaran basins (Basei et

97

al., 1998; Quiroz-Valle et al., 2019) and; iii) controls the regional strain

98

partitioning (this work – section 5.1).

5

99

The Paranaguá Terrane, the focus of this study, extends in NE-SW

100

direction, consistent with the Ribeira Belt regional trend, occupying 240 km of

101

length and 30 km of width (Fig. 1) in the south-southern Brazilian coast (Siga Jr,

102

1995; Cury, 2009). It is limited by sinistral strike-slip shear zones in the south

103

that separate the Paranaguá Terrane from the Luis Alves Microplate. To the

104

north, it is in contact with the Curitiba Terrane by thrust shear zones (Siga Jr,

105

1995; Cury, 2009). The Paranaguá Terrane is mainly formed by Ediacaran

106

granitic suites that intruded basement inliers of Paleoproterozoic migmatic

107

orthogneiss and Mesoproterozoic metasedimentary rocks (Cury, 2009).

108

These basement rocks are represented by two main units: i)

109

orthogneisses with dioritic, granodioritic, quartz-monzodioritic, trondhjemitic and

110

monzogranitic composition (locally migmatized) from the São Francisco do Sul

111

Complex with Rhyacian igneous crystallization (ca. 2.1 Ga) and Ediacaran

112

metamorphic rims for metamorphism and deformation (ca. 620 Ma) (Cury,

113

2009) and; ii) metasedimentary rocks from the Rio das Cobras Succession

114

formed by schists, quartzites, calc-silicate marbles and amphibolites. These

115

rocks present green schist facies regional metamorphism and later were

116

influenced by a high grade contact metamorphism near the Ediacaran granite

117

batholiths that formed migmatitic paragneisses (Guimaraes, 2019). The

118

provenance study shows mainly Mesoproterozoic (Ectasian) maximum

119

depositional age and Ediacaran ages for U-Pb zircon rims and monazite (ca

120

610 – 595 Ma)(Cury, 2009). The occurrence of these basement slices is mainly

121

limited by shear zones and granitic intrusions (Siga Jr., 1995; Cury, 2009).

122

The granitic suites were divided into three main units based on their

123

petrographic and geochemical characteristics (Cury, 2009): i) The Morro Inglês

6

124

Suite (617 – 581 Ma) is the most expressive unit in the Paranaguá Terrane,

125

being mainly constituted by sienogranites and monzogranites with medium to

126

coarse porphyritic texture, frequently foliated, and with geochemistry signatures

127

compatible with magmatic arc-related granitic rocks, with high-K to shoshonitic

128

calc-alkaline signatures (Siga Jr, 1995; Cury, 2009); ii) the Canavieiras-Estrela

129

Suite (638 – 577 Ma) crops out in the western section along shear zones,

130

nearby the contact between the Paranaguá Terrane and Luis Alves Cratonic

131

block (Fig. 2), and is constituted by foliated granitoids with calc-alkaline and

132

high

133

sienogranitic composition (Siga Jr, 1995; Cury, 2009); iii) the Rio do Poço Suite

134

(615 – 598 Ma) appears as restricted bodies, mostly represented by two-mica

135

sienogranites with medium- to fine-grained texture, commonly with magmatic

136

foliation.

137

peraluminous

138

environment (Cury, 2009).

139 140 141 142 143 144 145 146 147 148 149 150 151 152 153

Fig.1. A) Simplified tectonic map of the of the southern portion of Ribeira Belt and northeast part of Dom Feliciano Belt (south and southeast portion of Brazil). Legend: 1) recent sediments, 2) Curitiba Basin (Quaternary), 3) Paraná Basin (Phanerozoic); Southern Ribeira Belt: Ediacaran basins: 4) Castro, 5) Guaratubinha, 6) Campo Alegre; 7) Serra do Mar Suite (590-575 Ma); 8) Apiaí Terrane; Curitiba Terrane 9) Capiru (Mesoproterozoic) and Turvo-Cajati (Ediacaran) metasedimentary formations, 10) Atuba Complex (Paleoproterozoic); 11) Rio Piên Suite (Ediacaran); 12) Paranaguá Terrane; Dom Feliciano Belt: 13) Itajaí Foreland Basin (Ediacaran – Cambrian), 14) Neoproterozoic Brusque schist belt and intrusive granitoids, 15) Camboriu Complex (Paleoproterozoic), 16) Florianópolis Batholith (Ediacaran arc related granitoids), 17) Luis Alves Cratonic Block (Archean do Paleoproterozoic); 18) Main Shear Zones, 19) Neoproterozoic tectonic vergence (after Siga Junior, 1995; Basei et al., 2009; Cury, 2009; Passarelli et al., 2018 and references therein). B) Part of Western Gondwana reconstruction (red rectangle indicates Fig. 1A). Legend: Cratonic fragments: A Amazonia; SF – São Francisco; C-Congo; P - Paranapanema; L - Luis Alves; RP - Rio de la Plata; K -Kalahari; Mobile Belts: Aç – Araçuaí; Wc – West Congo; R – Ribeira; DF – Dom Feliciano; Ka – Kaoko; Da – Damara; G – Gariep (Adapted after Passarelli et al., 2018 and references therein).

154 155 156 157 158

Fig. 2. Geological map of the Paranaguá Terrane with part of the geochronological data available from Cury (2009), major lithological units, shear zones, mean foliations, stretching lineations and tectonic transport direction during the Ediacaran deformation (Modified after Cury, 2009). Cross-sections are indicated in the map.

potassium

The

quartz-dioritic,

geochemical association

data

related

leuco-granodioritic,

indicate to

an

monzogranitic

sub-alkaline anorogenic

to

signature

and

with

post-collisional

7

159

3. Methods

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Fieldwork resulted in four transects across the regional structural trend

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(Fig. 2) and some specific locations in the regions of: A) São Francisco do Sul

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Island - Garuva – Itapoá (southern Paranaguá Terrane in the Santa Catarina

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and Paraná State); B) Serra da Prata – Antonina – Paranaguá - Matinhos e

164

Guaratuba (central Paranaguá Terrane in the Paraná State); C) Salto Morato –

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Guaraqueçaba (northern Paranaguá Terrane in the Paraná State); D) Ariri -

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Iguape (northern Paranaguá Terrane in the São Paulo State). Microtectonic

167

analyses were carried out in a multiscale GIS project through the data obtained

168

from hand samples, thin-sections and structural data. In the same GIS system,

169

several geophysical maps were integrated to update the geological map of Cury

170

(2009), building a geological framework to organize the cross-sections and

171

stereograms of the Paranaguá Terrane in order to present a systematic

172

structural analysis of the area for further detailed studies.

173 174

3.1.

Aerogeophysical Methods

175

Magnetic domains and potential structures were interpreted from

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aeromagnetic data. Such structures were verified and compared with field and

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petrographic data. Additionally, regional aeromagnetic maps were made to

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discuss and evaluate how the magnetic anomalies and lineaments observed in

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the study area could be compared to adjacent tectonic units. Trying to avoid the

180

influence of the anomalies of the NW-SE Cretaceous dykes, a directional cosine

181

filter (300° azimuth) was applied to exclude most o f these anomalies and

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highlight the oldest structures.

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For the qualitative interpretation of gamma-spectrometric/lithological

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domains in the Paranaguá Terrane, due to higher mobility of potassium (Chan

185

et al. 2007) and uranium elements (Middelburg et al. 1988), which are greatly

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influenced by the strong erosion, weathering and landslides in the region

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(Silveira et al., 2014; Weihermann et al., 2016) the thorium map was used as

188

base. The analysis was made comparing the thorium map with the ternary

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composition map, trying to verify the quality of the interpretation of the domains

190

for further correlation with fieldwork data. Technical specifications of the

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airborne survey (after CPRM, 1978, 2011) and enhancement methods utilized

192

are shown in Table 1 (Supplementary Material 1).

9

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4. Results

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4.1.

Geophysical Framework

195

From the interpretation of the map of the vertical integral of the analytic

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signal amplitude (VIAS – Fig. 3), which highlights bodies with high magnetic

197

susceptibility and vertical extension, normally associated with regional

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representative structures (Paine et al., 2001), it was possible to observe that

199

the Paranaguá and Curitiba Terranes present low magnetic domains when

200

compared to the Luis Alves cratonic block.

201

Using enhancement methods, it is possible to observe the magnetic

202

anomalies in the Paranaguá Terrane and build a geophysical framework to

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support geological interpretations. Through the interpretation of maps as tilt

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Angle (TDR) and tilt angle of the horizontal gradient (THDR-TDR), two different

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domains were separated based on the direction and aspects of the lineaments

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of positive anomalies (Fig. 4). The first one, located in the southern part of the

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terrane, has a high density of N-S positive magnetic anomalies; and the second

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one, in the northern sector, shows NE-SW lineaments. Both domains reflect the

209

tectonic structures observed in the field (Section 4.2).

210

In the southern portion of the Paranaguá Terrane (Fig. 4C), rectilinear

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lineaments with 20 – 80 Km of length and 1 – 4 Km width with N-S direction are

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predominant, while shorter ones (2 to 10 Km length) with E-W direction offset

213

the first group (Fig. 4). The northern sector, on the other hand, shows a shift in

214

the direction and intensity of the lineaments, which are more continuous with

215

sigmoidal and anastomousing patterns and NE-SW to NNE-SSW direction (Fig.

216

4).

10

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Comparing the interpretation of the geological and aeromagnetic data

218

with the gamma-spectrometric maps (Fig. 5), it is possible to notice a positive

219

correlation between the high amplitude values of thorium (Fig. 5A) and ternary

220

composition (Fig. 5B) with the granitic suites of the Paranaguá Terrane (see

221

Fig. 2 and 5). The similarity between the geometry of the granites and the

222

magnetic lineaments suggests that the geological contacts of the study area

223

reflect a structural control, which was confirmed in the field and will be further

224

discussed in this work.

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Fig. 3: Regional aerogeophysical map of the vertical integral of the analytic signal amplitude (VIAS) applied to observe regional magnetic anomalies. It is noteworthy to observe the low magnetic values for the Paranaguá Terrane and a lower domain in between the two major magnetic blocks of Luis Alves Microplate.

230 231 232 233 234 235 236 237 238 239 240

Fig. 4: Aerogeophysical maps of the Paranaguá Terrane (Paraná and Santa Catarina region) of A) the tilt angle (TDR); B) tilt angle of the horizontal gradient (THDR-TDR) and C) structural domains interpreted using lineaments orientation and style.

Fig. 5. Aerogamaspecmetric maps of the Paranaguá Terrane of A) ternary composition; B) thorium anomalies and C) qualitative interpretation of thorium concentration in the terrane, usually high to high-medium amplitude values of thorium represent granitic suites in the area.

4.2.

241

Structural aspects of Paranaguá Terrane in southern and northern sectors

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The southern portion of the Paranaguá Terrane is structurally

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characterized by the development of steep foliations, mylonites and shear

244

zones (Fig. 2 and 6). The S1 (schistosities) is the main foliation of this sector

245

with the S2 showing different aspects (axial plane, crenulation, schistosities or

246

gneiss banding). These foliations present average directions of NS to N15-20W

247

(Fig. 6) with predominantly subvertical dip to E-SE for most of the units and

248

strike-slip stretching lineations, usually plunging between 11 to 20° to the south

249

(Fig. 6).

11

250

In this portion predominates high angle sinistral transpressional shear

251

zones (Fig. 7A,B,D) that occur internally and limiting the study area (Fig. 2 and

252

6). Near the shear zones the foliations tend to have mylonitic characteristics

253

with anastomosing and pervasive L-S type fabrics, also frequently associated

254

with small-scale isoclinal folding (1 – 40 cm wavelength -Fig. 7C), with fold axis

255

slightly oblique to parallel to the stretching lineation, usually defined by

256

muscovite, biotite, sillimanite and quartz. The mylonites frequently present

257

rotated porphyroclasts (Fig. 7D), S-C fabric and grain size reduction (see

258

section 4.3).

259

The main shear zones in this sector are: i) the NW-SE trending Palmital

260

Shear Zone, which establishes the contact between Luis Alves and Paranaguá

261

units (Fig. 2) and has narrow damage zone with strike-slip sinistral kinematics;

262

ii) the NE-SW trending Alexandra Shear zone, in the northwest contact between

263

Luis Alves and Paranaguá units (Fig. 2) with transpressional sinistral

264

kinematics, oblique to strike-slip stretching lineations and development of

265

mylonitic fabric in metasedimentary and granitic rocks; iii) the Cubatãozinho

266

Shear Zone, which occurs in the central portion of this sector (Fig. 2, 6), with

267

NNE-SSW strike and the development of a 3 to 5 km width proto- to mylonitic

268

zone with sinistral sense of shear and strike-slip characteristic and; iv) the

269

Guaratuba Shear Zone, which has N-S to N30E-S30W strike and represents

270

the contact between the southern and northern domains. It is a transpressional

271

shear zone with sinistral kinematics and development of metric and irregular

272

anastomosing mylonitic zones (alternating between low and high strain

273

domains).

274

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275 276 277 278

Fig 6. Geological cross sections (indicated in Fig. 2) and equal-angle stereograms of the southern portion of the Paranaguá Terrane, the green triangle represents the stretching lineations (L) and blue circles the fold axis (FA). A) A-A’ cross section and stereograms; B) B-B’ Cross section and stereograms.

279 280 281 282 283 284 285

Fig. 7. Structures observed in southern sector Paranaguá Terrane: A) Metagraywacke with quartz-feldspar sigmoid clast with sinistral shearing; B) High angle protomylonitic migmatite from the São Francisco do Sul Complex with sinistral kinematics (better indicated Fig. 7E); C) Isoclinal and disharmonic folding in migmatic orthogneisses; D) Rotated porphyroclasts in protomylonitic granite from the Morro Inglês Suite; E) Amphibole fish and sigma type K-feldspar porphyroclast with sinistral sense of shear in protomylonitic migmatite F) Sinistral S-C fabric in mylonitic migmatite.

286

The transition between the southern and northern blocks of the

287

Paranaguá Terrane is characterized by major granitic units and a gradual

288

change of the foliation strike and predominance of medium to high dip (Fig. 8A).

289

In this transition, the narrowing of the Luis Alves Microplate is noted in the

290

Antonina region (Fig. 3), with preferred high angle foliations with the main

291

direction of N30E (Fig. 2). Differently from the southern block, the rocks in this

292

region present less mylonitic deformation, which is usually concentrated near

293

shear zones found in the contacts among the major geological units or the

294

terrane limit.

295

In the northern portion, the foliations strike varies up to almost EW (Fig.

296

8B) and switch to N20-30E to the northern limit of Paranaguá Terrane. This

297

sector is characterized by foliations with medium to low dipping angle,

298

especially in Iguape (Fig. 9). The alternation and repetition between the

299

orthogneisses and the metasedimentary rocks in the region with asymmetric

300

structures indicating vergence to NW (Fig. 2 and 8) suggest regional thrust and

301

folding system. Kinematic indicators such as asymmetric boudins, suggestive of

302

sinistral sense of shear, are still observed in this portion (Fig. 10B)

303

The northern portion structures usually show asymmetric shapes (Fig.

304

10A), like overturned antiforms and sinforms, which turn to recumbent folds

13

305

close to the shear zones. Chevron folds (Fig. 10C), parasitic mesoscopic

306

asymmetric folds in Z pattern (Fig. 10A), as well as quartz-feldspar asymmetric

307

leucosomes, usually indicating vergence and tectonic transport to N-NW (Fig.

308

10D), were also observed in this sector. This vergence is also supported by the

309

low angle mylonitic structures, with down-dip stretching lineation plunging 10° to

310

30° to SSE in shear bands, quartz ribbon, S-C pairs

311

porphyroclast rotation kinematics. A late stage of deformation affecting these

312

structures can be suggested by plunging of the fold axis from 3 to 40° for both

313

NE and SW (Fig. 8), as well as stretching lineations dispersion (Fig. 9).

and K-feldspar

314

The main shear zones in the northern sector are thrusts represented by:

315

i) the Serra Negra Shear Zone, in the northwestern contact between the

316

Paranaguá Terrane and the NE portion of Luis Alves unit and part of the

317

Curitiba Terrane, where occur low angle mylonites with downdip stretching

318

lineations (Fig. 2) and; ii) the Icapara Shear Zone, in the contact between the

319

Curitiba and Paranaguá Terrane with thrust verging to north/northwest and low

320

angle foliations (Fig. 9). Small sinistral strike-slip shear zones were also

321

observed in some portions of the northern domain.

322 323 324 325 326 327

Fig. 8. Geological cross sections (indicated in Fig. 2) and equal-angle stereograms of the northern portion of the Paranaguá Terrane (same legend as Fig. 6): A) cross section C-C’ and stereograms related B) cross section D-D’ and steregrams showing the asymmetric folding indicating top to N-NW and some geological characteristics and relation between the geological units of the Paranaguá Terrane.

328 329 330 331

Fig. 9. Stereograms of the metasedimentary rocks from the Rio das Cobras Succession and granitoids in the most northwestern region (Iguape) in the Paranagua Terrane.

332 333 334 335 336 337

Fig. 10. Photographs showing the main structural aspects observed in the northern sector of Paranaguá Terrane: A) Mtype asymmetrical folds in migmatitic gneiss from the São Francisco do Sul Complex; B) asymmetrical boudinage in moderate angle dipping S2 foliation (sinistral kinematics); C) Orthogneiss with chevron folds; D) migmatitic paragneiss with asymmetrical sigmoidal leucosomes indicating top-to-NW in Iguape region.

14

338

A common characteristic for both sectors and all units of the Paranaguá

339

Terrane is the presence of brittle structures, with oblique to perpendicular strike

340

in relation to the main ductile structures with subvertical dip. These structures

341

are related to deformation at upper crustal levels and are represented by small

342

faults, fractures, joints and veins, commonly filled by calcite, epidote and quartz.

343

The structural characterization of the Paranaguá Terrane units and their

344

particularities are presented below.

345 346

4.2.1. São Francisco do Sul Complex

347

This unit crops out with a gneiss banding and local migmatic aspect (Fig.

348

7C), formed by segregation of quartz-feldspar bands and mafic levels with

349

oriented biotite parallel to the S1 foliation. The migmatic textures tend to occur

350

next to the contact with the granitic suites. In this unit the occurrence of

351

crosscutting foliations only occurs next to shear zones with the development of

352

mylonitic foliations that transpose partially the S1 foliation with dynamic

353

recrystallization of the quartz and reorientation of biotites and amphiboles. (i.e.

354

the interference between low and high angle tectonics can be observed in a

355

same outcrop – Fig. 11A).

356

It is noteworthy to observe that the São Francisco do Sul Complex

357

appears discordant with the structural pattern in some regions (Fig. 6A, 8A) with

358

low to high dipping foliations. Structures as asymmetric folding indicating top to

359

N-NW, leucosomes with sinistral kinematic (Fig. 7B) and oblique stretching

360

lineation are commonly observed.

361 362

4.2.2. Rio das Cobras Succession

15

363

In the Rio das Cobras Succession, a continuous schistosity(S1) is

364

defined by the orientation of biotite, muscovite and quartz, frequently parallel to

365

the compositional banding. This foliation represents the metamorphic green-

366

schist facies regional metamorphism (garnet isograd) and locally reaching low

367

amphibolite facies. The S2 foliation development was observed with different

368

intensities: i) near shear zones and far from granites bodies this foliation occur

369

as axial planes, crenulate cleavage (Fig. 11B), schistosity or mylonitic foliation

370

(strain increasing) with low grade mineral assemblage (Bt + Ms + Qtz); ii) near

371

shear zones and granitoids, this foliation occurs as schistosity, gneisses

372

banding with mineral assemblage of Pl + Sil + Bt + Qtz ± Kfs (locally migmatitic

373

textures -Fig. 11C) or high temperature mylonites. Late retrograde reactions,

374

usually observed next to the shear zones, are commonly described affecting the

375

regional metamorphism and high-grade mineral assemblage from S2 foliation,

376

which can form low temperature mylonites or simply consume the previous

377

mineral assemblage.

378 379

4.2.3. Granite Suites

380

The granitic suites of the Paranaguá Terrane show a complex

381

relationship with the development of foliations since there are different tectonic

382

moments of crystallization during the accretionary, collisional and post-

383

collisional setting (Cury, 2009). The granitoids in the terrane are either isotropic

384

or foliated. However, most of the batholiths appear oriented parallel with the

385

regional strike and dip of the near shear zones or geological units (Fig. 2,5,6,8).

386

In the Morro Inglês Suite, the magmatic foliation is frequent and near most

387

shear zones crops out with metric bands of mylonitic foliation (Fig. 11D). On the

16

388

other hand, the Canavieiras-Estrela Suite most of the time presents tectonic

389

foliation (Fig. 11E), while the Rio do Poço mostly crops out isotropic or with

390

magmatic foliation.

391 392 393 394 395 396 397 398 399

Fig. 11. A) Interference between low angle asymmetric folding and sinistral strike-slip tectonics on migmatitic orthogneiss from the São Francisco do Sul Complex; B) Metapelite in the northern portion of Paranaguá Terrane with S1 foliation, parallel to the compositional banding, with the development of a S2 crenulation cleavage; C) paragneiss with a relict garnet preserving the S1 foliation as perpendicular/oblique inclusion trails in relation to a well-developed S2 foliation defined by fibrolitic sillimanite, biotite and quartz (southern Paranaguá). Mineral assemblage phases show partial retrograde consume to white mica; D) Magmatic and tectonic foliation relationship, next to Guaratuba Shear Zone from the Morro Inglês Suite; E) Mylonitic granite from the Canavieiras-Estrela Suite in Cubatãozinho Shear Zone.

400 401 402 403

4.3.

Petrotectonics analysis

Through microstructural analysis, it was possible to observe two types of dynamic recrystallization: high- and low-temperature processes. The high-temperature mylonites are observed in gneisses from São

404

Francisco

do

Sul Complex,

Canavieiras-Estrela

Suite

and mainly in

405

paragneisses from Rio das Cobras Succession (Fig. 12A, B). These mylonites

406

present quartz dynamic recrystallization with high temperature chess-board

407

extinction with sillimanite inclusion (Fig. 12A), grain boundary migration (Fig.

408

12B) and bulging of feldspar, suggesting temperatures above 500°C (Stipp et

409

al., 2002; Passchier and Trouw, 2005; Stipp and Kunze, 2008). However, these

410

mylonites and recrystallization mechanisms are rarely preserved due to the low

411

temperature overprint of shear zones. High temperature conditions are also

412

recognized in the mineral assemblage of Rio das Cobras Succession (Sil + Kfs

413

+ Bt), as well by local migmatitic evidences (schlieren and ribbons) in rocks of

414

the São Francisco do Sul Complex.

415

Low temperature mylonites are more often recognized in the Paranaguá

416

Terrane, usually forming rocks with a predominance of quartz recrystallized by

417

subgrain rotation and bulging recrystallization (Fig. 12C, D) and microfractures

17

418

in feldspars (Fig. 12C). These microstructures are recognized in all units,

419

occurring near major shear zones. This deformation suggests temperatures

420

between 400-500° C (Stipp et al., 2002; Passchier a nd Trouw, 2005; Stipp and

421

Kunze, 2008).

422 423 424 425 426 427 428

Fig. 12: A) Chess-board patter in quartz with sillimanite inclusion in a paragneiss from the Rio das Cobras Succession; B) Paragneiss next to Icapara Shear Zone (northern Paranaguá) showing High-T dynamic recrystallization (Grain boundary migration); C) Protomylonitic migmatite from the São Francisco do Sul Complex showing ductile recrystallization of the quartz (bulging and subgrain rotation) while the K-feldspar has microfractures and discrete undulose extinction; D) Mylonitic granite thin section in Cubatãozinho Shear Zone with quartz recrystallized by subgrain rotation and bulging indicating sinistral movement.

18

429

5. DISCUSSION

430

5.1.

Strutural patterns and strain partitioning in Paranaguá Terrane

431

The geophysical and structural data clearly individualized two structural

432

domains in the Paranaguá Terrane (see section 4). The southern sector is

433

mainly formed by steep N-S to NNE-SSW striking foliations with a

434

predominance of strike-slip to oblique stretching lineations (Fig. 2,6), frequently

435

associated with the development of structures with sinistral kinematics (Fig. 7)

436

and

437

contrastingly, present more moderate to low angle dipping foliation with NE-SW

438

to E-W strike and oblique to downdip stretching lineations (Fig. 8,9). In this

439

portion, folding and thrust system were recognized by low angle shear zones

440

and asymmetrical folding indicating top-to-N-NW (Fig. 10).

strike-slip

to

transpressional shear zones.

The

northern

sector,

441

It is suggested that these structural patterns were a product of an oblique

442

collision, mainly related to the geometry of several tectonic blocks and transport

443

direction (Fig. 13). It is probable that the irregular geometry of the Luis Alves

444

Cratonic fragment induced a partitioning of deformation with main crustal

445

shortening direction to NNW. In oblique collisions, the formation of different

446

regimes of deformation, as described in the southern and northern sectors of

447

the Paranaguá Terrane is common (Tikoff and Teyssier, 1994). Portions with an

448

angle of collision below 30° tend to have a deforma tion controlled by simple

449

shearing, while in places with collision obliquity higher than 30° prevail pure

450

shear deformation (Fig. 13; Tikoff and Teyssier, 1994; Teyssier et al., 1995).

451

Thus, the Luis Alves led to a transpressional oblique collision through a

452

lateral escape of the Paranaguá Terrane, represented by the Palmital Shear

453

Zone (lateral ramp), and juxtaposition to Luis Alves and Curitiba units further

19

454

north. In the southern sector, where the geometry of the cratonic block and the

455

tectonic transport has low obliquity (Fig. 13), sinistral simple shearing

456

represents the main deformational pattern (Fig. 6, 7). The northern sector, on

457

the other hand, presents high angle of obliquity (Fig 13), where pure-shear

458

deformation structures were mostly developed (Fig. 8, 10), especially in Iguape

459

(Fig. 9).

460 461 462 463 464 465 466 467 468

Fig. 13: A) Regional aeromagnetic lineament interpretation of positive anomalies based on tilt angle map, showing the pattern of the structures in different Terranes and tectonic units of southeast and south of Brazil, special emphasis on number 1 (Paranaguá Terrane) lineament directions, 2 (Luis Alves Cratonic Block) with divergent pattern, 4 (Brusque unit – Dom Feliciano Belt) with lineament converging into Palmital Shear Zone (PASZ); B) Arrow showing tectonic transport and the angles indicating the increase of obliquity to the northern part of Paranaguá Terrane resulting in strain partitioning and practically perpendicular convergence with Dom Feliciano Belt (Brusque Group); C) Tilt angle map (TDR)

469 470

5.2.

Structural evolution of the Paranaguá Terrane

The

Paranaguá

Terrane

presents

granite

bodies

with

different

471

geochemistry signatures and geochronological ages (Siga Jr, 1995; Cury, 2009)

472

that difficult the hierarchy of the structures. On the other hand, mineral

473

assemblage and petrotectonic features developed by distinct tectonic

474

processes, associated with available geochronological data, can help to build

475

structural models for specific time intervals. To better constrain the results

476

obtained, the structural evolution in the Paranaguá Terrane can be divided in

477

two main moments: a progressive D1 deformation, related to the broad

478

crystallization granite in the area, between 640 – 580 Ma (Cury, 2009), and the

479

D2, which we link to Cambrian (Cury, 2009) late reactivations.

480

The progressive D1 deformation is separated in early and late D1. The

481

early D1 (640 – 610) is correlated with the beginning of the magmatism (638 ±

482

10, 617 ± 10 Ma, 615 ± 7, 614 ± 9 Ma; Basei et al., 1990; Cury, 2009), with arc-

483

related granite crystallization (Cury, 2009). The structures associated with early

20

484

D1 are the regional S1 foliation in the metasedimentary rocks, with greenschist

485

to lower amphibolite metamorphism facies (Patias et al., 2019, submitted) and

486

gneiss banding (locally migmatitic) in the São Francisco do Sul Complex,

487

evidenced by U-Pb zircon rims age with 625 ± 25 Ma (Cury, 2009), usually

488

related to thrusting (Fig. 11A, 14).

489

The late D1 (610 – 580 Ma) represents the progression of deformation

490

with peak of granite crystallization around 600 Ma (610 ± 5, 609 ± 28, 601 ± 7,

491

598 ± 20, 592 ± 13, 588 ± 6, 583 ± 10, 581 ± 19, 577 ± 5 Ma; Basei et al., 1990;

492

Siga Jr, 1995; Cury, 2009) and late stages of post-collisional granite

493

crystallization (Cury, 2009). The deformation in this period is related to high-

494

temperature mylonites (Fig. 11B) near shear zones and granitic batholiths, as

495

well

496

metasedimentary rocks, recording prograde metamorphism in the area

497

(Guimaraes, 2019). This moment is coeval with the partition of the

498

transpression (see section 5.1) and development of strike-slip shear zones in

499

the southern portion and thrusting and folding in the northern sector of

500

Paranaguá Terrane (Fig. 14). This is supported by the high temperature

501

mylonites or high-grade mineral assemblage in both sectors and ages

502

constrained between 611 and 599 Ma acquired by Cury (2009) in zircon

503

metamorphic rims (Fig. 2) and monazites, respectively. It is noteworthy that

504

most granites show regional concordance with the structural pattern (Fig.

505

2,6,8,9) and magmatic foliation parallel to it; so we argue that the granites used

506

the shear zones development as emplacement conduits at this moment.

as

and

S2

foliation

with

high

grade

mineral

assemblage

in

507

The transition between D1 and D2 is represented by a probable tectonic

508

quiescence with lack of isotopic data between 580 – 540 Ma or the absence of

21

509

more geochronological data. The D2 (540 – 500 Ma) is mainly correlated with

510

isotopic data from the Cambrian, mainly K-Ar ages in biotites (544 ± 19, 544 ±

511

11, 536 ± 17, 530 ± 10 Ma, 520 ± 15, 504 ± 4 Ma; Basei et al., 1990; Siga Jr,

512

1995; Cury, 2009) and sparse and localized U-Pb ages (540 ± 13, 535 ± 49,

513

498 ± 5 Ma; Cury, 2009), mostly related zircon metamorphic rims. This

514

deformation probable took place under low temperature retrograde conditions,

515

with shear zones reactivations producing low temperature mylonites (Fig. 12C,

516

D) and regional cooling and exhumation after granite emplacement.

22

517

5.3.

Regional implications

518

The Paranaguá Terrane distinct itself from the other tectonic units within

519

the Southern Ribeira Belt, especially by the large volume of granite bodies and

520

its structural evolution (this work). Part of these characteristics and similar ages

521

of deformation is also observed in the Dom Feliciano Belt (Basei et al., 2011;

522

Oriolo et al., 2016; Hueck et al., 2018), which is considered to be the probable

523

continuation of the Paranaguá Terrane in a broader mobile belt (Basei et al.,

524

1990, 1992; Cury, 2009; Bruno et al., 2018).

525

Hueck et al. (2019) individualize three main periods of evolution of

526

deformation in the northern Dom Feliciano (Santa Catarina sector). The first

527

stage (650 – 615 Ma), responsible for regional metamorphism (Philipp et al.,

528

2004; Basei et al., 2011) and low angle dipping structures (Hueck et al., 2019).

529

The deformation progressed to transpression (615 – 585 Ma) with pure shear

530

dominated dextral strike-slip (Oyhantcabal et al., 2011; Passarelli et al., 2011;

531

Hueck et al., 2019), development of shear zones and continuous emplacement

532

of granites (Hueck et al., 2019) that was also responsible for the second

533

metamorphic episode in the metasupracrustal rocks (Philipp et al., 2004; Basei

534

et al., 2011). Late stages of deformation (585 – 550 Ma) are recognized by

535

progressive deformation under cooling conditions (Hueck et al., 2019) and

536

correlated with K-Ar ages near the Major Gercino Shear Zone (Passarelli et al.,

537

2010).

538

We suggest that these similarities argue in favor that during late

539

Cryogenian and early Ediacaran, the Paranaguá Terrane and the Dom

540

Feliciano Belt share a common evolution (Fig. 14). However, during the

541

convergence of the continental terranes in the Ediacaran onto the Luis Alves

23

542

cratonic block, its irregular geometry forced the lateral scape of the Paranaguá

543

Terrane and development of a sinistral transpressional orogen (Fig. 14). The

544

northern Dom Feliciano, in the other hand, was forced into a high obliquity

545

collision (co-axial) with NW tectonic transport and developed a transpressional

546

orogen controlled by dextral pure-shear deformation (Passarelli et al., 2010,

547

2011; Oyhantcabal et al., 2011; Hueck et al., 2019). It is noteworthy that the

548

Paranaguá Terrane and the Dom Feliciano Belt show a contrasting isotopic

549

record after ca. 580 Ma, which could suggest that after this period both units

550

started to have an individualized tectonic history.

551 552 553

Fig. 14: Schematic Paranaguá Terrane and near crustal blocks and the evolution of the D1 progressive deformation.

24

554

6. Final Remarks

555

•

An integrated analysis of aerogeophysical maps and structural data,

556

together with geochronological data, indicates that the Paranaguá

557

Terrane was a product of a transpressional orogeny resulting from a

558

complex interaction of the Luis Alves Cratonic block with adjacent

559

terranes in the Ediacaran.

560 561

•

The convergence in the NNW direction generated a partitioning of the

562

deformation due to an increase of collision obliquity further north and

563

created portions dominated by simple-shear (southern sector) and by

564

pure-shear (northern sector) deformation. This is reflected by different

565

patterns, directions and styles of deformation in the Paranaguá Terrane.

566 567

•

Observed structures resulted from two deformation events, D1 and D2.

568

The D1 event is related to a progression of deformation and the main

569

stage of granite crystallization. The early D1 (640-610 Ma) is associated

570

with regional metamorphism and low angle tectonics, with N-NW tectonic

571

transport. The late D1 (610-580 Ma) is correlated with the strain

572

partitioning and development of shear zones in the southern and

573

northern sectors; structures with sinistral kinematics coupled to broad

574

granite crystallization and emplacement. The D2 (540-500 Ma)

575

represents a late deformation stage, with low temperature reworking,

576

especially next to shear zones.

577

25

578

•

The structural pattern, geological and geochronological similarities

579

suggest that the northern Dom Feliciano Belt and the Paranaguá Terrane

580

could represent a unique mobile belt, which were separated during the

581

Ediacaran by a lateral escape of the latter through the Palmital Shear

582

zone and Luis Alves block irregular geometry. This triggered strain

583

partitioning and created an opposite sense of shearing with sinistral and

584

dextral kinematics in the Paranaguá Terrane and northern Dom Feliciano

585

Belt, respectively.

586

26

587 588

Acknowledgments The

authors

are

thankful

to

the

funds

from

the

589

PETROBRAS/LAMIR/FUNPAR Microbial Project (n° 23075. 120789/2016-11);

590

The Fieldwork collaboration from the geologists Gustavo Machado Marangon,

591

Msc. Eduardo Menozzo da Rosa, Msc. Larissa Santos and Msc. Guilherme

592

Fedalto; The geophysicist Francesco Antonelli and the geologists Msc. Jessica

593

Weihermann and Msc. Luizemara Szameitat in the geophysics processing; The

594

team from the Laboratório de Análise de Minerais e Rochas (LAMIR-UFPR);

595

The support from Federal University of Paraná (UFPR) and the Geology

596

Department (DEGEOL-UFPR); The reviewers Dra. Renata Schmitt and Dr.

597

Sebastián Oriolo for the careful suggestions for the improvement of the

598

manuscript.

599 600

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•

Geophysics and structural analysis characterize a transpressional collision;

•

Different structural domains are related to the geometry of Luis Alves block;

•

Southern and northern domains present simple and pure-shear deformation respectively;

•

Isotopic data individualizes two deformation stages: D1(Ediacaran) and D2(Cambrian).