Central Brazil - UFOP

\PERGAMON Geodynamics 17 "0888# 156Ð178

9153!2696:88:, ! see front matter Þ 0888 Elsevier Science Ltd[ All rights reserved[PII] S9153!2696 "87#99931!7

Neoproterozoic geotectonic evolution of TocantinsStructural Province\ Central Brazil

Adelir Jose� Striedera\�\ Marcos Tadeu de Freitas Suitab

aDepartment of Mining Engineering*EE*Federal University of Rio Grande do Sul "UFRGS# Cx[ P[ 847 CEP 89[990!869 Porto Alegre\ RS Brazil

bMining Department*EM*Federal University of Ouro Preto "UFOP# CEP 42[399!999 Ouro Preto\ MG Brazil

Received 4 March 0886^ accepted 8 February 0887

Abstract

Tocantins Structural Province "TSP# is the main tectonic feature in Central Brazil[ It separates two maincratonic areas " former continental plates#] the Amazonian Craton to the West and the Sa½o Francisco Cratonto the East[ Recent geochronological data "UÐPb and SmÐNd# and structural studies show that the actualstructural framework of the province was developed during the Neoproterozoic[ It is herein proposed thatBrasiliano Orogenic Cycle in the TSP was developed in four broad tectonic stages] 0# an ocean openingstage began possibly 0169Ma^ 1# an island!arc system development stage started 0999Ma and its amal!gamation lasted until ca[ 799Ma^ 2# a continental collision stage began ca[ 799Ma with the accretion of theisland!arcs to the upper Amazonian plate\ the closure of the Goia�s Ocean and the development of a forelandbasin upon the lower Sa½o Francisco plate^ and 3# a post!collisional stage "549Ð499Ma# with the developmentof transcurrent faults "Transbrasiliano lineaments#\ back!thrust reverse faults\ and intrusion of alkalicgranitic plutons[ Þ 0888 Elsevier Science Ltd[ All rights reserved[

0[ Introduction

The Tocantins Structural Province "TSP\ Almeida et al[\ 0870# is an elongated fold and thrustbelt located in Central Brazil "Fig[ 0#[ It is characterized by a speci_c disposal of structurallineaments "Fig[ 1#[ In its northern part\ the lineaments are roughly NÐS^ near the 04>29?S parallel\however\ the western lineaments turn toward the west and then toward the south[ The easternlineaments are aligned SSE despite minor in~ections and reach the 10>S parallel\ where they turnsharply toward the west for 149 km and then sharply toward the ESE de_ning a tectonic syntaxis"Serra da Canastra In~ection\ Strieder and Nilson\ 0882b#[ The lineaments rising from this tectonicsyntaxis trend ESE for more than 249 km and turn toward the SW to make up the Cunha

� Corresponding author[ E!mail] adelirÝlapes[ufrgs[br

A[J[ Strieder\ M[T[d[F[ Suita : Geodynamics 17 "0888# 156Ð178157

Fig[ 0[ Lithotectonic sketch of the Tocantins and Mantiqueira structural provinces\ Brazil "after Strieder\ 0882a\ 0882b#[

A[J[ Strieder\ M[T[d[F[ Suita : Geodynamics 17 "0888# 156Ð178 158

Fig[ 1[ Generalized lineament sketch of the main structural elements in the TSP[ The structural lineaments in the easternsub!province "Bras(�lia subprovince# are from Strieder "0882a#^ the structural lineaments of the western ParaguaiÐAraguaia subprovince are modi_ed from Hasui and Costa "0889# and the map from Schobbenhaus Filho et al[ "0873#^the structural lineaments from Cunha de Guaxupe� region are modi_ed from Hasui et al[ "0889#[


de Guaxupe� "Hasui et al[\ 0889#[ Both lineament branches of the TSP are built mainly uponmetasedimentary rocks and have been named ParaguayÐAraguaia "the western# and Bras(�lia "theeastern# subprovinces "Strieder\ 0882a#[ These provinces are separated by an older granite!gneissicbelt\ large metamorphosed and deformed ma_c!ultrama_c and granitic intrusions\ and Archeanand Proterozoic volcano!sedimentary units[

Regional geological survey at TSP began in 0859|s and the _rst tectonic scheme was proposedby Almeida "0856#\ on the basis of Geosynclinal theory[ A later tectonic framework distinguished0# the Goia�s Median Massif formed by the oldest rock units\ 1# the Uruacžuano Belt composed byAraxa� metasedimentary unit with alpine!type ma_c and ultrama_c bodies earlier envisaged as theeugeosynclinal counterpart of the 2# eastern fold belt "Bras(�lia Belt#\ and the 3# western foldbelt "ParaguayÐAraguaia Belt#[ This framework was based on the _rst geochronological datingprogrammes "Almeida\ 0857^ Hasui and Almeida\ 0869^ Almeida et al[\ 0865#[ In the end of 0869|sand during the _rst half of the 0879|s\ the tectonic setting of the TSP was described on the basisof the Mobile Belt hypothesis "Almeida et al[\ 0879^ Lesquer et al[\ 0870^ Haralyi and Hasui\ 0870^Cordani and Brito Neves\ 0871#[ By this time\ the discussion was focused on the operation of one"Brasiliano# tectonic cycle "Cordani and Brito Neves\ 0871#\ or two "Uruacžuano and Brasiliano#tectonic cycles "Almeida et al[\ 0866^ Almeida et al[\ 0879^ Haralyi and Hasui\ 0871#[ In the secondhalf of the 0879|s\ Hasui and Haralyi "0874# reinterpreted strong linear gravimetric anomalies asthe locus of a continental suture on the basis of the plate tectonics^ however\ they regarded themain TSP features as long!lived structures inherited and reactivated since Archean times[ Hasuiand Haralyi "0874# also interpreted the TSP tectonic framework as evolved by superposed obliqueconvergence episodes in an ensialic environment[ Thus\ the dispute about the TSP evolution wasfocused on repeated movements along preferential structures during several tectonic cycles "e[g[Marini et al[\ 0873^ Hasui et al[\ 0883#\ or on the amalgamation and juxtaposition of di}erent oldercontinental fragments in the Brasiliano orogenic cycle "Brito Neves and Cordani\ 0880#[

Nowadays\ several rigorous geochronological results have been published "e[g[] Pimentel andFuck\ 0881^ Pimentel et al[\ 0880a 0880b\ 0881\ 0882a\ 0882b^ Ferreira Filho et al[\ 0883^ Suita etal[\ 0883a\ 0883b# that constrain the Neoproterozoic geotectonic evolution of TSP[ Also\ recentpetrochemical results on alpine!type bodies\ tectonically emplaced in the Araxa� metasediments\permit to recognize an ophiolitic melange related to the Hasui and Haralyi|s "0874# linear gravi!metric anomaly "Strieder and Nilson\ 0881a#[ Strieder "0882b# also described a number of structuralin~ections in the Bras(�lia subprovince\ similar to those described by Coward and Potts "0872#\ thatare at high angles to the linear gravimetric anomaly and point to frontal collisional tectonics[ Fuck"0883# also presented a brief framework to the TSP\ describing the inner composition of eachtectonic entity^ however\ he did not address considerations on timing and structural evolution ofthe province[

This paper presents an overview of the Neoproterozoic tectonic evolution of the TSP[ It is basedon structural features and constrained mainly by high precision UÐPb and SmÐNd ages[ Theoperation of a complete orogenic cycle during the Neoproterozoic of the TSP is related toagglutination processes that led to the formation of the Gondwana Supercontinent[ The _rstsection deals with the nature of the pre!Neoproterozoic continental lithosphere "i[e[ the cratonicareas related to the Brasiliano Orogenic Cycle#\ in order to examine the nature of Goia�s MedianMassif and the time constraints for the presence of an oceanic lithosphere in that region[ The secondsection deals with the Neoproterozoic structural framework\ discusses the main lithotectonic units


of the TSP and comments the observed structures[ The third section considers the geochronologicalconstraints of the Neoproterozoic Brasiliano Orogenic Cycle in the TSP[ Finally\ an integrateddiscussion of all these data is used to build up a tectonic scenario as to where TSP framework wasdeveloped[

1[ The intervening continental lithosphere

The TSP developed between two continental areas "plates# during the Meso! to Neoproterozoicof Central Brazil] the Amazonian "ASP# and Sa½o Francisco "SFSP# structural provinces "Almeidaet al[\ 0870^ Brito Neves and Cordani\ 0880#[ The northeastern limit of the TSP is covered by theParna(�ba Basin\ while the southwestern limit is covered by the Parana� Basin "Fig[ 0#^ so\ the presentdiscussion is focused on exposed areas[ The older central part of the TSP "Goia�s median massif#has similarities with Amazonian and San Francisco plates "Suita and Chemale Jr[\ 0884#[ It involvesseveral Archean tonalite!throndjemite!granite!greenstone belt associations "Danni et al[\ 0871#\Lower to Mesoproterozoic granite!gneisses units "Hasui and Costa\ 0889#\ large layered ma_c!ultrama_c bodies "Ferreira Filho et al[\ 0883^ Suita et al[\ 0883a\ 0883b#\ some MesoproterozoicA!type granites and their volcano!sedimentary counterparts "Pimentel et al[\ 0880a#\ and someupper Mesoproterozoic ma_c!felsic intrusions and volcano!sedimentary sequences "Suita\ 0885^Suita et al[\ 0883a\ 0883b#[

The most relevant lithotectonic associations in TSP "Figs 1 and 2# are the anorogenic granites andthe large layered ma_c!ultrama_c intrusions "Barro Alto\ Niquela¼ndia and Canabrava complexes#[They indicate divergent tectonic regimes associated with lithospheric stretching\ that could cul!minate in the formation of the oceanic crust[ In the Amazonian plate\ it is possible to distinguishtwo episodes of anorogenic granite generation] 0# the lower Mesoproterozoic granites of AmazoniaCentral dated 0[7 to 0[3 Ga\ and 1# the upper Mesoproterozoic granites of Juruena and Rondoniaregions dated 0[3 to 9[8 Ga "Dall|Agnol et al[\ 0876#[ The equivalent association in central part of theTSP is made up by the lower Mesoproterozoic granites and their volcano!sedimentary associations"Marini and Botelho\ 0875^ Pimentel et al[\ 0880a#[ The recent dating of the large layered ma_c!ultrama_c intrusions in Central Goia�s "Ferreira Filho et al[\ 0883^ Suita et al[\ 0883a\ 0883b#clearly de_ned an intracontinental divergent tectonic regime during the lower Mesoproterozoicand produced a clue on the origin of the anorogenic granites as earlier envisaged by Dall|Agnol etal[ "0876# and later discussed by Nilson et al[ "0883# and Suita et al[ "0883a\ 0883b#[ Suita et al["0883b# proposed a plume mantle model for the subcrustal ma_c underplating and generation ofthe A!type granites in the TSP during the lower Mesoproterozoic[

However\ no record of an orogenic cycle is found in central TSP after the Mesoproterozoicanorogenic episode\ as one can observe for the same period in Amazonian plate "Rio NegroÐJuruena Province] Dall|Agnol et al[\ 0876\ 0883^ Brito Neves and Cordani\ 0880#[ Thus\ it isadmitted that lithospheric stretching in the TSP area does not lead to an open ocean[ It is thusassumed that the lower Mesoproterozoic divergent tectonic regime has also a heterogeneousdistribution and evolution[

On the other hand\ some recent results point to a possible upper Mesoproterozoic divergenttectonic regime in the TSP area "Table 0#[ Suita et al[ "0883a\ 0883b# have dated a pegmatitichornblende grabbro by UÐPb multigrains fractions and found an upper intercept of 0179202 Ma[


Fig[ 2[ Sketch of main lithotectonic units and structures used to demonstrate the tectonic framework of the TSP[ Thebase map of this _gure is the same as that of Fig[ 0[ See text for additional discussion[


Table 0Compilation of geochronological data for TSP

Reference Geological unitsGeochronological method InterpretationResults

I*Emplacement of large ma_c!ultrama_c complexes of TSP "0\669 to 0\599 Ma#

Suita et al[ "0883a\ 0883b#^ Suita "0885# Barro Alto Layered Ma_cÐUltrama_c ComplexUÐPb multigrains fraction Age of magma di}erentiation and crystallization0\618210 Ma for the upper interceptFerreira Filho et al[ "0883# Niquela¼ndia Layered IntrusionUÐPb single grains Minimum age of magma di}erentiation and0\459Ð0\599 Ma for the upper intercept crystallization

II*Emplacement of A!type intra!continental magmatic rocks "0\669 to 0\599 Ma#

Pimentel et al[ "0880a# Goia�s Tin Province\ Central BrazilUÐPb single and multigrainsca[ 0\658 Ma for the upper intercept^ the lower intercept Soledade and Sucuri granites from the eastern Riois consistent with Pb!loss during thermal events of Parana½ subprovinceBrasiliano episodes "ca[ 549 Ma#[ Inherited componentsolder than 1[1 Ga0\503 to 0\463 Ma for the upper intercept Serra da Mesa Granite from western Rio Tocantins

subprovince0\66021 Ma for the upper intercept Acidic volcanics from Ara(� volcanosedimentary unit

III*Emplacement of ma_c and felsic igneous rocks "0\299 to 0\199 Ma#

Suita et al[ "0883a\ 0883b#^ Suita "0885#UÐPb multigrains fraction Serra da Malacacheta intrusive gabbro0\179202 Ma for the upper intercept Age of magma di}erentiation and crystallizationUÐPb multigrains fraction 0\15628 Ma CordieriteÐsillimanite gneiss probably from thefor the upper intercept Juscela¼ndia volcanosedimentary sequence

Development of granites and of volcanosedimentarysequences "bimodal magmatism# in an extensional regime

IV*Development of Calc!alkaline granites "849 to 799 Ma#

Pimentel "0889#^ Pimentel et al[ "0880b#^ Pimentel andFuck "0881#^ Pimentel et al[ "0882a#^ Pimentel et al["0882b#^ Viana and Pimentel "0883#UÐPb multigrain fraction of zircon\ SmÐNd model ages Granite!gneisses from the Areno�polis and Mara Rosaand RbÐSr isochron ages regions0[06 to 9[74 Ga SmÐNd model ages for granite!gneisses Age of primitive magma formationwith positive eNd Age of primitive magma crystallization


Table 0*continued


78826 Ma for the U!Pb upper intercept^ lower intercept Age of main metamorphic!deformational eventis concordant with sphene analysis "ca[ 526 Ma# Areno�polis\ Matrinxa½ and Sanclerla¼nda granite!ca[ 745 Ma "U!Pb single zircon age# gneisses and Jaupaci subvolvanic granite

Tonalitic gneiss from Mara Rosa region

V*Development of volcanosedimentary sequences "849 to 799 Ma#

Pimentel "0889#\ Pimentel et al[ "0880b#\ Pimentel andFuck "0881#\ Pimentel et al[ "0882a\b#\ Viana andPimentel "0883#U!Pb multigrain fractions of zircon\ Sm!Nd model agesand Rb!Sr isochron ages0[26 to 9[81 Ga Sm!Nd model ages for metarhyolites Age of primitive magma formationand metabasalts with positive eNd

81827 Ma and 653203 Ma for the upper intercept of Areno�polis\ Ipora� and Jaupaci volcanosedimentarymetarhyolites from Areno�polis and Jaupaci volcano! sequences associated with the calc!alkaline granite!sedymentary sequences^ lower intercept is concordant gneisseswith sphene analysis "ca[ 599 Ma# Island!arc volcanosedimentary sequences

Age of primitive magma crystallization and mainmetamorphic!deformational event

75127 Ma "U!Pb single zircon age# Age of primitive magma crystallization for Mara Rosametavolcanics

I*Metamorphism of low to medium grade metasedimentary sequences "Serra da Mesa#

Cassedane et al[ "0861# Sulphide lenses and veinlets in a thin dolomitic layeremplaced in a calcschist quartzite sequence 209 kmENE of Uruacžu� city "Porto Maranha½o#

PbÐPb in galenas0929269 Ma Age of metamorphic!deformational event

VII*Granulite facies metamorphism in the upper thermally softenned plate "799 to 549 Ma#

Suita et al[ "0883a\ 0883b#^ Suita "0885#UÐPb multigrains fraction in zircon "67122 Ma for the Quartz diorite\ granulite and amphibolites from Barrolower intercept# Alto Ma_cÐultrama_c ComplexUÐPb multigrains in monazite "67427 Ma# CordieriteÐsillimanite gneiss from Juscela¼ndia

volcanosedimentary sequencePbÐPb in rutile "528 Ma# Pegmatitic gabbro from Serra da Malacacheta


Table 0*continued[


VIII*Development of peralluminous syncollisional granites "799 to 599 Ma#

Pimentel et al[ "0881#683209 Ma for the upper intercept of UÐPb Marata� Gneiss Lithodememultigrains fractionca[ 1\999 Ma SmÐNd model ages for the gneiss with Age of magma generation from crustally residentnegative eNd material of ca[ 1\999 Ma

IX*Emplacement of late!tectonic granites "549 to 499 Ma#

Pimentel "0889#^ Pimentel and Fuck "0881# Granite intrusions "Rio Caiapo� \ Serra Negra and Ipora�#UÐPb multigrains fraction in the Areno�polis\ Ipora� and Jaupaci volcanoÐsedimentary489Ð374 Ma for the upper intercept sequences[ Alkalic granites related to late tectonic K1O!

rich magmas

Moura and Gaudette "0882#Single zircon Pb!evaporation Granite intrusions in metasedimentary Estrondo544213 Ma for Santa Luzia Granite Group and in transcurrent Transbrasiliano lineamentsBarradas et al[ "0881#RbÐSr total rock samples554201 Ma for Santa Luzia Granite409204 Ma for Matancža Granite Minimum age of magmatism

X*Development of Transbrasiliano Lineaments "549 to 499 Ma#

Lafon et al[ "0883# Sul_des from gold!bearing quartz veins emplaced inPb!evaporation in galenas the transcurrent shear zones441¦48:−41 Ma for the lower intercept and Ages of galena crystallization is gave by lower intercept^1098¦63:−79 Ma for the upper intercept the upper intercept points to the Pb source

XI*Development of the foreland basin "679 to 449 Ma#

PbÐPb in galena Age of sedimentation of pseudo!oolitic mineralizedCassedane et al[ "0861# Bambu(� Carbonates from Faz[ Tra(�ras "MG#675229 Ma

Age of deformation and mineralition in the VazanteCassedane and Lasserre "0858#Mine "Bambu(� Carbonates#639239 Ma


Table 0*continued[


Amaral and Kawashita "0856#569219 Ma for isochron age in total rock samples Bambui carbonates and shales near Sa½o Francisco city

"MG#599249 Ma for isochron age in total rock samples Minimum age for sedimentationThomaz Filho and Lima "0870# Age of metamorphic!deformational process in459239 Ma for isochron age in thin fraction samples intercalated shales and carbonates from Sete Lagoas Fm[

"Vazante\ MG#

Babinski et al[ "0882#PbÐPb in carbonate rocks Age of sedimentation and metamorphism7612189 Ma Deformed Bambu(� Carbonates575258 Ma Undeformed Sete Lagoas Fm[ carbonates^ minimum

age of sedimentation419242 Ma Undeformed Sete Lagoas Fm[ carbonates^ mobilization

of ~uids from the older foreland basin basement throughfaults

This rock intrudes the Malacacheta Sequence\ the upper part of the Barro Alto layered ma_c!ultrama_c complex[ In the same way\ Suita et al[ "0883a\ 0883b# have dated a garnet!cordierite!biotite!sillimanite!quartz gneiss from a tectonic sliver within the basal part of the Barro AltoComplex and found an upper intercept of 015628 Ma[ These results agree with the divergentregime known to occur in the Amazonian plate "Dall|Agnol et al[\ 0876\ 0883#[ Nevertheless thepetrotectonic nature of the Juscela¼ndia volcano!sedimentary sequence is not fully understood\ itsnorthern volcano!sedimentary sequences counterparts "Coitezeiro and Palmeiro�polis#\ locatedwest of the Niquela¼ndia and Canabrava layered complexes\ have petrochemical characteristicsthat corroborate such a divergent tectonic regime[ Brod and Jost "0878\ 0880# have shown abimodal volcanism with alkaline a.nity\ as yet as alkaline granitic intrusions on the westernborder of the Niquela¼ndia Layered Complex^ Brod and Jost "0878\ 0880# have also distinguishedsome ma_c intrusive bodies in the granitic!gneissic basement of the Coitezeiro volcano!sedimentarysequence\ that are chemically di}erent from Niquela¼ndia layered complex[ Arau� jo "0875# found atholeiitic chemical a.nity in the basic volcanism of the Palmeiro�polis volcano!sedimentarysequence and regarded its ZnÐCuÐPb deposits to belong to a mid!ocean ridge setting[ The operationof a divergent regime in the upper Mesoproterozoic of the TSP seems probable[

2[ TSP Neoproterozoic structural framework

The main tectonic feature of the TSP is a strong gravimetric anomaly "Hasui and Haralyi\ 0874#clearly de_ned for 20699 km long^ it is seen to juxtapose high density rocks to the west over lowdensity metasedimentary rocks to the east\ in order to develop a strong Bouguer gravity gradient


greater than 69 mgals "Fig[ 0#[ This linear gravimetric feature is related to an ophiolitic me�langepetrotectonic association "Strieder and Nilson\ 0881a#\ making up integral part of a large\ regionallyextended nappe structure "D1#\ named Abadia¼nia Nappe by Strieder and Nilson "0882a#[ TheAbadia¼nia Nappe lithologies and structures may be regionally correlated and are delimitated bythe Bras(�lia Main thrust fault "the ~oor thrust# and the Serra Dourada breaching fault "the possibleroot thrust#[ These elements led to the de_nition of the Abadia¼nia Nappe Thrust Sheet "ANTS#\ acharacteristic tectono!stratigraphic terrane of Central Brazil "Fig[ 0 and 3#[ The ANTS and thelinear gravimetric anomaly are interpreted as the TSP suture zone[

The ANTS internally ordered {{pseudo!stratigraphy|| was developed during a penetrative mylon!itic episode "D0^ Strieder and Nilson\ 0883#[ The {{pseudo!stratigraphic|| sequence is composed bya "0# gneissi_ed granite unit "Padre Souza Gneiss Suite#\ "1# gneissi_ed subvolcanic!micrograniteunit "Marata� Lithodeme#\ "2# di}erentiated ma_c!ultrama_c bodies granulitized prior theiremplacement in the nappe structure "Brumado Gneiss Suite#\ and the "3# Abadia¼nia Supersuite"Araxa� metasedimentary suite and a Tectonic Block fragments suite#\ which is the ophioliticme�lange[

The Araxa� metasedimentary suite is made up by a transitional sequence of quartzites\ muscovitequartzites\ graphite!muscovite!quartz schist\ garnetÐmicaÐquartz schists\ and stauroliteÐgarnetÐmicaÐquartz schist[ The tectonic block fragments were strongly deformed since D0\ and do notshow any pre!D0 deformational structure^ then\ they are believed to be tectonically emplaced inthe Araxa� metasedimentary Suite during D0 mylonitic event[ The characteristics of the Araxa�metasediments and their association with strong linear gravimetric anomalies suggest subductiontrough deposits[ The gneissi_ed granites "Padre Souza Suite and Marata� Lithodeme# are per!aluminous and show a.nity to sin!collisional granites "Strieder\ 0882b#^ they were also deformedfrom D0 deformational phase onward[

Fig[ 3[ Actual cross!section through the Tocantins Structural Province as indicated in Fig[ 2 "A!B!C# to illustrate themain structures discussed in the text[ The horizontal scale is the same as that of Fig[ 2[ The vertical scale is about 3times the horizontal scale\ but some geological units and structures are exaggerated to put them in evidence[


The Tectonic Block Fragments suite is composed by microgabbros "epidote!amphibole schistsblocks#\ serpentinites and their Mg!rich schists in the contact aureole "serpentinite blocks# andbiotite!muscovite!carbonate schist "marble blocks#[ The serpentinite blocks are less than 4[9 kmlong and are invariably metasomatized at their contacts with the country Araxa� metasediments"Strieder and Nilson\ 0881b#^ they have lens!like pods "1[9 m long\ 9[4 m thick# of typical Al!richpodiform chromitite "Strieder and Nilson\ 0881c#[ The epidote!amphibole schist blocks are larger"³09Ð01 km long# and preserve some deformational pods\ where the original texture may berecognised "Strieder and Nilson\ 0881d#[ The marble blocks were interpreted\ based on theirdiscrepant sedimentary characteristics\ as exotic fragments "Strieder\ 0878\ 0882b^ Strieder andNilson\ 0881a#[ Further examination recognised structural and sedimentary features that enabletheir correlation with the lower Paranoa� metasediments thrust sheet "Roscoe and Arau� jo Filho\0883#[

The geometry of tectonic structures important for elucidating the TSP evolution was detectedin the lineament analysis of LANDSAT images "Strieder\ 0882b^ Strieder and Nilson\ 0882b#[Besides the thrust surfaces\ structural lineament in~ections were identi_ed "Fig[ 1# and they areuseful as kinematic indicators of thrust sheet displacement direction\ as well as to quantify thethrust displacement itself "Coward and Potts\ 0872#[ The structural in~ections show the samedisplacement direction "S69Ð79E#\ which is at high angles to the main thrust faults and suture zonelinear gravimetric anomaly[ The collisional process\ then\ must had been of frontal type\ insteadof oblique as suggested by Hasui and Haralyi "0874#[ These structural features do not favorsuggested crustal block thrusting and rotation[

The largest structural in~ection lies along the 04>29?S parallel\ west of Bras(�lia\ is named PirineusMegain~ection "PMI# and extend for at least 149 km "Strieder\ 0882b#[ Around the western edgeof Bras(�lia\ the ANTS is eroded in the Bras(�lia Tectonic Syntaxis "Strieder and Nilson\ 0882b#\which shows 89 km of minimum displacement of ANTS over the lower Paranoa� metasedimentsthrust sheet "Fig[ 0#[ The PMI di}erential movement is accommodated by a series of transcurrentfaults that crosscut the recumbent fold forming the ANTS[ In the north side\ the transcurrentfaults are WSW oriented and show dextral movements\ while the southern transcurrent faults areESE oriented and have a sinistral sense of movement "Strieder\ 0889\ 0882b#[ The PMI is associatedwith a large re!entrance of linear gravimetric anomaly of the suture[ The sur_cial structural recordfor this re!entrance is just observed in the ANTS "PMI# and in the upper thrust sheets\ as one cansee in the south border of Barro Alto layered ma_c!ultrama_c complex[ This means that the lineargravimetric anomaly reentrance is a feature superposed on the upper thermally softened crustalplate and\ then\ has been interpreted as a result of a rigid wedge indenter related to the border ofthe underthrusting Sa½o Francisco plate "Strieder and Nilson\ 0881a#[

The lineament analysis has shown some breaching faults in the central part of Bras(�lia Sub!province "Strieder and Nilson\ 0882a\ 0882b#[ For example\ the Chapada das Covas breachingfault "Strieder\ 0882b# cut across both the lower Paranoa� metasediments thrust sheet and upperANTS dividing them into two blocks "Fig[ 2#^ the western block is thrusted over the eastern "Fig[3#[ Strieder "0882b# attributed the onset of the Chapada das Covas breaching fault to the wedgeindentation of the underthrusting Sa½o Francisco plate[ Another possible breaching fault may bethe Serra Dourada thrust "Fig[ 2#[ It is located to the west and delimitates the ANTS exposure[ AtSerra Dourada\ the recumbent fold on Araxa� metasediments is deformed into an open synformalfold at the footwall of the thrust fault "Strieder\ 0882b^ Strieder and Nilson\ 0882a\ 0882b#[ The


upper thrust sheet at Serra Dourada consists of tonalitic gneisses of the Goia�s Greenstone Belt"Fig[ 3#[

Toward the south\ the linear gravimetric anomaly is continuous and contours the Cunha deGuaxupe� "Hasui et al[\ 0889#[ The ESE in~ection of the linear gravimetric anomaly in the Cunhade Guaxupe� is related to the Serra da Canastra In~ection[ The Serra da Canastra in~ection is anarrow tectonic syntaxis "Strieder and Nilson\ 0882b# and its lineaments show physical con!tinuation toward the north margin of Cunha de Guaxupe�[ This means that some lithotectonicunits of the ANTS may be correlated with those occurring in the Cunha de Guaxupe�\ such as Sa½oJoa½o del Rei and Andrela¼ndia metasediments[ Roig and Schrank "0881# interpreted theAndrela¼ndia metasediments as an ophiolitic melange\ which is in good accordance with the resultsobtained by Strieder and Nilson "0881a# for Araxa� metasediments[

The Cunha de Guaxupe� lithotectonic units are thrust toward the east "Vasconcellos\ 0877# andthis is veri_ed by the linear gravimetric gradient of the suture zone[ Thus\ the Cunha de Guaxupe�is regarded as a tectonic wedge connected to the upper thermally softened continental crustundergoing overthrusting[ Nevertheless the Cunha de Guaxupe� is not a rigid indenter\ its laterallimbs show transcurrent faults superposed on the thrust faults "Wernick et al[\ 0868^ Hasui et al[\0889^ Ebert et al[\ 0882#[ These faults accommodate the _nal stages di}erential movements on theCunha de Guaxupe�[ The overthrust of a thermally softened continental wedge give rise to a tectonicantitaxis "Strieder and Nilson\ 0881a#\ since its con_guration is opposed to that developed at PMI[

3[ Geochronological constraints on the TSP Brasiliano Orogenic Cycle

The kinematic evolution of the TSP can be described into stages constrained by recent geo!chronological and structural data "Fig[ 4#[ The oldest Neoproterozoic age clearly related to theBrasiliano Orogenic Cycle in the TSP was obtained by Pimentel et al[ "0880b# and by Pimenteland Fuck "0881# in the Bom Jardim de Goia�s region "western Goia�s#[ They dated a granite!gneissunit through UÐPb and SmÐNd methods and found ages of ca[ 839Ð784 Ma for its mantlederivation[ The associated volcano!sedimentary sequences were also dated at ca[ 829Ð659 Ma[ Thecomposition of these units display chemical a.nity with juvenile magmatic arcs^ the granite!gneisses are calc!alkaline rocks "I!type# and the volcanics vary from low!K1O basalts to high!K1Orhyolites "Pimentel and Fuck\ 0881#[ In reality\ this _nding was the _rst record of ensimaticmagmatism conclusively related to the Neoproterozoic evolution of the TSP "Pimentel and Fuck\0881#[

To the north\ the Mara Rosa volcano!sedimentary sequence and its plutonic counterparts wereonce correlated with the Pilar de Goia�s greenstone belt sequence "Danni and Ribeiro\ 0867#[However\ recent precise geochronological data has revealed their Neoproterozoic origin "Pimentelet al[\ 0882a\ 0882b^ Viana and Pimentel\ 0883#[ The geochemical features of the volcanic "Kuyumj!ian\ 0878# and plutonic rocks "Viana and Pimentel\ 0883# were regarded to calc!akaline magmasof island!arc tectonic settings[ The SmÐNd isotopic ratios con_rm the island!arc setting\ becausethe positive eNd indicates primitive magmas "Viana and Pimentel\ 0883#[ The tonalitic gneisses inthe Mara Rosa region were dated 745 Ma\ while the metavolcanic rocks gave an age of 75127 Ma"UÐPb single zircon method\ Pimentel et al[\ 0882a\ 0882b\ Table 0#[ The model age obtained forthe tonalitic gneisses\ metavolcanics and intrusive subvolcanic rocks is 0[9 Ga "Viana and Pimentel\


Fig[ 4[ Kinematic evolution of the Tocantins Structural Province "TSP#[ The sequence of block diagrams shows thetectonic stages and structures discussed in the text[ See text for additional discussion[ "A# Initial conditions of Goia�sOcean subduction[ "B# Initial collisional structure of the Amazonian and Sa½o Francisco continental plates[

0883#[ These data con_rm the existence of a Neoproterozoic ocean in Central Brazil during theNeoproterozoic ðFig[ 4"a#Ł and seem\ to date\ to constrain the beginning of the subduction processto ca[ 839 Ma "Table 0#[

The _nal closure of the intervening ocean between the Amazonian and Sa½o Francisco continentalcrusts\ however\ was not yet well constrained ðFig[ 4"b#Ł[ Pimentel et al[ "0881# dated the Marata�Lithodeme as 683209 Ma^ since this peraluminous gneissic granite is deformed from the ANTS

organization onward\ it seems to indicate that the continental collision in the TSP took placearound 799 Ma[ The time span between the onset of subduction and the continental collision mayseem to be large[ But\ the 799 Ma for the continental collision agrees with the expected time of theindentation process at PMI "Strieder\ 0882b# and the granulite facies metamorphism of the greatma_c!ultrama_c layered complexes in Central Goia�s "689Ð669 Ma] Ferreira Filho et al[\ 0883^Suita et al[\ 0883a\ 0883b#[

Considering the 799 Ma continental collision in the TSP\ it is interesting to observe that I!typeto A!type granitic intrusions that intrude earlier Neoproterozoic granite!gneisses "ca[ 849Ð784 Ma\Pimentel and Fuck\ 0881# are younger than Marata� Lithodeme^ their age spread from 549 Ma to449 Ma "Table 0#[ These granitic intrusions are also located in the older overthrust terranes thatseparate the ParaguaiÐAraguaia and Bras(�lia subprovinces "Goia�s median massif# and have beeninterpreted as late! to post!tectonic ones "Pimentel and Fuck\ 0881#[ Some of these intrusions are


Fig[ 4 continued[ "C# Collisional duplication of the Amazonian plate by breaching faults^ this stage was developed duringthe _nal penetration of the rigid indenter of the Sa½o Francisco plate and ampli_ed the ~exural movements in the forelandsedimentary basin[ "D# Final collisional structure of the TSP^ the back!thrust faults cut o} the transcurrent faults ofTransbrasiliano lineaments and ampli_ed vertical movements on the hinterland sedimentary basin[

related to large transcurrent faults developed as consequence of indentation process in the PMI

"Gottardo\ 0885#[During the collisional stage\ a shallow water sedimentary basin developed just over the linear

gravimetric low "Fig[ 0#[ It is mainly composed by quartzites\ pelites\ and platformal carbonateswith algal mats and stromatolites[ These sedimentary rocks were deformed during thrusting andmetamorphosed to a low grade facies "Fig[ 3#[ The thrust displacement is directed toward the ESEand decreases in intensity in the same direction\ so that one can yet _nd undeformed horizontalstrata covering the older Sa½o Francisco plate geological units away from the suture zone[ Thissedimentary basin and its geological units were interpreted as a foreland basin "Kiang et al[\ 0877#\or as a foreland fold and thrust belt "Pimentel et al[\ 0881#[ The Pb!Pb ages from the carbonate


unit galena|s "Amaral\ 0857^ Cassedane et al[\ 0861^ Babinski et al[\ 0882# and Rb:Sr from peliteunits "Amaral and Kawashita\ 0856^ Thomaz Filho and Lima\ 0870# spread from ca[ 679 Ma toca[ 449 Ma "Table 0#[ The age data range for the foreland basin seems to constrain its onset to theclosure of the intervening ocean and the beginning continental collision at the TSP "ca[ 683 Ma[for Marata� Lithodeme#[ The age span for the foreland basin development is also indicated by thelate! to post!tectonic granitic intrusions into the overriding plate "Table 0#[ The geochronologicaldata also indicate that sedimentational and deformational episodes took place in the same timespan in this foreland sedimentary basin[

4[ Integrated discussion on the TSP tectonic evolution

The details of geological\ petrochemical and geochronological data on the TSP lithotectonicunits is rapidly increasing[ However\ there are some important gaps\ specially relating to structuralinformation[ Much has been written about local geological units in the TSP and the importanceof the Brasiliano Tectonic Cycle in the structural reorganization of older lithotectonic terranes hasincreased[ Thus\ it seems appropriate to present an overall tectonic framework of the TSP[

The main question regarded to the onset of the Brasiliano Tectonic Cycle concerns to the ageof the opening of the Goia�s Ocean[ The most voluminous data that indicate an extensional regimein Central Brazil have been obtained from the large ma_c!ultrama_c complexes and granites andrhyolites of anorogenic!type dated as ca[ 0699 Ma "Pimentel et al[\ 0880a^ Suita et al[\ 0883a\0883b#[ However\ due to the scarcity of geochronologic data indicative of metamorphic!defor!mational episodes in the time span between 0699 and 0999 Ma\ and due to the improbable existenceof the ocean over such a long time\ it seems that\ at least in this part of the older continental crust\the 0699 Ma anorogenic episode did not culminate in ocean opening[

The 0179Ð0156 Ma ages obtained for a pegmatitic hornblende grabbro in the Barro Alto LayeredMa_c!ultrama_c Complex and for a garnet!cordierite!biotite!sillimanite!quartz gneiss slivers inthe Juscela¼ndia Volcanosedimentary Sequence "Suita et al[\ 0883a\ 0883b# seem to point to ayounger extensional episode\ as recorded by the petrochemical features of the others volcano!sedimentary sequences "Arau� jo\ 0875^ Brod and Jost\ 0878\ 0880#[ More data are clearly needed\but the present results help in selecting the adequate lithological units in order to solve the problem[To date\ it seems adequate to characterize an upper Mesoproterozoic magmatic event during anextensional regime\ that culminate with the opening of the Goia�s Ocean in the TSP[ The presentgeochronological data\ then\ show a time span of 149Ð299 Ma from the onset of ocean opening tothe _rst records of ocean subduction[ The 0999 Ma age for the beginning of the subduction in theTSP\ therefore\ must be taken as a minimum\ since the complete ocean consumption and long!lived collisional episode may have obliterated a part of the geological records[

The recent geochronological\ structural and geochemical data regarded to the Neoproterozoicshow that the Brasiliano Orogenic Cycle must be understood in a di}erent way[ The recognizedensimatic units "Pimentel and Fuck\ 0881^ Viana and Pimentel\ 0883# put an end point in thepurely ensialic assumptions for the development of the TSP[ At the same time\ the model ages forthe Marata� Lithodeme "638209 Ma magmatism derived from 1[9 Ga crustal material\ Pimentel etal[\ 0881# and its syncollisional peraluminous a.liation "Strieder\ 0882b#\ and granulite meta!morphism of the ma_c!ultrama_c complexes "Suita et al[\ 0883a\ 0883b# point to an important


collisional episode in the TSP[ The dismembered ophiolitic blocks in the Araxa� metasedimentsrepresent arc!derived units "Strieder and Nilson\ 0881a^ Strieder et al[\ 0883#[ The Araxa�meta!sediments are then better regarded as accretionary prism\ than a passive margin sedimentarysequence as interpreted by Hasui et al[ "0883#[

Thus\ it is possible to distinguish two major tectonic phases in the TSP] 0# the _rst one ischaracterized by island!arc amalgamation with the western Amazonian plate "849Ð799 Ma# ðFig[4"a#Ł\ and 1# the second is characterized by continental lithospheric juxtaposition "799Ð599 Ma#ðFig[ 4"b#Ł[ The Brasiliano Tectonic Cycle in Central Brazil may be constrained to the 849Ð599 Matime span and\ in this way\ it is not Grenville "0[2Ð0[9 Ga#^ to date\ it is possible that\ during theGrenville Orogenic Cycle\ the TSP was subject to rifting episodes "Suita\ 0885#[

It must be remembered\ however\ that the geochronological data are still scarce to allow a cleartectonic picture of the convergence[ The geochronological data\ to date\ are from speci_c geologicalunits at speci_c localities[ The regional correlations are constrained\ because the thrust surfacesare not yet well!de_ned\ neither the restoration of thrust displacements have been tried[ It is\therefore\ hard to propose a tectonic evolution based on temporal and areal parameters[ Takinginto account the geometry of the Amazonian and Sa½o Francisco plates borders in the TSP frontalconvergence\ some degree of tectonic di}erentiation may be envisaged[ It means that one may _nddi}erent ages for island!arc amalgamation and continental collision at di}erent parts of the TSP[It will be important to refer future geochronological data to a clear structural framework in orderto interpret these data in space and time[

An attempt to de_ne the structural framework of the TSP was presented by Strieder "0882b#and Strieder and Nilson "0882b#\ yet this work is still in progress[ The preliminary results presentedby Strieder and Nilson "0882b# are focused on the south part of the Bras(�lia Subprovince\ andshow the location of the thrust faults[ Three important features were distinguished] 0# the di}er!ential thrust displacement structures\ 1# the lowermost boundary thrust "LBT#\ and 2# the breachingfaults[ The di}erential thrust displacement structures indicated the frontal collisional process "Fig[1#[ The LBT makes possible to put apart the autochthonous from the para!autochthonous toalochthonous zones "Figs[ 0 and 2#[ The breaching faults\ on the other hand\ introduce a tectoniccomponent not well understood at this moment] the duplication of the former thrust sheet "Fig[3#[ To date\ it is not clearly known which of the thrusts identi_ed by Strieder and Nilson "0882b#are of breaching type and which are not\ since there is no detailed work on thrust surfaces[Similarly\ there has not been an attempt to restore thrust displacements and to correlate thegeological units in each thrust sheet[

The identi_cation of the Chapada das Covas breaching fault "CCBF# has been mainly based onthe Paranoa� metasediments thrust over the ANTS "Figs[ 2 and 3#[ The development of thisbreaching fault is related with the indentation of the Sa½o Francisco rigid wedge in the PMI

"Strieder\ 0882b#[ Toward the west\ the Serra Dourada breaching fault "SDBF# juxtaposed theGoia�s Greenstone Belt units over the ANTS "Strieder and Nilson\ 0882b#[ Since the SDBF truncatesthe ANTS recumbent fold "F1#\ and since similar geological units "Serra da Mesa and Estrondo!Araguaia metasediments# are present to the northwest over the greenstone belt units\ it may bepossible that some others large breaching faults will be discovered "Figs[ 2 and 3#[

The main clue on TSP breaching faults is provided by the juxtaposition of di}erent geologicalunits in the {{Goia�s median massif|| separating the Bras(�lia from ParaguaiÐAraguaia subprovinces[The structure of {{Goia�s median massif|| plays an important role in the tectonic framework of the


TSP[ It has been suggested that its structure near the PMI was formed as a result of the trappingof small continental plates or magmatic arcs during the convergence of the large continental platessuch as the Amazonian and Sa½o Francisco "Strieder and Nilson\ 0881a#[ Fuck "0883# has followedthis interpretation\ regarding the {{Goia�s median massif|| as a microcontinent trapped between themain plates[ Costa et al[ "0876# suggested a crustal!scale pop!up resulting from an oblique collisionduring the Late Archean[ Later\ Hasui et al[ "0883# suggested Lower Proterozoic frontal collisionsdirected westward "ParaguaiÐAraguaia Subprovince# and eastward "Bras(�lia Subprovince#[ Boththese interpretations consider the {{Goia�s median massif|| as a kind of microcontinent[

It is nowadays realized that a microcontinent must be rimmed by thrust surfaces with ophioliticme�lange\ and by gravity anomalies[ In the {{Goia�s median massif||\ however\ the gravity anomalyis clearly present at its eastern border[ Despite the scarcity of gravity measurements on the westernParaguaiÐAraguaia subprovince\ one can see a slowly decreasing followed by a slowly increasingBouguer gravimetric gradient westward "Hasui and Haralyi\ 0874#[ The gravity structure of thewestern ParaguaiÐAraguaia subprovince is di}erent from the Eastern Bras(�lia subprovince and itsophiolitic me�lange "ANTS#[ The gravity structure of the western ParaguaiÐAraguaia subprovincedoes not support the interpretation of a suture zone[

Studies still in progress by Cunha "0885# and Gottardo "0885# reveal that transcurrent Trans!brasiliano lineaments "Schobbenhaus Filho et al[\ 0864# result from the indentation process atPMI\ and that these lineaments and Neoproterozoic granitic plutons are a}ected by low anglereverse cleavages and faults directed toward the west[ These reverse faults convert several geologicalunits into slices and are interpreted as back!thrusts of the Brasiliano Orogenic Cycle in the TSP

"Cunha\ 0885^ Gottardo\ 0885^ Strieder et al[\ 0886#[The structure of the {{Goia�s median massif||\ on the other hand\ may be seen as a triangular

zone developed by the juxtaposition of di}erent geological units through thrusting and breachingfaults directed toward ESE ðFig[ 4"c#Ł and through back thrusts directed westward ðFig[ 4"d#Ł[Thus\ the {{Goia�s median massif|| is not a microcontinent\ but a collage of Archean greenstonebelts and granite!gneisses\ Meso and Neoproterozoic volcanosedimentary units\ as well as granite!gneisses and ma_c!ultrama_c complexes[ The collage was mainly produced by thrusting duringthe island!arc amalgamation stage\ and by thrusting and breaching during the continental collisionstage[ The thrusting and breaching during the continental collision certainly lead to the constructionof a high Neoproterozoic orogenic cordillera positioned in the {{Goia�s median massif||[

Following the continental collision\ the indentation process in the PMI developed large trans!current faults in the upper thermally softened plate "Strieder et al[\ 0883#[ These transcurrent faultswere named Transbrasiliano lineaments "Schobbenhaus Filho et al[\ 0864#[ The onset of suchtranscurrent faults generated space for the emplacement of calc!alkaline to alkalic type granites\as well as the gold!bearing quartz veins in the shear zones "Gottardo\ 0885#[ The time span ofgranite emplacement in the transcurrent shear zone is between 659 Ma and 449 Ma "Table 0#[

Following the continental collision\ there was also the development of a foreland basin over thedowngoing Sa½o Francisco plate[ The deposition of a series of metasedimentary units\ such asParanoa�\ Paracatu and Bambu(�\ are connected with the migration of the basinal depocenter andthrusting in its inner part[ On the other hand\ the time span recorded for the foreland development"Table 0# is similar to that recorded for the transcurrent shear granitic plutons "659Ð499 Ma#[ Thispoints to a synchronous development during the convergence of the continental plates[

The pilling up order of the foreland basin sediments do not yet consider the thrust e}ects in


inverting stratigraphic sequences\ since no stratigraphic restoration have been tried[ Some resultsare available concerning the basement of the foreland basin[ High resolution seismic pro_lingconducted by PETROBRA� S "Teixeira et al[\ 0882# showed that the downgoing Sa½o Franciscoplate displays rift!like structures in_lled with coarse sediments[ This feature may be interpreted asthe results of the ~exural rigidity of the downgoing plate\ instead of the evolution in a passiverifted margin of the Sa½o Francisco plate as interpreted by Dominguez "0882#^ Braun et al[ "0882#and Martins et al[ "0882#[ Considering the high displacements measured for the thrust faults"149 km\ Strieder and Nilson\ 0882b#\ the rifted Sa½o Francisco margin must have been subductedand its structures destroyed during the convergent deformation[

The foreland basin may also be divided into two segments according the results obtained fromthe lineaments| studies of Strieder and Nilson "0882b#[ The identi_cation of the Lower BoundaryThrust "LBT# does permit to distinguish the 0# autochthonous zone and the 1# para!autochthonousto alochthonous zone[ The _rst one is made up by nearly horizontal low grade to non meta!morphosed strata[ The second one\ on the other hand\ is made up by deformed and low grademetamorphosed strata[ The intensity of metamorphism\ deformation and thrust displacementdecreases eastward[

Acknowledgements

The authors thank Prof[ Joa½o Felipe C[L[ da Costa "DEMINÐUFRGS#\ Prof[ Farid ChemaleJr[ and Prof[ Le�o A[ Hartmann "IGÐUFRGS# for revision and comments about the text[ Theauthors thank the referees for improving this paper[ We also thank to Doctoral Candidate\Evandro Gottardo\ for helping with _gures[ AJS thanks to Brazilian Research Council "CNPq#for research grant[

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Hasui\ Y[\ Haralyi\ N[L[E[\ 0874[ A mega!estruturacža½o de Goia�s[ In] Simp[ Geol[ Centro!oeste\ II\ SBG:CO!BS\ Goia¼nia"GO#\ Ata[[[[\ pp[ 019Ð033[

Hasui\ Y[\ Costa\ J[B[S[\ 0889[ O Cintura½o Araguaia] um novo enfoque estrutural!estratigra�_co[ In] Congr[ Bras[Geologia\ 25\ Natal "RN#\ SBG:NE\ Anais[[[\ Vol[ 4\ pp[ 1424Ð1438[

Hasui\ Y[\ Costa\ J[B[S[\ Ebert\ H[D[\ 0889[ Estruturacža½o da extremidade oriental da chamada Cunha Guaxupe�] dadospreliminares[ In] Congr[ Bras[ Geologia\ 25\ Natal "RN#\ SBG:NE\ Anais[[[\ Vol[ 4\ pp[ 1185Ð1297[

Hasui\ Y[\ Costa\ J[B[S[\ Haralyi\ N[L[E[\ 0883[ Estrutura em quilha Brasil Central] uma feicža½o fundamental na geologiade Goia�s e Tocantins[ Geocie¼ncias "USP#\ Sa½o Paulo "SP#\ Vol[ 02\ pp[ 352Ð386[

Kiang\ C[H[\ Miranda\ F[P[\ Magalha½es\ L[\ Alkimin\ F[F[\ 0877[ Consideracžo½es sobre a evolucža½o tecto¼nica da Baciado Sa½o Francisco[ In] Congr[ Bras[ de Geologia\ 24\ Bele�m "PA#\ SBG:NO\ Anais[[[\ Vol[ 4\ pp[ 1965Ð1989[

Kuyumjian\ R[M[\ 0878[ Geoqu(�mica e o signi_cado do posicionamento geotecto¼nico das rochas pluto¼nicas da regia½ode Chapada\ Goia�s\ Brasil[ In] Congr[ Bras[ Geoqu(�mica\ 1\ Rio de Janeiro "RJ#\ SBGq\ Anais[[[\ pp[ 084Ð190[

Lafon\ J[M[\ Kotschoubey\ B[\ Barradas\ J[A[S[\ 0883[ RbÐSr and PbÐPb dating of the proterozoic igneous rocks andassociated gold mineralization in the Monte do Carmo region\ state of Tocantins\ Brazil[ In] Ages and Isotopes ofSouth American Ores Symposium\ IGCP\ Project 231\ Chile\ 4 p[

Lesquer\ A[\ Almeida\ F[F[M[\ Davino\ A[\ Lachaud\ J[C[\ Maillard\ P[\ 0870[ Signi_cation structurale des anomaliesgravime�triques de la partie Sud du Craton de Sa½o Francisco "Bre�sil#[ Tectonophysics 65\ 162Ð182[

Marini\ O[J[\ Fuck\ R[A[\ Danni\ J[C[M[\ Dardenne\ M[A[\ Logue�rcio\ S[O[C[\ Ramalho\ R[\ 0873[ As faixas dedobramentos Bras(�lia\ Uruacžu� e ParaguaiÐAraguaia e o Macicžo Mediano de Goia�s[ In] Schobbenhaus\ C[\ Campos\D[A[\ Derze\ G[R[\ Asmus\ H[E[ coords[\ Geologia do Brasil\ Public[ Esp[ DNPM\ p[ 490\ 0 Mapa Geol[ 0]1[499[999[

Marini\ O[J[\ Botelho\ N[F[\ 0875[ A prov(�ncia de granitos estan(�feros de Goia�s[ Rev[ Bras[ Geoc[ 05 "0#\ 008Ð020[Martins\ M[\ Teixeira\ L[B[\ Braun\ O[P[G[\ 0882[ Consideracžo½es sobre a estratigra_a da Bacia do Sa½o Francisco com

base em dados de subsuperf(�cie[ In] Simp[ sobre o Cra�ton do Sa½o Francisco\ 1\ Salvador "BA#\ SBG:BA e SGM:BA\Anais[[[\ pp[ 056Ð058[

Moura\ C[A[V[\ Gaudette\ H[E[\ 0882[ Evidence of Brasiliano:Panafrican deformation in the Araguaia Belt] implicationfor Gondwana Evolution[ Rev[ Bras[ Geoc[ 12 "1#\ 006Ð012[

Nilson\ A[A[\ Botelho\ N[F[\ Ferreira Filho\ C[F[\ 0883[ Rifteamento crustal Meso!proterozo� ico no centro!norte deGoia�s[ In] Congr[ Bras[ de Geol[\ 27\ Balnea�rio de Camboriu� "SC#\ SBG:SC\ Anais[[[\ Vol[ 0\ pp[ 147Ð148[

Pimentel\ M[M[\ 0889[ Late Proterozoic crustal evolution of the Tocantins Province in Central Brazil] an isotopic andgeochemistry study[ Ph[D[ Thesis\ Oxford\ England\ Oxford University\ p[ 137[

Pimentel\ M[M[\ Heaman\ L[\ Fuck\ R[A[\ Marini\ O[J[\ 0880[ UÐPb zircon geochronology of Precambrian tin!bearingcontinental!type acid magmatism in central Brazil[ Precambrian Research 41\ 210Ð224[

Pimentel\ M[M[\ Heaman\ L[\ Fuck\ R[A[\ 0880[ Zircon and sphene UÐPb geochronology of upper proterozoicvolcanic!arc rock units from southwestern Goia�s\ Central Brazil[ Journal of South America Earth Science 3 "3#\184Ð294[

Pimentel\ M[M[\ Fuck\ R[A[\ 0881[ Neoproterozoic crustal accretion in central Brazil[ Geology 19\ 264Ð268[Pimentel\ M[M[\ Heaman\ L[\ Fuck\ R[A[\ 0881[ Idade do meta!riolito da Sequ�e¼ncia Marata�\ Grupo Araxa�\ Goia�s]

estudo geocronolo�gico pelos me�todos UÐPb em zirca½o\ RbÐSr e SmÐNd[ An[ Acad[ Bras[ Ci[ 53 "0#\ 08Ð17[Pimentel\ M[M[\ Fuck\ R A[\ Machado\ N[\ Fuck\ R[F[\ Ribeiro\ R[K[\ Viana\ M[G[\ 0882a[ Dados geocronolo�gicos

UÐPb preliminares da regia½o de Mara Rosa "Goia�s#] implicacžo½es para a e�poca de mineralizacža½o de Au e para aevolucža½o tecto¼nica Neoproterozo� ica no Centro!oeste[ In] Congr[ Bras[ Geoqu(�mica\ 3\ Bras(�lia "DF#\ SBG:DF\ Res[Expandidos\ pp[ 144Ð147[

Pimentel\ M[M[\ Rodrigues\ J[B[\ Fuck\ R[A[\ Machado\ N[\ 0882b[ Idade UÐPb em zirco½es do metarriolito da Sequ�e¼nciaVulcano!sedimentar de Ipora�\ oeste de Goia�s[ In] Congr[ Bras[ Geoqu(�mica\ 3\ Bras(�lia "DF#\ SBG:DF\ Res[ Expand!idos\ pp[ 148Ð150[

Roig\ H[L[\ Schrank\ A[\ 0881[ Caracterizacža½o da zona de sutura Jacu(�!Conceicža½o da Aparecida\ limite norte do


complexo de nappes de Guaxupe� "MG#[ In] Congr[ Bras[ Geol[\ 26\ Sa½o Paulo "SP#\ 0881\ SBG!SP\ Bol[ Res[ Exp[[[\Vol[ 0\ pp[ 172Ð174[

Roscoe\ J[S[\ Arau� jo Filho\ J[O[\ 0883[ Estudo estrutural preliminar do front de empurra½o do Araxa� sobre o Paranoa�na porcža½o oriental da Megain~exa½o dos Pirineus\ Goia�s Central[ In] Simp[ Reg[ Geol[ Centro!oeste\ 3\ Bras(�lia "DF#\SBG:BS!CO\ Anais[[[\ pp[ 066Ð079[

Schobbenhaus Filho\ C[\ Ribeiro\ C[L[\ Oliva\ L[A[\ Takanohashi\ J[T[\ Lindenmayer\ A[G[\ Vasconcelos\ J[C[\ OrlandiFilho\ V[\ 0864[ Folha Goia�s "SD 11#[ In] Schobbenhaus Filho C[\ coord[\ Carta Geolo�gica do Brasil ao Milione�simo\Bras(�lia\ DNPM\ pp[ 04Ð73\ 88Ð002\ 0 mapa[

Schobbenhaus Filho\ C[\ Campos\ D[A[\ Derze\ G[R[\ Asmus\ H[E[\ 0873[ Geologia do Brasil] testo explicativo doMapa Geolo�gico do Brasil e da a�rea ocea¼nica adjacente incluindo depo�sitos minerais "0]1499999#[ DNPM\ Bras(�lia"DF#\ 490 p[

Strieder\ A[J[\ 0878[ Geologia\ Petrologia e Tecto¼nica dos Corpos de Serpentinito e Rochas Encaixantes\ Abadia¼nia"GO#[ Dissertacža½o de Mestrado "IGeoÐUnB#\ Bras(�lia "DF#\ 197 p[ "ine�dito#[

Strieder\ A[J[\ 0889[ Ana�lise estrutural na regia½o de Abadia¼nia "GO#[ Rev[ Bras[ de Geoc[ 19 "0!3#\ 128Ð146[Strieder\ A[J[\ 0882a[ Tecto¼nica colisional no Brasil Central] evolucža½o e implicacžo½es no padra½o estrutural[ In] Simp[

Nac[ Est[ Tecto¼nicos\ 3\ Belo Horizonte\ 0882\ Anais[[[ Belo Horizonte\ SBG:MG\ pp[ 186Ð290[Strieder\ A[J[\ 0882b[ Deformacža½o e metamor_smo na regia½o de Santa Cruz de Goia�sÐCorrelacža½o tectono!estratigra�_ca

e evolucža½o tecto¼nica regional[ Tese de Doutoramento "IGeo!UnB#\ Bras(�lia "DF#\ p[ 147[ "ine�dito#[Strieder\ A[J[\ Nilson\ A[A[\ 0881a[ Melange o_ol(�tica nos metassedimentos Araxa� de Abadia¼nia "GO# e implicacžo½es

tecto¼nicas regionais[ Rev[ Bras[ Geoc[ 11 "1#\ 193Ð104[Strieder\ A[J[\ Nilson\ A[A[\ 0881b[ Estudo petrolo�gico de alguns fragmentos tecto¼nicos da melange o_ol(�tica em

Abadia¼nia "GO#] I*o protolito dos corpos de serpentinito[ Rev[ Bras[ Geoc[ 11 "2#\ 227Ð241[Strieder\ A[J[\ Nilson\ A[A[\ 0881c[ Estudo petrolo�gico[[[] II*as cromitas prima�rias e as suas transformacžo½es

metamo�r_cas[ Rev[ Bras[ Geoc[ 11 "2#\ 242Ð251[Strieder\ A[J[\ Nilson\ A[A[\ 0881d[ Estudo petrolo�gico[[[] III*texturas e composicža½o qu(�mica dos corpos ma�_cos[ Rev[

Bras[ Geoc[ 11 "2#\ 252Ð260[Strieder\ A[J[\ Nilson\ A[A[\ 0882a[ Abadia¼nia nappe emplacement and dispersion] some constraints on the evolution

of Central Brazil[ In] Simp[ sobre o Cra�ton do Sa½o Francisco\ 1\ Salvador\ 0882\ Bol[ Res[ Exp[\ Salvador\ SBG:BA\pp[ 166Ð168[

Strieder\ A[J[\ Nilson\ A[A[\ 0882b[ Ana�lise preliminar de lineamentos na Prov(�ncia Estrutural do Tocantins[ In] Simp[Nac[ Est[ Tecto¼nicos\ 3\ Belo Horizonte\ 0882\ Anais[[[ Belo Horizonte\ SBG:MG\ pp[ 161Ð165[

Strieder\ A[J[\ Nilson\ A[A[\ 0883[ Estratigra_a de terrenos precambrianos] o exemplo da La¼mina de Cavalgamento daNappe de Abadia¼nia[ In] Congr[ Bras[ de Geol[\ 27\ Baln[ Camboriu� "SC#\ SBG:SC\ 0883\ Bol[ Res[ Exp[\ Vol[ 2\ pp[146Ð147[

Strieder\ A[J[\ Cunha\ F[S[S[\ Gottardo\ E[\ 0886[ O registro e o signi_cado tecto¼nico de estruturas back thrust naProvincia Estrutural do Tocantins[ In] Simpo�sio Nacional de Estudos Tecto¼nicos\ Pireno�polis "GO#\ SBG!DF\ 0886\Bol[ Resumos Expandidos\ p[ 6Ð8[

Strieder\ A[J[\ Gottardo\ E[\ Cunha\ F[S[S[\ Binotto\ R[B[\ Mesquita\ M[J[M[\ 0883[ O signi_cado tecto¼nico dosLineamentos Transbrasilianos no processo colisional Neoproterozo� ico da Prov(�ncia Estrutural do Tocantins[ In]Congr[ Bras[ de Geol[\ 27\ Baln[ Camboriu� "SC#\ SBG:SC\ 0883\ Bol[ Res[ Exp[\ Vol[ 0\ pp[ 032Ð034[

Suita\ M[T[F[\ 0885[ Metalogenia e Geoqu(�mica de Platino� ides em Alguns Complexos Ma�_co!ultrama�_cos no Brasil]alguns crite�rios e guias com e¼nfase no Complexo Ma�_co!ultrama�_co de Barro Alto[ Unpublished Thesis\ UniversidadeFederal do Rio Grande do Sul "IG!UFRGS#\ Porto Alegre "RS!Brasil#[

Suita\ M[T[F[\ Chemale Jr[\ F[\ 0884[ Nature of the Uruacžuano Cycle in the Sa½o Francisco and Tocantins Provincesand its relations with the Amazonian Craton[ In] Simpo�sio Nacional de Estudos Tecto¼nicos\ 4\ Gramado "RS#\Extended Abstracts\ SBG!RS\ p[ 87Ð099[

Suita\ M[T[F[\ Kamo\ S[L[\ Krogh\ T[\ Fyfe\ W[S[\ Hartmann\ L[A[\ 0883a[ U:Pb ages from the high!grade Barro AltoMa_c!ultrama_c Complex "Goia�s\ Central Brazil#] Middle Proterozoic Continental Ma_c Magmatism and UpperProterozoic Continental Collision[ In] Lanphere\ M[A[\ Dalrymple\ G[B[\ Turrin\ B[D[ "Eds[#\ Abstracts\ InternationalConference on Geochronology and Cosmochemistry\ Berkeley "California\ U[S[A[#\ U[S[ Geological Survey\ CircularNo 0096\ p[ 298[

Suita\ M[T[F[\ Hartmann\ L[A[\ Kamo\ S[L[\ 0883b[ The Nature of the Barro Alto Layered Ma_c!ultrama_c Complex


and a discussion on the role of the Brasiliano and the Uruacžuano Cycles in Goia�s\ Central Brazil[ In] ExtendedAbstracts\ International Symposium on the Physics and Chemistry of the Upper Mantle\ Sa½o Paulo "SP!Brasil#\ pp[71Ð73[

Teixeira\ L[B[\ Martins\ M[\ Braun\ O[P[G[\ 0882[ Evolucža½o geolo�gica da Bacia do Sa½o Francisco com base em s(�smicade re~exa½o e me�todos potenciais[ In] Simp[ sobre o Cra�ton do Sa½o Francisco\ 1\ Salvador "BA#\ SBG:BA e SGM:BA\Anais[[[\ pp[ 068Ð070[

Thomaz Filho\ A[\ Lima\ V[Q[\ 0870[ Datacžo½es radiome�tricas de rochas sedimentares pel(�ticas pelo me�todo Rb:Sr[ Bol\Te�cn[ Petrobra�s\ Rio de Janeiro "RJ#\ Vol[ 13\ no[ 1\ pp[ 098Ð008[

Vasconcellos\ A[C[B[C[\ 0877[ O Grupo Andrela¼ndia na regia½o norte de Ouro Fino "MG#[ Dissert[ de Mestrado "IG!USP#\ Sa½o Paulo "SP#\ 088 p[ "ine�dito#[

Viana\ M[G[\ Pimentel\ M[M[\ 0883[ Dados geoqu(�micos e isoto�picos SmÐNd preliminares para rochas metavulca¼nicase metapluto¼nicas da regia½o de Mara Rosa[ In] Simp[ Geol[ Centro!oeste\ 3\ Bras(�lia "DF#\ SBG:CO!BS\ Anais[[[\ pp[037Ð040[

Wernick\ E[\ Fiori\ A[P[\ Bettencourt\ J[S[\ Choudhuri\ A[\ 0868[ A tecto¼nica r(�gida do _m do Ciclo Brasiliano e a suaimplicacža½o na estruturacža½o da borda sul e sudoeste do Cra�ton do Sa½o Francisco] tentativa de um modelo preliminar[In] Simp[ sobre o Cra�ton do Sa½o Francisco e suas faixas marginais\ 0\ Salvador "BA#\ SBG:BA\ Anais[[[\ pp[ 053Ð057[

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