Manizales medellín geolgía (salida Mine)

7/30/2019 Manizales medelln geolga (salida Mine)

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GEOLOGICALTRANSECTTHROUGHANACCRETIONARYMARGIN,WESTERNCOLOMBIA

FIELDTRIPSEPTEMBER3-52011

Preparedby

Dr.CesarVinascoUniversidadNacionaldeColombia.cvinasco@unal.edu.co

Dr.JamesPindellTectonicAnalysisLtd.UK

Dra.MarionWeber-UniversidadNacionaldeColombia

Dr.AgustnCardonaCorporacinGeolgicaAres.

Dra.LuzMaryToro-UniversidaddeCaldas

INTRODUCTION

Thenorthwesternmarginof SouthAmericais characterizedby theinteractionoftheSouthAmerican,

CaribbeanandPacificplates.Thisinteractioninvolvedmultipleepisodesofaccretionofoceanicterranes

(MORB, island arc and plateau) against the Pre-Mesozoic continental margin since the Lower

Cretaceous.Thisinteractionresultedinformationofsubduction-accretioncomplexesthatunderwenta

complextransitionfromprimitivetomoreevolvedcrust.

Overthelastfiveyears,newradiometric,geochemicalandfielddatahasenabledtherevisionofcurrent

geodynamicmodels for thenorthwesternAndean andCaribbeanrealms,allowingtoreaddresslong-

standingandimportantquestionsregardingsubduction-accretionmodels.Suchquestionsinclude:the

natureofaccretedterranes;thegrowthofbatholithswithincontinentalandoceanicplates;andtherole

ofmajorshearzonesresponsiblefortheredistributionoflitho-tectonicelementsinthemargin.

During the upcoming XIV Latin-American Geological and XIII Colombian Geological Congresses,

(Medellin, Colombia, September 2011), more specifically in the Special SessionCrustal growth and

modificationattheCaribbeanplatemargins,projectIGCP546"SubductionZonesoftheCaribbean",

newU-Pb,geochemical,isotopic,structuralandcartographicdatawillbepresented.U-Pbresultsfocus

onprovenance studiesundertakenonkeymetasedimentary sequences,providingnew insightto the


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understanding of regionalmodels.Recently generated information inother fields (e.g., geochemical,

isotopic,structuralandcartographic)alsosupportsthismodel.

PhysiographicallyspeakingthewesternmostsegmentoftheColombianAndesencompassestheCentral

and Western Cordillera aswell as the Atrato basin and the BaudoRanges (Fig. 1). The Central andwesternCordilleras areseparatedby theCaucaRiverdepression.Thegeologicalconfiguration closely

follows the physiographic trend whereby the two cordilleras belong to two contrasting domains

separatedby theRomeralFaultSystem(RFS)(Fig.2).TheRFSenclosesaseriesofrocks(includingthe

ArquiaComplex),whichishereinterpretedasanextensiveshearzone(kilometric-scale)composedof

multiplelithologicalunitsofvaryingages,diverseorigins,polydeformed,andinfaultedcontact.ThePre-

Mesozoic continentalmargin worked as aMeso-Cenozoic back stop, which is defined by the actual

CentralCordillera.TheaccretedterranesareinturnrepresentedbytheWesternCordillera,someofthe

componentsoftheArquiaComplexandrocksoftheBaudoRange(Figs.1,2).


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Fig.1.SimplifiedgeologicalmapoftheColombianAndes.Thelowerinsetshowsadetailedgeologicalmapofthe

studyareainAntioquiaandCaldasstates.ModifiedfromGonzlezetal.(1988)

DespitethecomplexdistributionofreportedagesfortheCentralCordillerablock,whichsuggestthe

presenceofpre-Mesozoicconstituents,anUpperPaleozoicLowerMesozoiceventisperhapsthemost

importantorogeniceventrecordedfortheblock.Thiseventcouldbeassociatedwiththebuildupof

PangeadrivenbythecollisionbetweenLaurentiaandGondwanaduringtheAlleghenianorogeny

(Vinascoetal,2006),andresponsibleforthesubsequentclosureoftheprotoAtlanticocean(Pindelland

Dewey,1982;Pindell,1985;PindellandKennan,2002).Triassictectonicregimerecordedforthe

Pueblitodiorite(Fig.2,#6)suggestsadominantleftlateralregimebythistime,incontrasttothe

dextraldominantregimefortheCretaceous.

However,thismodeldoesnotseemtoworkfornorthernmostColombiawheretheSierraNevadade

SantaMartamarksthenorthernterminationoftheAndeanchainwhereCardonaetal(2010)found


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temporaldiscrepanciesthatprecludeanyconnectionofthisareawiththemainAlleghanian-Ouachitan

Pangeanorogen.Furthermore,severalauthorshavesuggestedthatthepresentCentralCordillerablock

hasresultedfromnorthwardmigrationduringtheLateCretaceoustoEocene.


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.

Fig2.Localizationandlocalgeologicalmap.


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The Central Cordillera basement can be regarded as an Upper Paleozoic Permian metamorphic

sequence intruded by crustal syn-tectonic Permian and post tectonic Triassic granitoids with arc

imprints.ThebasementisalsointrudedbyupperCretaceousgraniticsuites,mainlyrepresentedbythe

AntioquiaBatholith(Figs1,2),relatedtoawell-establishedwesternsubductionzonecharacteristicofan

activecontinentalmargin(Botero,1963;Saenz,2003;Restrepo-Moreno,2009).Cretaceousmagmatism

hasregionallyresetstheK-Arsystem.TheCentralCordillerablockhasbeendescribedandgivenvarious

names through time including: Cajamarca Group (Nelson, 1957); Cajamarca Complex (Maya and

Gonzalez, 1995); the Tahami terrane (Toussaint and Restrepo, 1989), the Central Cordillera

PolymetamorphicComplex(ToussaintandRestrepo,1989)andtheCajamarcaValdiviaTerrane(Cediel,

etal.2003).

Other well-documented geochronological events in the region occurred during Devonian and

Cretaceoustimes(Halletal.,1972;Gonzlez,1980;ToussaintandRestrepo,1989).Finally,otherevents

are recorded during the entire Tertiary. These events are mainly associated with deformational

processes,syntectonicsedimentationandMio-Pliocenevolcanism(e.g.,AmagaandCombiaformations

respectively)

TheeasternmosttraceoftheRFSisdefinedbytheSanJeronimofault(MayaandGonzalez,1995).This

faultdefinesthebeginningofabroadboundarythatseparatestheCentralCordillerain theeast from

theaccretedterranestothewest.Regionally,thisbroadboundarycorrespondstoakilometricshear

zone hosting a series of rocks including: (1) the Cretaceous sedimentary-volcanic sequence of the

QuebradagrandeComplex(Fig.2,#7);(2)lowgradedevonian(?)metasediementaryrocksofSinifan

Schists(Fig.2,#8);(3)maficandultramaficTriassicsuprasubductionintrusives(Fig.2,#6)andfinally(4)

Permian(?)and/or(?)cretaceous(?)lowtomediumgrademetavulcano-sedimentaryN-MORBtype

sequences of the Arquia Complex (Fig.2, #5). The Amaga Formation (Fig. 2), a coal-bearing, Oligo-

Miocene sedimentary sequence (Grosse, 1926; Silva et al., 2008) unconformably covers the older

lithologicalunits.Mio-PliocenevolcanicandsubvolcanicrocksoftheCombiaFormation(Fig.2)covered

and intruded the Amaga Formation and other older rocks. Geometrically, the RFS shear zone is

characterizedbyan anastomosedarrangeof faults yielding ablock tectonics configuration.The rocks

andstructuresinsidetheshearzonearethemainfocusofthefieldtrip.

Asequenceofbasalticvolcanicsandflysh-typesedimentaryrocksoutcroptothewestoftheCauca-

Almaguerfault,whichis thewesternmostelementoftheRFS(MayaandGonzalez,1995).Theserocks


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areLower Cretaceous in ageandbelong to theBarrosoFormation,andareentirely confined to the

WesternCordilleraof Colombia. Theboundary with themeta-vulcanosedimentarysequences of the

Arquiacomplexisnotclear.Recently,Garciaetal(2010)suggestedthatthewesternmostmetabasic

rocksoftheArquaComplexaretransitionaltovolcanicrocksofthewesternCordilleraimplyingthatat

leastsomecomponentsoftheArquiacomplexbelongtothissequence.

Differentauthorsagree that theLateCretaceoustoearlyCenozoictectonicevolutionofthenorthern

SouthAmericanmarginwascontrolledbyitsinteractionwiththemarginsofanallochthonous(Pacific-

derived), anomalously thick Caribbean oceanicplate and itsassociated arc (Burke,1988;Kerr et al.,

1997;Pindelletal.,1998;Montesetal.,2005;Spikingsetal.,2005;Luzieuxetal.,2006;Vallejoetal.,

2006;Maresh etal., 2009;Weber etal., 2009). SubsequentPalaeogene orogenic phases seem tobe

relatedtovariationsinplateconvergence(velocityandangle)ortoaccretionaryphenomena(Pindellet

al.,1998;Restrepo-Morenoetal.,2009;Vallejoetal.,2009;Jaillardetal.,2010).Cardonaetal(2011),

suggest that the Caribbean oceanic plate influenced the Late CretaceousEocene orogeny of the

northern Andes by thecollision of theCaribbean arcwith thecontinentalmarginabout 90Mawith

subsequentinstallationofthesubductionregimepossiblysinceabout65Ma.Thissituationseemstobe

differentfromthatoftheCentralAntioquiasegmentoftheCentralCordillerawheresubductionregime

isrecordedatleastsince90Ma.Finally,theysuggestmagmaticquiescenceandblockupliftafter50Ma

asproductofshallowsubductionandobliqueconvergence.

RegionalreconstructionsgivenbyPindell(inprep)sinceJurassictimesinvolvestheeastwardsubduction

ofFarallonplateunderthecontinentalmarginrepresentedbytheCentralCordillera.Theresultofthis

subductionisrepresentedbytheQuebradagrandebeltcontainingthearcandbackarcrockswhilethe

Arquia belt containsHP-LTsubduction related rocks. Thesearcswere closed by120Maagainst the

CentralCordilleraandcontinuoussubductionlastinguntil70Ma.Concurrently,offshoreinthePacific,

theCaribbean-ColombianOceanicPlateau(CCOP)wasbeingextrudedatintra-oceanichotspotsontothe

Farallonlithospherefrom100to88Ma(Kerretal2003).TheeastwarddippingsubductionofFarallon

crust beneath the now composite terranes of Colombia allowed the plateau to converge with the

Colombianmargin. TheFarallon lithosphere continued tobe subducted beneath theaccreted upper

crustal material, albeit at a low dipping Benioff Plane. Panamanian subduction began in the

Maastrichtian,thusisolatingaCaribbeanPlateoutoftheFarallon.SouthAmericabeganamorehead-on

overthrustingoftheCaribbeanlithosphereinCampanian-Maastrichtiantime,accretingplateaubasalts


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that were arriving at the trench into the Western Cordillera. During the Tertiary, South America

overthrust more and more the Caribbean Plate ina flat slab geometry. Thus,afteraccretion of the

Western Cordillera at the start of this overthrusting, first the Central Cordillera (Paleocene-Middle

Eocene;Laramide)andthentheEasternCordillera(LateOligocene-Miocene;earlyAndean)havebeen

thrust over theeastern leading edge of theunderthrusted Caribbean lithosphere.Presently, seismic

tomography indicates that theCaribbean slab occurs beneathnorthern Colombiaall theway to the

LlanosBasin(vanderHilstandMann,1994).Finalepisodesofdeformationinthechainarerelatedto

thecollisionof thePanama-ChocoblockinEarlyMiocene-earlyPliocene (Pennington,1981;Toussaint

and Restrepo, 1988; Duque-Caro, 1990; Mann and Corrigan, 1990; Van der Hilst and Mann, 1994;

Taboadaetal.,2000;Trenkampetal.,2002).CollisiondriveschangesintheRFSkinematicsfromright-

lateralinthesouthtoleft-lateralinthenorth(Suterelat,2008).ThePanama-Chocoblockcollideswith

NWSouthAmericainanEtoESEdirection(Duque-Caro,1990;Taboadaetal.,2000).Itisconsideredas

a rigid indenter, which induces deformations north of 5N reaching the lowlands of the Eastern

Cordillerasome600kmeast(Suter,etal.2008).Thecollisionisconsideredtoberesponsibleforthe

latest andmajorphaseof uplift in the Colombian Andeswhichcorresponds tothe Andean tectonic

phasethataffectedthethreecordilleras(Taboadaetal.,2000;Cortesetal.,2005).

In the model depicted above, the Quebradagrande belt corresponds to an autochthonous arc

contemporaneous to the Arquia belt produced by eastward subduction of the Farallon plate.

AlternativeshypothesissuggestthatArquiaComplexisacompositecollectionofrocksincludingpre-

mesozoicanduppercretaceousfragments.Someofthesefragmentswouldberemobilizedpiecesfrom

bothCentralandWesternCordilleraina longlastingshearzone,developedtothecontinentalmargin

sinceTriassictimes,assuggestedbyASMstudiesinthePueblitodiorite(Fig.2,#6)(Rodriguezetal.

2010). TheQuebradagrandecomplexcouldrepresentanintracratonicmarginalbasintrappedduring

the collision of the CaribbeanColombian Cretaceous oceanic plateau, which accreted west of the

ArquaComplexintheEarlyEocene(Niviaetal.2006).

Ontheotherhand,MorenoSnchezetal(2007)standsthatthereisnotproveoftheexistenceofany

metamorphicbasementtothewestoftheQuebradagrandeComplex.Instead,theyinvokethepresence

ofamagmaticarcwestoftheQuebradagrandeComplex.

Finally,acompletedifferentlineofargumentationfortheoriginoftheCaribbeanplateisgivenby


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James,K.(2006)whosuggestaninter-Americanoriginfortheplate.Argumentsarebasedmainlyinthe

existence of coeval of Caribbean and neighbouring continental areas of regional deposits of Albian

shallowwaterlimestones,Paleocene-MiddleEoceneflyschdeposits,MiddleEocene limestones,and

thepresenceofa regionalLateEocenehiatuscompatiblewithaninter-Americanlocation,notwitha

changing Pacific-Caribbean development. Additionally, the internal structural conformity of the

CaribbeanPlateandoftheMayaandChortisblockswithregionalgeologyofMiddleAmericashowsthat

nomajormigrations or rotations have occurred (James, 2006), aspects invokedbymodels of pacific

origin.

Wehopethatnewdatatobepresentedduringthespecialsessioncontributetobetterelucidatethe

regionalmodels.Moreimportantis,although,theopeningofnewwaysofcooperationandthelooking

forresearchpathsyetunexplored.

FIELDTRIP

A3-dayfieldtripGeologicaltransectthroughtheevolutionofanaccretionarymargin willguideus

throughthevariouselementsthatformedthecurrentwesternSouthAmericanmargin(Fig.1,2).These

include thepre-Mesozoic South Americanbasement rocks, accreted metamorphosed mixed oceanic

domains(ArquiaComplex),anearlierCretaceousunitwitharc-affinity(QuebradagrandeComplex),the

Colombian-Caribbean plateau (CCP), and various magmatic rocks that range from Cretaceous to

Miocene,suggestingactivemagmaticactivitythroughtime.

ThetripwilltakeusfrommodernMedellncitytothehistoricalcolonialtownofSantaFedeAntioquia,

along the CaucaRiver, heading afterwards to themountainous city ofManizales,where coffee and

volcanoesarepartofthelandscape.

Generalinformation

Figure2showsthemainroadslinking Medellin-SantaFedeAntioquiaBolomboloLaPintada

Manizales.Themapincludesfieldpointsofobservation(yellowstars)onageologicalbasemap,which

inturnshowsthemainlithologicalunitsreferredinthetext.


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Santa FedeAntioquia is a nacionalhistoricalmonument given its colonial architecture. It possess 6

churchesandhousesoftheXVI,XVIIyXVIIIcenturies.Thetownislocatedat550m.a.s.landameanof

25Co.Itisrecommendedwearingproperclothsforwarmclimateandkeepenoughliquid.

Picturesofthearea,includingpanoramicalviewsandrockcharacteristicsareavailableatthislink:

https://picasaweb.google.com/116714157401905796743/PanoramicalPicturesNearSantaFeDeAntioquia

?feat=directlink

Itinerary

ThefieldtripisintendedtoshowanoverviewofthecomplextransitionoftheCentralCordilleraintothe

WesternCordillerathroughtheRFS.ThefirstdaywewillcrosstheCaucaValleyinthenorthernpartof

theareauntilreachrocksoftheWesternCordillerarepresentedbytheSabanalargaBatolith(Fig.2,

circle2).DuringthejourneywewillobserveoutcropsoftheAmagaFormationanddeformedrocksof

theArquiacomplex.TheseconddaywewillheadtothesouthlookingforLaPintada(Fig.2)andArqua

creektoseeexposuresofmafic tointermediateTrmagmatismandgarnetiferousamphibolitesofthe

ArquiaComplex.DuringtheJourneyitispossiblevisitoutcropsoftheThevolcanicBarrosoFormation,

sedimentsoftheAmagaformationandvolcanicsoftheCombiaformation.Thethirddaywewillheadto

Manizales.DuringthislastjourneywewillobserverocksbelongingtotheQuebradagrandeandArquia

Complex.

Day1(September3)

ThefieldtripbeginsintheMedellincityheadingNWtotheSantaFedeAntioquiatown.Thefirstfield

pointisknownas theBoquern(Fig2 -Yellowstar1).ThispointallowstheobservationoftheAburra

ValleytotheeastwhereMedellinislocated.ItispossibleeitherobservetheCaucaValleytotheNorth.

In this area we can observe Tr (?) Amphibolites of the Central Cordillera and medium grade schist

belonging to the Cajamarca Complex. Amphibolites are probably related to deformed gabbros and

amphibolites located within the RFS although some authors considered it as allocthonous blocks

obductedinthelowerCretaceous(ToussaintandRestrepo,1989).


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The journey takesus to the CaucaValley whereOligo-Miocene sediments of the Amaga Formation

outcrops (Fig. 2- yellow star 2). The siliciclastic Oligo-Miocene successions in the region bear key

geologicinformationtounravelthepaleotectonicandpaleogegraphicevolutionofNWSouthAmerica.

Twomodelsareactuallybeingconsidered,andinterandeandepressionmodelfordeposition(Guzmn,

2003;Sierra,2003;Silva,2008),orapeneplainconfigurationmodel(Grosse,1926)withapotentialfor

marineinfluence(Escobar,1990;SchulerandDoubinger,1970).

Passing5kms inNWdirection fromSantaFedeAntioquia,wearenow fullylocated inthewestern

cordilleradomain.InthispointoutcropthelowerMesozoicSabanalargaBatolith(Fig.2yellowstar3).

Somepicturesoflandscapesaretakenfromthisplace(seelinkofpictures-panoramicalpictures).

We spend the night in Santa Fe de Antioquia where there are plenty of nice places for diner and

drinking.

(http://www.google.com/search?q=santa+fe+de+antioquia&hl=es&prmd=ivnsm&tbm=isch&tbo=u&sou

rce=univ&sa=X&ei=8h3DTdTMBoq2twe-9ICqBQ&ved=0CEIQsAQ&biw=1280&bih=639).

Day2(September4)

MostpartofthedaywillbededicatedtotheneighboringareasofSantaFedeAntioquiawithintheRFS

areaofinfluence.WewillvisitthePuentedeOccidente,abridgeovertheCaucariver(Fig.2yellowstar

4)(seelinkofpictures-panoramical pictures). In this place outcrops L-tectonites Tr(?) gabbrosand

amphibolites.ThesemaficrocksarecontinuouswithPueblitodioritefurthersouth(Fig.2#6).Rodriguez

etal.(2010)presentevidenceof intrusivecontactwithschistof Sabaletas(Fig.2 #5), implyingapre-

mesozoicageforatleastsomefragmentsoftheArquiaComplex(seelinkpicturesstructuresinschist).

Other authors consider the contact as being regionally faulted of Sabaletas schist with Tr Pueblito

diorite.

Next,wewillcrosstheCaucaRiverheadingtothesmalltownofSucre.Wecanobservewestverging

thrustingstructuresofultramaficrocksoverlowgrademetasediements.Ifhikingsome30minutesalong

QuebradaSecawecanobserveathrustofQuebradagranderocksoverTertiary(?)syenogranitesverging

tothewest.Thewestvergingofstructuresisageneralizedcharacteristicofthearea.Almostallofthe


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actualcontactsbetweenunitsinsidetheshearzone(RFS)arelowanglethrustsverging totheW-SW.

ThisisprobablyaCenozoicstructure.

Hiking along the Barbudo creek isanoption; itwould depend of the weather. Along the creek it is

possibleobservestructuresassociateswithdeformedTrgabbrosandamphibolites(seelinkpictures

Barbudo creek), deformed sediments and volcanics of Quebragrande formation (see link pictures

structures in Quebradagrande). The Barbudo creek is the best route in the area to see structures

associated withRFS. Includesdiscrete shear zones, associated folding, stretched boudins, etc. Some

graniticsillsareobserved intrudingtheshalesequence(seelinkpicturesBarbudocreek).Ultramafic

rockscanbeseen few kms eastofSucrealonga localroad. Theycorrespondto lenseshapebodies

paralleltoregionalNNWstructures.FinallywewillascendtowardsLlanadasvillagetotheeast.Inthis

pointoutcropsschistofCajamarcaComplexagain.Thisisanexcelentpointtoobservelandscapestothe

westandsouth-west(seelinkpicturespanoramicalpictures).

IntheafternoonwewillheadtothesouthlookingforLaPintada(Fig.2).Duringthejourneyitispossible

observevolcanicsrocksofMio-PlioceneCombiaFormationandlandscapesassociated(seelinkpictures

panoramicalpictures).

WewillspendthenightinLaPintada(MiradordePipinta) whichisahotellocatedclosetotheCauca

riverwitha very nice view of geoformsassociated withMio-Plioceneporphyritic rocks. These rocks

normallyhostimportantdepositsofgoldandbasicmetalsactuallybeingexplotedintheMarmatomine

district.

Day3.(September5)

FromLapintadawewillheadtothesouthtotheManizalescity.Thefirstpointofobservationwillbein

theGuavitacreekwheremassiveserpentinitewithperidotitecoresappears.Onekmfromthispointwe

willvisit theRioArquiawhereoutcropsblackandgreenintercalatedschistsintrudedbyandesiticand

daciticMio-Plioceneporphyritic rocks. Locally theschists presente faultedcontactwith garnetiferous

amphibolites. Finally, getting to the Manizales we will observe Metagabbros and Permian intrusive

gneisses.


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Wewillspendthenightinthecity.Manizalesislocatedat2153m.a.s.l.closetotheNevadodelRuiz,an

activevolcanowhichreach5321m.a.s.l.(http://intranet.ingeominas.gov.co/manizales/Ruiz)Manizales

istheColombianCoffee-GrowersAxistogetherwithPereiraandChinchintowns.

Somepicturesofthecitycanbeseenat:http://www.google.com/search?q=manizales&hl=es&prmd=ivnsum&tbm=isch&tbo=u&source=univ&sa

=X&ei=sJjJTaG0F4Le0QHdqtjnCA&ved=0CEUQsAQ&biw=1280&bih=617

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