Kinematics of Sürgü Fault Zone (Malatya, Turkey): A remote sensing

16 Pages·2013·8.26 MB·English

by  Ayten Koç

JournalofGeodynamics65 (2013) 292–307

ContentslistsavailableatSciVerseScienceDirect

Journal of Geodynamics

journal homepage: http://www.elsevier.com/locate/jog

Kinematics of Sürgü Fault Zone (Malatya, Turkey): A remote sensing study

AytenKoc¸ ∗,NuretdinKaymakcı

DepartmentofGeologicalEngineering,MiddleEastTechnicalUniversity,Ankara06531,Turkey

a r t i c l e i n f o a b s t r a c t

Articlehistory: TheSürgüFaultZone(SFZ)islocatedinSEAnatoliaextendingfromGöksuninthewesttoC¸elikhanin
Receiv ed11January2012 the east,w herei tbifu rcates fr omtheE as tA natolian FaultZone. Adet ailedan aly sisa long the f aultusi ng
AReccceepivteedd i4n Ar euvgiussetd2 f 0o1rm2 3 August 2012 sate llite images , d igital elev ation mod els ( DEMs) an d aeri al pho to graphs r evealed that th e S FZ dis plays
characteristicdeformationpatternscommontodextralstrike-slipfaults,includingpressureridges,dis-
Available online 13 August 2012
placedlinearvalleys,anddeflectedstreamcourses.Inadditiontothis,faultslipdatacollectedfrom17

sitesindicatedthattheSFZisadextralstrike-slipfaultzonehavingreverseandnormalcomponentsinits
Keywords:
westernandeasternparts,respectively.Thetypeofdip-slipcomponents,orientationofthepalaeostress
Strike-slipfault
configurations,andrelatedstructuresalongthefaultarecompatiblewithalongstrikevariationsofa
Remotesensing
FPaaulaletoksint reemssa atincaslysis tsitvreikset-rselaipm faduelflt escytsitoenms atlhoantg stuhpepfoarutlst tzhoen edeinxdtriacla tneatthuaret tohfe thdee xftaruallt ozfofsneet. oOfbtsheerSvFeZd hmaasxbiemeunmm couremtuhlaan-
SEAn atolia 3km since theestablis hmen tof thes tream networ kin the region. Accor din gto th epr eferre dtect onic

modelsuggestedinthisstudy,thepresentdextralmotionalongtheSFZoccurswithinaregionalsinistral

systemrelatedtowestwardsescapeoftheMaras¸Block,squeezedbetweenAnatolianBlockandArabian

PlateinN–Sdirection.

© 2012 Elsevier Ltd. All rights reserved.
1. Introduction principal displacement zone (PDZ), or y-shear (Fig. 1a) develops

generallyatanadvancedstageofstrike-slipdisplacement,parallel

The structural deformation patterns in strike-slip fault zones tothemainshearzone(Nayloretal.,1986).Theotherstructures
havebe enestabli shedsinceth e1980s( Bid dleandCh ristie -Blick, inc lud e Syn thetic Shea r (or r-s he ar), Antith etic Shear (r(cid:4)-shear),

1985; Sylvester, 1988). Strike-slip fault zones are classified as Secondary Synthetic Shear (p-shear), extension structures (nor-

convergent, divergent and simple or through-going strike-slip malfaults,gashes),andcompressionalen-echelonfoldsandhigh

faults,dependingonthemovementvectorsofinterveningblocks anglereversefaults(Fig.1a).Ther-,andp-shearsaresub-parallel
(Sande rson and M ar chin i, 1984). In simple str ike-slip zon es, the (appr oximate ly ±15 ◦) to the y-sh ea r an d they al l ha ve the same
major horiz onta l compres sion ax is makes a n approxim ately 45◦ senseofslip.Ho wever ,th ean glebetw een the y-sh eara ndt her(cid:4)-
angle withthezo ne(Fig.1a)w hilet hisang lei shigherinthec on- shear isa roun d75◦and they have opposite slip senses(F ig.1 a).T he

vergentstrike-slipfaultsandindivergentstrike-slipfaultzonesit angularrelationshipbetweenthestructuresismainlycontrolled
islessth an45◦ (Sa nders ona nd Marchini, 1984).De velop ment of bythein ternalfrictio nangleo fthe faultedm ate rialand thecohe-

convergent and divergent strike-slip fault zones depends on the sionandtheyobeytheCoulomb–Mohrcriterion(JaegerandCook,

changeintheregionalstressfieldorreactivationofzonesofweak- 1971).

ness(Deweyetal.,1995).Analogandnumericalmodels(Wilcox TheEastAnatolianFaultZone(EAFZ)isoneofthemajorsinistral

etal.,1973;SegallandPollard,1983)demonstratedthatthepat- intra-continentalstrike-slipfaultsinEasternAnatoliaalongwhich

ternofstructureswithinstrike-slipfaultzonesiscontrolledbythe the Anatolian Block is moving westwards (S¸engör and Yılmaz,

typeandorientationofhorizontalmajorandminorcompressive 1981) (Fig. 1b). The EAFZ displays all the characteristic features

stressesaswellasalongstrikevariationsofthemasterfaultstrand ofasinistralstrike-slipfaultzone(Perinc¸eketal.,1987;Perincek

(AmbraseysandTchalenko,1970;BiddleandChristie-Blick,1985; and C¸emen, 1990; Lyberis et al., 1992), and recent GPS studies

WoodcockandFischer,1986;Sylvester,1988).Inastrike-slipfault indicatethatthefaultzoneistransferringthetotalconvergentvec-

zone, the master fault strand (MFS), which is also known as the tor into strike-slip motion (Reilinger et al., 2006), which implies

thatoverallEAFZisasimple(through-going)strike-slipfaultzone

withoutconvergencenordivergence.Ontheotherhand,anum-

∗ berofsplayfaultsbifurcatefromthemainstrandoftheEAFZand
Correspondingauthor.
transferthedeformationoutofthefaultzone.Faultkinematic(e.g.
makEc-ı)m.ail addresses: [email protected] (A. Koc¸ ), [email protected] (N. Kay- Arpatan dS¸a rog˘lu,1972; S¸aro g˘l uet al.,1 992;P erinc¸ eketal.,1 987;

0264-3707/$–seefrontmatter© 2012 Elsevier Ltd. All rights reserved.

http://dx.doi.org/10.1016/j.jog.2012.08.001
A.Koc¸,N.Kaymakcı/JournalofGeodynamics65 (2013) 292–307 293

Fig.1. (a)Riedeldeformationpatternterminologyforasinistralshearzone(afterAmbraseysandTchalenko,1970;Sylvester,1988),(b)majoractivestructuresaround

easternMediterranean,(c)majorpaleotectonicunitsofTurkey(modifiedfromS¸engörandYılmaz,1981),(d)majorpaleotectonicandactivestructuresincentralandSE

Anatolia(afterKaymakcietal.,2010).AF:AltınyaylaFault,BF:BozovaFault,DF:DeveliFault,DFZ:DeadSeaFaultZone,EAFZ:EastAnatolianFaultZone,EF:Ecemis¸Fault,

GF:GürünFault,IF:Ilic¸Fault,KDF:Karcadag˘Fault,KF:KozanFault,NAFZ:NorthAnatolianFaultZone,MF:MalatyaFault,OF:OvacıkFault,PF:PertekFault,SF:SarızFault,

SFZ:SürgüFaultZone,YF:Yes¸ilyurtFault.

Perincek and C¸emen, 1990; Lyberis et al., 1992; Kaymakci et al., thecontroversialbehavioroftheSFZ.Forthesepurposes,various

2010andreferencestherein)andGPSstudies(e.g.Reilingeretal., image processing and enhancement techniques were applied to

2006)indicatemostofthesesplayfaultsarereactivatedolderstruc- data sources including Landsat TM, ETM+, Quickbird and ASTER

tureswhichdonotnecessarilyobeyColoumb–Mohrdeformation imagery combined with SRTM and 1/25,000 scale digital eleva-

criterion.SürgüFaultZone(SFZ)isoneofthesplayfaultswhich tion models, and stereo-pairs of aerial photographs. The results

bifurcates from EAFZ around C¸elikhan with approximately E–W obtainedfromremotelysenseddatahavebeenverifiedinthefield.
strikeand theb ifurcat ionang le isabou t30◦( Fig.1d).Morph otec- During th e fie ld verific ation, f ault slip d ata w ere co lle cted and

tonicfeaturesandfaultkinematicdataindicatethattheSFZisa detailedobservationsofthestructureswereperformed.

dextralstrike-slipfaultzonecontrarytoexpectedsinistralsense

proposedbypreviousstudies(ArpatandS¸arog˘lu,1975;Perinc¸ek 2. Geologicalsetting

andKozlu,1984).ThismakestheSFZapeculiarstructureasbeinga

dextralfaultzonesub-paralleltoamajorsinistralintra-continental TheLateCretaceoustorecenttectonicdevelopmentoftheeast-

EAFZ.SuchmotionalongtheSFZseemsnottobefeasibleaccording ernMediterraneanregionisrelatedtotheconvergencebetween

topublishedanalogandnumericalmodelsandmostofthefield theAfro-ArabianandEurasianplates,whichismostlyaccommo-

observations elsewhere. Therefore, the dextral nature of the SFZ datedbynorthwardsubductionofbranchesoftheNeotethysOcean

deservesexplanation. (S¸engörandYılmaz,1981;BarrierandVrielynck,2008)leadingto

Inthiscontext,themainpurposeofthisstudyistodetermine theformationoftwomajorsuturezones(Fig.1c).Theseincludethe

thegeometry,deformationmechanismandkinematicsoftheSFZ northernandsouthernbranchesoftheNeotethysOcean(S¸engör

by using remote sensing techniques and field studies including andYılmaz,1981).ThenorthernoneisdemarcatedbytheIzmir-

fault slip measurements. Additionally, it is aimed to construct a Ankara-ErzincanSutureZoneanddevelopedbetweenthePontides

tectonicmodelinordertoprovideasatisfactoryexplanationfor (Eurasia)inthenorthandTauride-AnatolidePlatform(Gondwana)
294 A.Koc¸,N.Kaymakcı/JournalofGeodynamics65 (2013) 292–307

Fig.2. (a)Samplelocationsand(b)majortectonicelementsinthevicinityofthestudyarea(legendislikeinFig.1)(afterPerinc¸eketal.,1987;Kaymakcietal.,2006,2010).

inthesouth(Fig.1c).Theinterveningcontinentalblockscollided demarcatedbytheBitlisZagrosSutureZoneanddevelopeddueto

after the oceanic lithosphere was completely subducted north- collisionbetweentheArabianPlateandtheEurasianPlate(Fig.1c)

wards under the Pontides by the end of the Late Cretaceous bytheEocenetoOligocene(GhasemiandTalbot,2005;Hüsingetal.,

and collision lasted until the end of the Oligocene to Earliest 2009;Rollandetal.,2012)orlater,bytheendofMiddleMiocene

Miocene(Kaymakcietal.,2001,2003,2009).Thesouthernbranchis (S¸engörandYılmaz,1981;Deweyetal.,1986;Keskin,2003;S¸engör
A.Koc¸,N.Kaymakcı/JournalofGeodynamics65 (2013) 292–307 295

Fig.3. Simplifiedgeologicalmapandactivefaultsofthestudyarea(partlymodifiedfrom1/500,000scalegeologicalmapofMTA).Halfarrowsindicatedirectionoffault

blockmovements.

etal.,2003;Faccennaetal.,2006;Hüsingetal.,2009;Okayetal., andChristie-Blick,1985;Sylvester,1988;CunninghamandMann,

2010). 2007).
Although the exact timing of collision between Eurasian and TheSFZ(ArpatandS¸arog˘lu,1975;Perinc¸ekandKozlu,1984)has

Arabianplatesisstillunderdebate,theconsequencesofthiscolli- averypeculiarcharacteristicinhavinganalmostE–Wtrend(Fig.2).

sionarebetterknownNevertheless,post-collisionalconvergence ThefaultzonebifurcatesfromtheEAFZintheeastanddelimitsa

ineasternAnatoliaisstillactiveandgavewaytothedevelopment number of NNE–SSW trending major faults including Sarız Fault

of transcurrent tectonics that is dominated by the dextral North (SF),GürünFault(GF),andMalatyaFault(MF)(Fig.1d).Itisalmost

Anatolian and sinistral East Anatolian fault zones. Along these perpendiculartotheN–SconvergencevectorbetweentheArabian

fault zones, the Anatolian Block is escaping westwards toward andEurasianplates(Reilingeretal.,2006)andhasmorphotectonic

theHellenictrench(Fig.1b)whichaccommodateAfrica-Eurasian features and kinematic data indicating dextral strike-slip nature

convergencetogetherwithCyprussubductionzone(S¸engöretal., withreverse(inthewest)andnormal(intheeast)components;

1985;S¸engör,1987;DeweyandSengör,1979;Arpat,1972;Arpat however,itissub-paralleltothesinistralEAFZ(Fig.2).Thismakes

andS¸arog˘lu,1975;KhairandTsokas,1999). theSFZanenigmaticstructureinhavingadextralstrike-slipchar-

Apart from Arabian collision, the present tectonic scheme of acterwithinasinistralstrike-slipsetting.Thisisunexpectedsince
southern and south-ea stern Ana tolia has be en shape d by su b- itsstr ikedev i atesonly 30◦ count erclock -wis ef romthestri keof

ductionoftheoceaniclithosphereoftheAfricanplatebelowthe theEAFZ;hence,itisnotanantitheticstructureoftheEAFZ.Most

Taurides that probably had been subject to slab roll-back, slab ofthewesternsegmentoftheSFZdevelopedalongthesouthern

detachment,slabbreak-offandSubductionTransformEdgeProp- boundaryoftheMaras¸Block(Fig.3),whichcontainsmagmaticarc-

agator(STEP)(GoversandWortel,2005)faultprocessessincethe massifandSupraSubductionZoneophiolitesdevelopedduringthe

MiddleMiocene(Faccennaetal.,2006;Gansetal.,2009;Kaymakci LateCretaceoustoEocenebetweentheTauride-AnatolidePlatform

etal.,2010;VanHinsbergenetal.,2010;Biryoletal.,2011).This inthenorthandAfro-ArabianPlateinthesouth(Fig.1c)(Robertson

resultedinthedevelopmentofcompressional–contractionalgeo- etal.,2006;Kaymakcietal.,2010),

dynamicsineasternAnatoliathatismanifestedbythrustingand The SFZ and palaeotectonic (pre-Late Miocene) evolution of

strike-slipfaultingwithconsiderablereversecomponents.West- the region has been studied mainly by Arpat (1972), Arpat and

wards, the compressional–contractional deformation in eastern S¸arog˘lu(1975),Perinc¸ekandKozlu(1984),Perinc¸eketal.(1987),

Anatoliahasbeengraduallyreplacedbystrike-slipandextensional Kozlu(1987),MuehlbergerandGordon(1987),S¸arog˘luetal.(1992),

tectonics in response to these mantle processes, that dominate Yurtmenetal.(2002),andRobertsonetal.(2006).However,the

mainly in central Anatolia and in western Anatolia respectively geometry, morphotectonics, deformation mechanism and kine-

(S¸engör et al., 1985; Dewey et al., 1986; Perinc¸ek et al., 1987; maticsoftheSFZisstillunclearandthediscrepancybetweenits

S¸engör,1987;Reilingeretal.,2006).Theendresultisacomplex dextralnatureandexpectedsinistraldisplacementisunderdebate.

array of faults and fault zones that have changed character in Geographically, the regional extent of the SFZ lies between

spaceandtimesincetheMiddleMiocene.Forexample,incentral theGöksun–C¸elikhan,Dog˘ans¸ehirandNurhakregionswheredif-

andsouth-easternAnatolia,threetypesoffaultshavedeveloped ferent Mesozoic to Paleogene tectonic units collided and were

(Fig.1d)(Kaymakcietal.,2010).Theseinclude:(1)sinistralstrike- amalgamatedduringtheNeogene(Fig.3).Thegeologicalmapof

slipfaultswithNNE–SSWtoNE–SWstrike,(2)curvilinearfaults the region was prepared mainly by Turkish Petroleum Co. geol-

with average E–W strike and (3) dextral strike-slip faults with ogists during the early 1980s (Perinc¸ek and Kozlu, 1984) and

NW–SEstrike.Atpresentmostofthesestrike-slipfaultshavenor- also covered by the 1/500,000 scale Sivas and Hatay sheets of

malorreversecomponents.Themostimportantfactorsgoverning thegeologicalmapofTurkeycompiledbyGeneralDirectorateof

normalorreversecomponentalongastrike-slipfaultaretheirori- MineralResearchandExploration(Ankara,Turkey)(Fig.3).How-

entationandcurvaturewithrespecttomaindisplacementzoneand everthesemapsaremainlyconcentratedonlithostratigraphicand

regionalstresstensor.Forexample,re-strainingorreleasingbends largescalestructuresthatdonotincludemostoftheactivestruc-

oroff-setsaccommodatelocalcontractionandextension(Biddle tures.
296 A.Koc¸,N.Kaymakcı/JournalofGeodynamics65 (2013) 292–307

3. Dataandmethods

This study integrates data sets obtained from two different

disciplines:(1)remotesensingand(2)fieldobservation.Morpho-

tectonic structures and kinematic indicators were mapped and

interpreted using remote sensing techniques and subsequently

theywereverifiedinthefield.Additionally,fault-slipdatawerecol-

lectedfrommesoscopicfaultsduringfieldstudiesforpalaeostress

inversionanalysis.

3.1. Remotesensinganalysis

Theappliedremotesensingtechniquesincludedprocessingand

interpretation of satellite images, and stereographic aerial pho-

tographs with the utilization of mirror stereoscopes. The used

satellite imagery included Landsat 4, 5 and 7 (TM and ETM+),

AdvancedSpace-borneThermalEmissionRadiometer(ASTER),and

Quickbird images obtained from Google Earth and 167 stereo-

graphicaerialphotographswith1/35,000scaletakenbyGeneral

Command of Mapping (Turkey). Further image enhancement

techniques, including contrast enhancement, color composites,

PrincipalComponentAnalysis(PCA)andDecorrelationStretching

(DS)wereperformedontheASTERandLandsatdatainorderto
enha nceim agevisual izat ion. Additi onall y,90m× 90m ( 3(cid:4)(cid:4))res o-

lutionShuttleRadarTopographicalMission(SRTM)dataand25m

resolutiondigitalelevationmodels(DEMs)preparedfrom1/25,000

scale topographic maps are used to aid the interpretations. The

abovementionedimagesandDEMshavedifferentlevelsofspa-

tial(ground)andspectral(i.e.,differentwavelength)resolutions,

andtheyareusefulfordistinguishinglithologiesandfordelineat-

ing structures at different scales. Finally, all of these data were

co-registered and combined in a GIS environment together with

previouslyobtainedmapstocarryoutanintegratedanalysis.

3.2. Groundtruthingandfaultslipdataanalysis

Fieldstudiesweremainlycarriedoutonthemainstrandofthe Fig.4. Fieldphotographsoffaults.(a)Intenselyshearedreversefaultaroundsite4
SFZforg roundt ruthin gofth estructu res an dki nema ticindi cat ors (vie w toS)a nd(b)norma lf aultsa rou ndsite19 (viewt oNW)( seeF ig.2afo rth e
locatio ns of the site s).
interpreted from the remotely sensed imagery in various scales.

During the field studies, various compressional and extensional
structu resw ereo bserved indiffer entlocationsalo ngth efaultzone Atotalof246faultslipmeasurementsweretakenfrom17sites
(Fig.4aand b)in additiont os lickensid edsurfac es(Fig .5), block tilt- acros sthe SF Z.Du ring the analysisofthefa ultsl ipdata ,misfi tf aults
ing( i.e. ,rot ati on withres pe cttohorizon talaxis) ,alig ne dmin eral within eac h an alyzed clu ster wer e sepa rated fro m th e bulk data
wat ersp rings,na rrow linearva lle ys,andfaul trocks (phaco ids,fault basedo nma ximumm isfitang le(AN G)andma ximum qu ality esti-
brecci a,catacl asites,fa ultgo uge,etc .). mator (RU P)andthe nanaly zedse parate ly.T hisprocess wasapp lied
Furth er,thefault slipd atacol lectedfromexposedfaultplanes iterati velyu ntil reliab leresults wereobta ined .Thecr iteri aofthe
(Fig.5)alon gth emai nstr ando ftheSFZ were usedfor stress inver- reliabilitya rede termine das20◦ forth emaximu mde viation (A NG)
sion to resol ve t he kin ematic s of t he f ault z one u sin g Ang elier’s and50◦fo rthe maximumv al ueofth equ alityestim ator(RUP) forall
meth od (Angel ier, 1994). This is base d on the r econst ruction of thef aultsin ea chdataset inacc ord an cewith themetho d(Ang eli er,
thestres sellipsoid inorde rtod et ermine re lativ emagnitudesa nd 198 8, 199 4) . The faul ts t ha t did not fu lfill t hes e condit ions were
orie ntatio nsofthe pri nciple st resses(Ang elier,19 79,1984,19 90). consid ereda sspu rious (19d ata) and they wered isregarded from
Therearetw of und amental assumpt ionsinthi sappr oach: (1)the furtherana lys isandma keu parou nd8 %of alldat a.Inversiono fthe
bulks tate ofst ressinasmal lareaisunifo rm and (2)theslip dir ec- datawa scarried out onth ere mainin g2 27 sli pme asuremen ts.

tion is parallel to the maximum resolved shear stress along an

optimallyorientedplaneofweakness(Wallace,1951;Bott,1959). 4. Resultsanddiscussion

Duringtheconstructionofthestressconfigurations,themaximum

shearstressdirectionisdeterminedbycalculatingtheshapefac- The enhanced satellite images of the Sürgü Fault Zone (SFZ)

torandorientationofthestressellipsoidbyusingthebest-fitting display various kinematic indicators and morphological features

reduced stress tensor based on the given fault slip data and the relatedtoitsactivity.Themostprominentofthesearethelinearly
orientati onsof thethr eeprin cip alst ressa xes((cid:2) :m axim um, (cid:2) : arrange dp re ssurerid ges forme dmainlyal on gthe Kur ucao vaseg-
1 2
intermediate a nd (cid:2) : m inimum). The sh ape facto r of any str ess ment (Fig . 6a), and step- overs al ong the main cou rse of the SFZ.
3
ellipsoid is d eterm ine d from; ˚= ((cid:2) −(cid:2) )/( (cid:2) −(cid:2) ) a nd ranges Pressu re r idges are associated with strik e-slip motio n a nd con-
2 3 1 3
between tw o extreme v alues of 0 and 1. The ˚ con strai nts all- trolledby initial fau ltgeometry .Inad dition,the orientat iono fthe
possible cases between uniax ial ((cid:2) =(cid:2) ; ˚=0 o r (cid:2) =(cid:2) ; ˚ =1) pressur er idgesc learly definesth es trikeofth eSF Z,whichism a inly
2 3 1 2
to tri-ax ial str ess config urations ((cid:2) > (cid:2) >(cid:2) ; ˚ = 0.5) (An ge lie r, inanE–W dire ction.I tstarts from the C¸e likh anB asinin t heeast
1 2 3

1994). and continues to the Sürgü Village in the west, and controls the
A.Koc¸,N.Kaymakcı/JournalofGeodynamics65 (2013) 292–307 297

Fig.5. ReversefaultdevelopedinthewesternendoftheSFZaroundGöksun(site1,seeFig.2foritslocation).(a)Slickensidedfaultsurface(viewtoSW),(b)itsclose-up

picture,and(c)palaeostressconfigurationofthesefaults.NoteNW–SEdirectedcompression.

Fig.6. (a)Uninterpretedand(b)interpretedASTERimage(bandcombination;R:3,G:2,B:1)showingpressureridgeswithinananastomosingpatternoffaults(yellowlines),

EAFZ:EastAnatolianFaultZone.(c)ASTERimage(bandcombination;R:3,G:2,B:1)showingdextrallydisplacedstreamsalongtheSFZbetweenC¸elikhanBasinandSürgü

Village.(Forinterpretationofthereferencestocolorinthisfigurelegend,thereaderisreferredtothewebversionofthearticle.)
298 A.Koc¸,N.Kaymakcı/JournalofGeodynamics65 (2013) 292–307

northern margin of the Kozaklı Basin (Fig. 6b). Within the zone westernpart,thedifferentsegmentsoftheSFZareeasilyrecog-

of pressure ridges, a number of deflected streams with appar- nizedduetoabruptchangesinelevationonlinearscarpsandcliffs.

entdextraloffsetarealsoobserved(Fig.6c).Maximumobserved Inthisarea,thehightopographyofthesouthernblocktectonically

deflectionsinthestreamcoursesreachupto3km(Fig.6c).Simi- limitsthealluvialplainoftheGöksunandElbistanbasins.Alongthis

larly,displacedstreamsarealsodetectedNWofNurhakandeastof segment,themaincourseoftheSFZisbentgraduallysouthwards

Derbent(Fig.7a).However,thedeflectionpatternismorecomplex (Fig.7c).

and non-uniform, unlike the deflections observed in the Kozaklı Aerialphotographsusedinthisstudyalloweda3Dvisualization

Basin.InthatpartoftheSFZ,someofthestreamchannelsdonot capability and facilitated verification of the detected lineaments

havecleardownstreamcontinuationsandthismaybeduetocon- and geomorphological features observed on the satellite images

tortionofthedrainage.Thisresultsinfanningoutofstreamcourses suchaslonglinearridges(Fig.8a),suddenreliefchanges,stream

thatdonotyieldavisiblechannelcourse.Therefore,themaximum course deflections (Fig. 8b) or truncations (contortions) and dis-

observeddextraldisplacementaroundDerbentisapproximately turbed stream network (Fig. 8c). The pressure ridges (which are

1km(Fig.7a). also shutter ridges along the Kurucaova segment of the SFZ)

Remote sensing analysis also provided information from dif- and the deflected streams in the northern margin of the Koza-

ferent lithologies by processing and enhancement of spectral kli Basin (Fig. 8a) and in the east of Derbent and northwest of

information.Thejuxtapositionofdifferentlithologiesisthediag- Nurhak(Fig.8b)areclearlyvisibleandrecognizableintheaerial

nosticcriterionfordeterminationoffaulttracesandtheiroffset.For photographs and Quickbird images (Fig. 8d) with the deflection

example,anumberofdifferentlithologiesarejuxtaposedalongthe magnitudesjustasobservedontheASTERimages.Moreover,the

centralsegmentoftheSFZonaverysharptraceandresultinavery belt of pressure ridges can be divided into a number of small

prominentcolorcontrastintheASTERimagesduetotheirdiffer- blocks bounded by NE–SW striking en echelon faults with sinis-

ingpetrographyandmineralogy(Fig.7b).Ontheotherhand,atits tral off-set, and displays an anastomosing pattern supporting

Fig.7. OriginalandinterpretedimagesfromSürgüFaultZone.(a)DeflectedstreamsalongtheSFZinaroundDerbentoverlaidonASTERimage.BandcombinationsRGB:5,2,1

withsaturationenhancement(seeFig.2foritslocation)(yellowboxindicatesthepositionofFig.6b).(b)MasterstrandoftheSFZnearSürgüDamindicatedwithwhite

arrowsandoverlaidondecorrelationstretched(DS)ASTERimage.Bandcombinations;RGB:4,2,1.NoteverysharptraceofthemasterstrandoftheSFZ.(c)SubsetofanASTER

imagedepictingaverysharptraceofthewesternpartoftheSFZ(forthesakeofsimplicityfaulttraceisnotdelineatedbutindicatedwitharrows).Theimageisproducedby

DSandPrincipalComponentAnalysis(PCA).Bandcombination;RGBI:5,3,1,intensityisPC-1.(Forinterpretationofthereferencestocolorinthisfigurelegend,thereaderis

referredtothewebversionofthearticle.)
A.Koc¸,N.Kaymakcı/JournalofGeodynamics65 (2013) 292–307 299

Fig.7. (Continued).
300 A.Koc¸,N.Kaymakcı/JournalofGeodynamics65 (2013) 292–307

clockwise block rotations along the dextral Kurucaova segment movementoftheSFZandmayindicatepaleotectonicmovement

(Fig.8a). sense of the fault zone. This has further implications, such that

In the west, relief information extracted from the aerial pho- duringthepaleotectonicperiodthefaultzonewasalsoadextral

tographsindicatesasuddenelevationchangeandabuttingofthe strike-slipfaultzonethatreactivatedduringtheneotectonicperiod

southern block of the SFZ to the alluvial plain of Göksun Basin co-axiallyoritkeptitsslipsensesincethen.

(Fig.8c).Thissectionischaracterizedbythesharpnorthdipping Thehostlithologiesofthecollectedfaultslipdatarangefrom

mainstrandoftheSFZandanumberofNE–SWtrendingen-echelon PaleozoictoMesozoicmarblesandmetamorphics,toLateCreta-

folds.Sincethesefoldsweredevelopedwithinpre-Neogeneunits ceousophiolitesandophioliterelatedunits,toPaleocenevolcanic

which pre-date the SFZ, they are not taken into consideration, andclasticunits,andtoNeogenesedimentaryandvolcanicunits

even though they have compatible orientations with the dextral (Fig.3).Thefaultslipdataonthepre-Cenozoicunitsmaybelong

Fig.8. OriginalaninterpretedimagesfromSürgüFaultZone.(a)Aerialphotoshowingpressureridgeswithinananastomosingpatternoffaults(red)anddextrallydisplaced

streamcourses(blue).EAFZ:EastAnatolianFaultZone.Notethatallthestreamsflowsouthwards.(b)DeflectedstreamsinEofDerbentandNWofNurhakoverlaidonthe

aerialphoto(seeFig.5bforitslocation).(c)Aerialphotoshowingwesternpartofthestudyarea.MainstrandoftheSFZisdippingnorthwardsandisindicatedwithred

arrows.Singlyplunginganticlinesandsynclinesareindicatedwithyellowlines.Divergentwhitearrowsarealluvialfans.(d)Quickbirdimage(obtainedfromGoogleEarth)

indicatingdextrallydeflectedstream.(Forinterpretationofthereferencestocolorinthisfigurelegend,thereaderisreferredtothewebversionofthearticle.)
A.Koc¸,N.Kaymakcı/JournalofGeodynamics65 (2013) 292–307 301

Fig.8. (Continued).

tobothpastandpresentdeformationphases.However,adjacent (oblique) in all sites except sites 9 and 19 (Fig. 9a) where (cid:2) is
1

Quaternary basins partly juxtaposed by the fault itself indicate vertical.Thisischaracteristicfortriaxialstressconditionswhere
currentacti vitytha tiscon sistentwith th esli pdata .Fore xample, ˚ value s are cl ose to 0.5 (Ta ble 1). In ad dition , oblique o rienta-

thefaultzonethrustovertheQuaternaryunitsclosetowesternend tions of principal stresses characterize a triaxial strain condition

(nearsites1–4),aroundSEofGöksun(Fig.5).Similarly,thefault thatdeviatesgreatlyfromAndersonian(Anderson,1951)typesof

juxtaposestheQuaternaryunitslaterallyalongtheKurucaovaseg- faults(Reches,1978,1983;Krantz,1988).

mentwherethefaultplanedisplaysclearstriations.Basedonthese Thehorizontalcomponentsoftheconstructedstressconfigura-

observations,faultslipdatacollectedfromfreshsurfacesofthefault tionsareplottedinordertounderstandthestyleofdeformation

plane,incontactwithQuaternarydeposits,havebeenassociated and to check compatibility of the constructed principal stress

withthelatestphaseofdeformationalongtheSürgüFaultZone. directions, and to assess the nature of local and regional struc-

ExtractedstressconfigurationsshowninFig.9andTable1indi- tures.Apartfromsomeextensionalsolutions(sites9and19),the
catethatthe major principalstress ((cid:2) )is ge nera ll yori ented ( sub-) horizo ntalco mpo nento fmostofthe (cid:2) directi onsat ea chsi tem ake
1 1
horiz onta lly, where as(cid:2) an d(cid:2) a rein te rchangeab lysub-v ertical anapproxi mately45◦a ng lewi th the localtrendof th eSFZ and they
2 3