Long-term evolution of the North Anatolian Fault

22 Pages·2009·1.38 MB·English

Long-term evolution of the North Anatolian Fault:
new constraints from its eastern termination
AURE´LIAHUBERT-FERRARI1,*,GEOFFREYKING2,JE´ROMEVANDERWOERD3,
IGORVILLA4,ERHANALTUNEL5&ROLANDOARMIJO2
1SectiondeSismologie,ObservatoireRoyaldeBelgique,ruecirculaire3,
B-1180Brussels,Belgium
2LaboratoiredeTectonique,InstitutdePhysiqueduGlobedeParis,UMR,4placeJussieu,
Paris,75252Cedex05,France
3IPGS-EOST,UMRCNRS/ULP7516,5,rueReneDescartes,
Strasbourg,67084Cedex,France
4InstituteofGeologicalSciences,UniversityofBern,Baltzerstrasse1-3,
CH-3012Bern,Switzerland
5Dept.ofGeology,EngineeringFaculty,OsmangaziUniversity,Eskisehir,Turkey
*Correspondingauthor(e-mail:[email protected])
Abstract: Thedeformationand40Ar–39Ardatingofrecentvolcanism,thatremarkablysitsacross
theNorthAnatolianFaulteasternterminationinTurkey,togetherwithpreviousstudies,putstrong
constraintsonthelong-termevolutionofthefault.Wearguethatafterafirstphaseof10Ma,
characterizedbyasliprateofabout3mm/a,andduringwhichmostofthetracewasestablished,
theslipratejumpedtoabout20mm/aonaverageoverthelast2.5Ma,withoutsubstantialincrease
ofthefaultlength.Thetransitioncorrelateswithachangeinthegeometryatthejunctionwiththe
EastAnatolianFaultthatmakestheextrusionprocessmoreefficient.
The right-lateral North Anatolian Fault (NAF), narrow zone and that the internal deformation of
together with the conjugate East Anatolian Fault Anatolia though existing (Tatar et al. 1996;
(EAF), accommodates the westward extrusion of Gu¨rsoyetal.1997;Jaffeyetal.2004)isnegligible
theAnatolianblocktowardtheAegeanSubduction (Fig.1).ThepresentgeodeticsliprateoftheNorth
Zone (Fig. 1; McKenzie 1972; Tapponnier 1977). Anatolian Fault (22+3mm/a: McClusky et al.
This process started most probably 12Ma ago (2000); 24+1mm/a: Reilinger et al. (2006)
during a late phase of collision between Arabia is not significantly different from its Holocene
and Eurasia (Dewey et al. 1986; McQuarrie et al. slip rate (18.5+3.5mm/a; Hubert-Ferrari et al.
2003) characterized by the uplift of the Anatolian (2002)) deduced from offset geomorphological
Plateau, the end of marine sedimentation (Gelati markers. The study of the offset morphology at a
1975; S¸engo¨r et al. 1985), the onset of volcanism wide range of scales (Hubert-Ferrari et al. 2002)
in eastern Anatolia (Yılmaz et al. 1987; Pearce suggests that deformation has remained localized
et al. 1990) and the onset of motion of the North along the present fault zone for several million
Anatolian Fault (S¸engo¨r et al. 1985; Barka 1992). years. Barka & Hancock (1984) further suggest
Indeed biostratigraphic data unequivocally con- that a broad right-lateral shear zone was existing
strain a Late Miocene age for all basins located beforedeformationfullylocalizedinearlyPliocene
along the North Anatolian eastern strand (see time on the present strand of the North Anatolian
S¸engo¨r et al. (2005) for a review). Some still Fault. The present North Anatolian Fault has also
propose a later initiation time around 5+2Ma a nearly uniform total displacement of c. 85km
(Barka&Kadinsky-Cade1988;Bozkurt&Koc¸yigˇit along most of the fault (Armijo et al. 1999;
1996;Bozhurt2001).Thepresent-daykinematicsof Bozkurt 2001; Westaway & Aeger 2001; Hubert-
the extrusion, constrained by GPS measurements Ferrarietal.2002;S¸engo¨retal.2005)andisthus
(McClusky et al. 2000; Reilinger et al. 2006), similartoatransformboundary.Thetotaldisplace-
shows that deformation is localized along a single mentoftheNorthAnatolianFault,togetherwiththe
From:VANHINSBERGEN,D.J.J.,EDWARDS,M.A.&GOVERS,R.(eds)CollisionandCollapseatthe
Africa–Arabia–EurasiaSubductionZone.TheGeologicalSociety,London,SpecialPublications,311,133–154.
DOI:10.1144/SP311.5 0305-8719/09/$15.00#TheGeologicalSocietyofLondon2009.
134 A.HUBERT-FERRARIETAL.
Fig.1. ContinentalextrusionoftheAnatolianblockawayfromtheArabia–Eurasiacollisionzone.ThecurrentGPS
vectorsrelativetoEurasiaareindicated(McCluskyetal.2000).NAF,NorthAnatolianFault;EAF,EastAnatolian
Fault;DSF,DeadSeaFault;ASZ,AegeanSubductionZone.BoxisareaofFig.2.
ageofthefault(12Ma),yieldsanaveragegeologi- (Hubert-Ferrari et al. 2002). East of the Erzincan
calsliprateof7mm/a. basin a second strait segment extends for 80km
WefocusontheKarliovaTripleJunctionarea, with a N1108E strike to a small pull-apart near
wheretheeasternextremityoftheNorthAnatolian Yedisu. East of Yedisu, the faulting geometry is
Fault joins the East Anatolian Fault. This pivotal typical of a damage fault pattern occurring at the
regionmarksthetransitionbetweenthecontinental tip of strike-slip fault with slightly more diffuse
shortening to the east and the extrusion regime to deformation combining fault branching, horsetail
the west. In addition recent volcanism covers and reverse faulting (Kim & Sanderson 2006). A
entirelytheregionandprovidesidealchronological third segment of the North Anatolian Fault splits,
markers to record deformation. By mapping the about 10km SE of Yedisu, in different curved
activefaultsandtheiroffsets,andbycharacterizing strands that ruptured in 1949 (Ambraseys 1988).
therelationshipbetweenfaultingandvolcanism,we This segment forms a large horsetail with normal
proposethattheextrusionprocesshasevolvedwith faulting deforming the eastern flank of the Turna
time, with two distinct phases characterized by Mountain until the East Anatolian Fault. Farther
very different slip rates. Interestingly, the Triple NE, a fourth segment extends over 30km to the
Junction (TJ) evolution can be approximated by a Triple Junction and accommodates almost only
simpleplate-tectonicmodel. strike-slip motion as shown in Figure 3 and by
focal mechanisms of earthquake of magnitude
M.5.5 (Fig. 2). The third and fourth segments
ActivefaultingattheAnatolia–Eurasia– formarestrainingstep-over.Secondaryfoldingpar-
Arabiatriplejunction alleltothePeric¸ayRiveroccursjustnorthofthelast
segmentoftheNorthAnatolianFault.
We have established a detailed map of the three EastoftheTripleJunctiontheVartofaultsystem
mainfaultsystems(theNorthAnatolianFault,the extendsover50km,formingalargemostlyexten-
VartoFault,andtheEastAnatolianFault)relevant sional horsetail. Most of the deformation is loca-
to the triple junction deformation combining Spot lized on the Main Varto Fault that is in strait
imagesanalysisandfieldwork(Figs2–5). continuation of the fourth segment of the North
At its eastern extremity the North Anatolian Anatolian Fault. This main strand, located exactly
Fault can be divided in 4 main segments (Fig. 2). atthefootoftheBingo¨lhalf-caldera,accommodates
Tothewest,afirstsegmentoftheNorthAnatolian mostlystrike-slipfaultingthoughpartlyhiddenby
FaultstrikesN1258Eandendsattheeasternextre- landslides (Fig. 4). In 1966, the Varto M 6.8
¼
mity of the Erzincan basin. This is a complex earthquake (Wallace 1968; Ambraseys & Zatopek
basin (Barka & Gu¨len 1989; Fuenzelida et al. 1968) ruptured its eastern part with aftershocks
1997; Hubert-Ferrari et al. 2002), with the having thrusting mechanism. More diffuse strike-
left-lateral Ovacık fault terminating southward slip and normal deformation exists south of the
(Westaway & Aeger 2001). The seismic behavior MainVartoFault,withaclearsouthwarddecreasing
of the North Anatolian Fault appears to be gradientofdeformation.Thenetworkofsecondary
decoupledonbothsidesofthismajordiscontinuity faults in the Varto horsetail is at a slight angle to
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Fig.2. TheAnatolia/Eurasia/ArabiaTripleJunction:presentfaultgeometry,seismicity(focalmechanismsandearthquakeruptures),volcanismandsedimentarybasins
(seelocationinFig.3).BoxesareareasofFigures3–7.TotaloffsetontheEastAnatolianFault(EAF)constrainedby20+5kmoffsetofametamorphicbodybounded
byMiocenesedimentsandvolcanism(S¸arogˇluetal.1992).
1
3
5
136 A.HUBERT-FERRARIETAL.
Fig.3. Right-laterallyoffsetmorphologyalongeasternmostsegmentoftheNorthAnatolianFault(seelocationin
Fig.2).Top:Spotimage.Bottom:Interpretationconfirmedbyfieldwork,showingriveroffsetsreaching3.7km,and
rivercaptures(offsetsdande).
the Main Varto Fault; most splay from the 1972). The recent M 6.4 earthquake in May
Triple Junction, though some splay from the East 2003 ruptured a mino¼r conjugate fault (O¨rgu¨lu¨
Anatolian Fault just SE of the town of Karliova et al. 2003), probably related to the major change
(Fig. 6). The Varto horsetail is also associated instrikeoftheEastAnatolianFaultnearthetown
with fissure-fed lava flows and intrusion located of Bingo¨l (Figs 1 & 4). Near the town of Goynuk
mostly along faults. The largest intrusions form the East Anatolian Fault forms a small short-cut
significantvolcanicdomeselongatedalongbound- pull-apart associated with lacustrine sediments
ing faults (Figs 4 & 5). South of the town of intercalated with lavas ofthe Turna Mountainand
Varto the fissural volcanism cross-cuts older withlignitedeposits(Fig.7).
volcanicproductrelatedtotheBingo¨lhalf-caldera
(Buket & Go¨rmu¨s¸ 1986; Buket & Temel 1998).
Significant shortening in the Triple Junction area RecentvolcanismattheAnatolia–Eurasia–
occurs only 20km south of Varto along the Mus¸ ArabiaTripleJunction
fold-and-thrust belt (Fig. 2; S¸engo¨r et al. 1985;
Deweyetal.1986). ThemostsalientfeatureoftheTripleJunctionisthe
AttheTripleJunction,theEastAnatolianfault presence of widespread recent volcanism (Figs 2,
ends against the North Anatolian and Main Varto 6a; Dewey et al. 1986) that has spectacularly
Fault systems. Its last 75km segment smoothly recordedthecumulateddeformation.
bendseastwardasitapproachestheTripleJunction. AlongtheNorthAnatolianFault,weareableto
ItrupturednearBingo¨lduringaM 6.9earthquake reconstructasinglevolcanicedificefromtwooffset
¼
in1971(Arpat&S¸arogˇlu1972;Seymen&Aydın, structures (Fig. 6). The first structure, neatly cut
EVOLUTIONOFTHENORTHANATOLIANFAULT 137
Fig.4. DeformationsplayingeastofKarliovaTripleJunctionformingthelargeVartohorsetail(seelocationinFig.2).
MainVartoFaultatthefootoftheBingo¨lCalderaaccommodatesmainlyright-lateraldeformationwithathrusting
componentatitseasternextremity.Secondaryright-lateralandnormaldeformationassociatedwithvolcanic
domesoccurstosouth.Top:Spotimage.Bottom:Interpretationconfirmedbyfieldwork.Inset:beheaded
drainagesystemalongtheMainVartofaultconfirmingright-lateralmotion.
tothesouthbytheMainVartoFault,istheBingo¨l Both structures are composed of volcanic rocks
half-calderaeastofKarliova.Thesecondstructure, having similar stratigraphic ages (Yılmaz et al.
cuttothenorthbytheNorthAnatolianFault,isthe 1987; S¸arogˇlu & Yılmaz 1987, 1991). We can
semi-circular Turna Mountain west of Karliova. restorethepositionoftheTurnaMountainopposite
138 A.HUBERT-FERRARIETAL.
Fig.5. PhotosofthevolcanicdomesassociatedwiththeVartoFaultsystem(viewpointsinFig.4).
totheBingo¨lhalf-calderabyaleft-lateraldisplace- variable amounts of aqueous high- and low-
ment of 50km along the mean direction of the temperature alteration, especially of the ground-
North Anatolian and Main Varto Fault systems mass. Geologically meaningful results have been
(Fig. 6b). As a result a volcano with a nearly reported in spite of the alteration (e.g. Fleming
conical morphology can be reconstructed. The etal.(1997)andreferencestherein).Inthepresent
caldera palaeo-topographyalong the NorthAnato- work we will show that consistent results can be
lianFaulthasbeenstronglymodifiedbystrike-slip obtainedfromwholerocksamplesbythedeconvo-
faulting and related enhanced erosion. Secondary lutionoftheleastalteredAr-bearingphasesfromthe
normal faulting affecting the Turna half-caldera alterationproductsusingtheCa–KandCl–Kratios
(Fig.6c)hasalsoalteredtheinitialvolcanicstruc- derivedfromArisotopesystematic(seeVillaetal.
ture. Despite the alterated original morphology, 2000).Tounraveltheeffectsofalteration,themost
the reconstructed volcanic topography excludes reliable criterion is a low Cl–K ratio, as Cl is
any significant relative long-term vertical move- observedtobecharacteristicallyhighinsecondary
ment across the North Anatolian Fault. Indeed the minerals. Steps having a constant and low Cl/K
topographicprofileinFigure5cacrosstheTurna/ signature(whichusuallycoincideswithaconstant
Bingo¨l volcano shows a coherent triangular shape and low Ca–K ratio, typical of groundmass) are
which centre location is nearly identical to the termed ‘isochemical’ and used to calculate a
centre location of the Bingo¨l half caldera as weighted average age. In two cases, no constant
definedbyitssummitalshape. chemicalratioswereobtained,butCl–Kratioscor-
The age of the volcanism around the Karliova relatewithage,sothatweperformedaregressionto
TripleJunctionisconstrainedby40Ar–39Ardating zerochlorine(seeFig.8).
(Figs7,8&Tables1and2).40Ar–39Arageswere ThefactthatlavasformingtheTurnaMountains
obtained on groundmass samples of lavas, with K andtheBingo¨lhalf-calderahavesimilarages(Figs7
concentrations ranging from 0.8% to 3.3%. As in & 8) but distinct from the surrounding volcanism
practicallyallterrestrialbasalts,oursamplesshow supports the morphological restoration of the
EVOLUTIONOFTHENORTHANATOLIANFAULT 139
Fig.6. Volcanoreconstructionbya50kmleft-lateraldisplacementalongNorthAnatolianandMainVartoFault
systems(seelocationinFig.2).(a)PresentmorphologyofthejunctionoftheNorthandEastAnatolianFaultswith
activefaultsinblackandvolcanism.Thicklines:mainfaults;thinlines:secondaryfaults;lineswithticks:normal
motioncomponent.(b)Afterrestorationof50km,theTurnaandBingo¨lmountainsareputinfrontofeachother,
reconstructingasinglevolcanicedifice.Volcanopalaeo-topographyisstronglymodifiedalongtheNorthAnatolianand
MainVartoFaultsystems.OnitsSEflank,normalfaultingalsodeformsthetopography.ThesomitalshapeoftheBingo¨l
half-calderahasanellipticalshapereflectingaslightelongationofthevolcanoinaNW–SEdirection.(c)Topographic
profileacrosstherestoredvolcano.Thelocationofvolcanocenterextrapolatingupwardthevolcanoflanksisnearly
identicaltotheonederivedfromthesomitalshapeoftheBingo¨lhalfcalderashowingthatlong-termupliftacrossthe
NorthAnatolianFaultisnegligible.
caldera. The Turna Ar–Ar age of 2.85+0.05Ma (Chataigner et al. 1998; Poidevin 1998; Bigazzi
(sample Tu1 in Fig. 8c coherent with sample Tu2 et al. 1998). The Bingo¨l half-caldera lies to the
in Figs 8c & d) precisely matches the ages of the NW on the 6.9 to 5.6Ma old volcanism of the
Bingo¨l half-caldera (samples Bi1: 3.13+0.09 Arasvalley(Innocentietal.1982a)andtotheNE
Ma, Bi2: minimum age 3.11+0.33Ma, Bi3: on the 8.3 to 6.0Ma old Erzurum volcanism
3.1+0.29Ma in Figs 8a & b); these ages are [8.3+0.1Ma to 6.0+0.3Ma (Innocenti et al.
coincident with, and are more reliable than, the 1982a); 6.9+0.32 (Bigazzi et al. 1994);
whole-rock K–Ar ages obtained by Pearce et al. 6.83+0.36 (Bigazzi et al. 1997); 8.4+0.2Ma
(1990) (see Fig. 7). Both half calderas rest on top (Chataigneretal.1998)].Onthecontrarythevol-
of older volcanic rocks (Figs 2 & 7). The Turna canism south of the Main Varto Fault is more
volcanismliesonthe7.3to4.1MaoldSolhanfor- recent than the Bingo¨l half-caldera as attested by
mation(seeFig.7,andsampleSo1inFig.8f).The fissure-fed lava flows and fault-related intrusions
ageofthisformationisquitewellconstrainednear cross-cutting Bingo¨l related volcanic products
the East Anatolian Fault because its volcanism (Buket & Go¨rmu¨s¸ 1986; Buket & Temel 1998).
was an obsidian source during prehistoric time The latter is also supported by 40Ar–39Ar dating
140 A.HUBERT-FERRARIETAL.
Fig.7. Detailmappingofvolcanismatthetriplejunctionwithlocationofvolcanicsamplesandages(seelocationin
Fig.2,agespectrainFig.8,andgeochemicalcompositioninTable1).MappingoftheTurnaandBingo¨lvolcanismdone
combiningfieldwork,Landsatimages,andreinterpretedpublishedgeologicalmaps(Altinli1961;Bingo¨letal.1989;
Tarhan1993,1994;Buket&Temel1998;Herece&Akay2003).LocationsofsamplesofPearceetal.(1990),Buket&
Temel(1998),Poitevin(1998)usedinFig.9areshown.SamplesfromBingo¨lMt.(Bi1:3.1+0.09Ma;Bi2:min.age
3.1Ma;Bi3:3.1+0.3Ma)andTurnaMt.(Tu1:2.88+0.06Ma;Tu2:2.323.9Ma)showsimilar40Ar–39Arages,
whileSohlanvolcanismsouthofTurnaMt.(So1:5.39+0.12Ma)isolderandfissuralVartovolcanismisyounger
(Va1andVa2sampledatthebaseofthedomesalongincisedrivervalleyhaveagesof2.6+0.12,2.2+0.23Ma
respectively,whereasVa3andVa4sampledontheflankofthedomeshaveagesof0.46+0.24Maand0.73+0.4Ma
respectively).Agesobtainedarecoherentwithotherpublished40Ar–39Ar,K–Ar,andfissiontrackages.
(Fig.8)withsamplestakenatthebaseofandonthe volcanic domes are 0.46+0.24Ma and
twomainvolcanicdomesrelatedtotheVartohorse- 0.73+0.39Ma old (Fig. 8g and h). Those ages
tail(Fig.4).The40Ar–39Arages(Fig.8),although are coherent with ages of fissure volcanisms
oflowerprecision,indicatesthatvolcanismsouthof further south along the Murat river across the
the Bingo¨l half caldera started 2.2+0.23 to Mus¸ fold-and-thrust belt (Fig. 7; Bigazzi et al.
2.6+0.12Maago(Fig.8e)andthatthetwomain 1996,1998).
EVOLUTIONOFTHENORTHANATOLIANFAULT 141
(a) (b)
(AMgae) Bi1, isochemical age is 3.13 ±0.09 Ma Age Bi2,zeroCl minimum age is 3.11 ± 0.33
Bi2, minimum age is 3.11 ± 0.33 (Ma)
88 Bi3, isochemical age 3.1 ± 0.29 Ma
8
66 6
44 4
22 2
0
000 20 40 60 80 % 39 Ar100 0 0,0005 0,001 0,0015 Cl/K 0,002
(c) (d)
Age
(AMgae) TTuu21,, aislotecrhaetmionicsa bl augt ea g2e.8 i8n± t0h.e0 6r aMnage of 2.3-3.9 Ma (Ma) TTuu21,,
8 5 alteration trend
6
4 3
2
1
0 0 0.001 Cl/K 0.002
0 20 40 60 80 % 39 Ar100
(e) (f)
Age
Age (Ma) So1, isochemical age is 5.39±0.12 Ma
(Ma) Va1, isochemical age is 2.60 ± 0.12 Ma 8
8 Va2, isochemical age is 2.22 ± 0.23 Ma
6
6
4
4
2 2
0
00 20 40 60 80 % 39 Ar 100 0 20 40 60 80 % 39 Ar 100
(g) (h)
Age Age Va4,Zero-Caregression age is 0.46 ±0.24
(Ma) Va3,Cl/K-Zero-Caregression age is 0.46 ±0.24 (Ma)
8 Va4, isochemical age is 0.73 ±0.39 Ma 3
6
2
4
2 1
0 0
0 20 40 60 80 % 39 Ar 100 0 2 4 6 8 10 12 Ca/K 14
Fig.8. 40Ar–39Ardatingagespectraforlavasnearthetriplejunction(seesamplelocationsinFig.7anddatainTable
2).AnalyticalproceduresofthestepwizeheatingexactlyfollowedtheonesdetailedinVillaetal.(2000).(a)Age
spectrumforsampleBi1,Bi2,Bi3;Bi1isochemicalageis3.13+0.09Ma(1sigmaerror)usingsteps5–7havingCl–K
ratio,0.0046;Bi2zeroClminimumageis3.11+0.33Ma;forBi3,steps3and4,havingCl–Kratio,0.0052and
Ca–Kratio,3,defineanisochemicalageof3.11+0.29Ma.(b)Three-isotopecorrelationplotforBi2;thezero-Cl
minimumageis3.11+0.33Mausingaregressiononsteps1–5.(c)AgespectrumforsampleTU1andTU2;TU1
isochemicalageis2.88+0.06Mausingsteps4–7havingCl–Kratio,0.00015.(d)Three-isotopecorrelationplotfor
TU1andTU2.Theusualcriteria(lowCl–KandCa–Kratios)producenosimplepatternforTU2.Steps3–6with
relativelylowCl–Kratiohaveagesintherange2.3–3.9Ma.ComparisonwithlessalteredTU1,andwithothermore
alteredsamplesoftheNorthAnatolianFaultsuite,suggeststhattwodistinctalterationepisodesarerecorded,both
revealedbyhighCl–Kratios.Zero-Clextrapolationsofthetwotrendsarecompatiblewiththe2.85MaageofTU1.(e)
AgespectrumforsamplesVa1andVa2.ForVa2,theCa–Kratiosarebimodallydistributedandrequiretwophases;the
isochemicalage,calculatedontheK-richsteps1–4,is2.22+0.23Ma.ForVa1,theisochemicalageonsteps1–6,
havingCl–Kratio,0.008,is2.60+ 0.12Ma.(f)AgespectrumforsampleSO1.Theisochemicalageis
5.39+0.12Maonsteps2–7.(g)AgespectrumforsamplesVa3andVa4.TheVa4isochemicalageis0.73+0.39Ma
onsteps1–4.(h)Three-isotopecorrelationplotforsampleVa3.Thezero-Caregressionageis0.46+0.24Mausing
steps2–5.BothVa3andVa4samplesrobustlydefineanage ,1MaforthelatestphaseofVartofissuralvolcanism
southofBingo¨lhalf-caldera.
FinallytheBingo¨l/Turnalavashaveanundistin- rocks form a well defined trend from basaltic
guishablegeochemistryconsideringmajorortrace trachy-andesitetotherhyolitefield,andcanbecon-
elements, quite distinctive from the surrounding sideredtobetransitionalbetweensub-alkalineand
volcanism. In total alkali versus SiO diagram mildlyalkalineincharacter.Themorerecentdyke
2
(Fig. 9a & Table 1) the Bingo¨l/Turna volcanic volcanismjustsouthoftheBingo¨lHalfCalderais
142 A.HUBERT-FERRARIETAL.
BinBugkoetl eMt Tte.m veol l(c19. 9:8) 140
Pearce et al. (1990)
10 Turna Mt. volc. : 120
Varto fissural volc. :
NaO+KO) wt. %22 68 SPooBwsiCAsesoutlooeeaahlukauussvtettaattitthetn khhoon p e m effomet tttv feT hhe aTeoteetlaum.a l. EEr .c(b neAA1b.o l9 oFFM :(d,,9d1ty89y.)9:8) Ni ppm146800000
( 4 east of EAF (Goynuk) 20
east of EAF(Karliova)
Poitevin et al. (1998):
east of EAF (Cavular- 0
2 Orta Duz) 0 50 100 150 200 250 300 350Cr ppm
40 50 60 70 80 SiO2 wt. %
2 200
%1,5 ppm150
wt. Rb
O 2 1 100
Ti
0,5 50
0 0
40 50 60 70 80 SiO2 wt. % 0 100 200 300 400 500 600 Sr ppm
140
18
120
16 100
% m
O wt. 2 14 Ni pp 6800
Al2 12
40
10
20
8
40 50 60 70 80 SiO2 wt. % 0 20 30 40 50 60 Y ppm
0,5
5
0,4
4
PO wt. %2300,,23 KO wt. %223
0,1 1
0 0 0
40 50 60 70 80 SiO2 wt. % 50 100 150 200 250Rb ppm
600
500
400
m
pp300
Sr
200
100
0
0 20 40 60 80
Mg*100/(Mg+Fe) molar ratio
Fig.9. Plotofsomemajor,minorandtraceelementsforsampleslocatedinFigure7.DatashowthattheBingo¨land
Turnavolcanismsaresimilar,whereasthevolcanismssouthoftheBingo¨lhalf-calderaandalongtheEastAnatolian
Faulthavedifferentcharacteristics.VolcanismsouthofthemetamorphicbodymappedinFigure7oneithersideofthe
EastAnatolianFaultisidenticalconfirmingatotaloffsetof20 + 5kmontheEastAnatolianFaultandanactivation