commercial purposesinaccordancewithWileyTermsandConditionsforSelf-Archiving continental plate",whichhasbeenpublishedinfinalformatDOI:10.1111/jmg.12304.Thisarticlemaybeusedfornon- This isthepre-peerreviewedversionoffollowingarticle:"Metamorphiczoningandbehaviouranunderthrusting This article isThis article by protected copyright. All rights reserved. 10.1111/jmg.12304 doi: to differences between lead the of thisversion citethisarticle and asVersion Record.Please copyediting, paginationbeen throughthe andproofreadingtypesetting, process,may which This article acceptedhas been for publication andundergone fullpeer review buthasnot words:Key fluidsthehydrous into crust. metamorphic thatfacilitates recrystallization entry of the is largelycoupled todeformation recrystallization first at elevated that temperatures and amphibolite-facies) (middle crustthat the relatively is dry,competent, and responds metamorphic bysignificant differs continental oforogenic systemsplate inmetamorphic character in from parts other ofEarth’s collisionalpart systems. Thedata petrophysical rheology, properties, and distribution inanelsewhere of inaccessible volatiles The exposed provides section potential forincreasingunderstanding of the thermal evolution, metamorphic gradient field athighertemperatures andP/Tthantheclassical Barrovian style. described prograde metamorphismthrough The decompression. investigated is and section the first terrane eclogite-bearing which records more metamorphic protracted recrystallization both an startedfirst at that advanced stage ofcollision, at underthrusting underwent metamorphic short-lived plate recrystallization anddeformation deformation metamorphic andpartial melting. The record rocks that, byandlarge, the underthrusting essentiallystructurally plate remained coherent highly despite ductile transition demonstrates that, terrane, withthe the exception of eclogite-bearing the beneath The lithotectonic the overridingjust contact the gradual of plate. metamorphic underthrusting plate and back extruded the along interface withoverlying the occurs crust, depth. Aneclogite-bearing terrane, tectonic detached edge from leading the ofthe granul high-pressure (550 facies metamorphic recrystallization atis first recorded conditions of tomiddle lower amphibolite- continental platelower define metamorphic aregional zoning zones. by eight Significant assemblages Fe- in granulite-facies.Metamorphictransition from unmetamorphosed tohigh-pressure underthrustingof plate,composed igneous lower Proterozoic protoliths, exposes gradual the coherentbelt A200kmorogeny. structurally ofthemid- wide continental metamorphicplate that records the and evolution duringcollisional behaviour OrogenScandinavia Sveconorwegianin billion-year-old exposes anunderthrustinglower by one- inferred geophysical Bysurveying. margin oftheeroded contrast,theeastern deeply platesLower continental ofcollision arenormallyzones properties andtheir inaccessible ABSTRACT Short title: [email protected] 2 [email protected] 1 MöllerCharlotte plate Metamorphic zoning and behaviour ofan underthrusting continental

Accepted ArticleGeological 28Uppsala, SurveyofSweden, Sweden; Box670,SE-751 Sölvegatan 12, Department ofGeology, LundUniversity, in situ – An exposed underthrustingAn exposed successively with contact 600 °C),progressing towards the plate the upper to collision, Sveconorwegian, collision, partial granulite,eclogite, metagabbro melting,

1* exposure of lower acoherentunderthrusting continental plate, and defines a

Ti and Jenny Andersson ite -rich metagabbro-rich inacontinuous ~120kmwide acrossthe transect -facies ~850-facies at °Cand10 continental plate 2 demonstrate – 11 kbar, the latter the11 kbar, latter corresponding to~40 km c . 980 that lower theunderthrusting – SE 970 Ma; this contrast970 Ma; isin the to -223 62Lund,Sweden; -223 to upper levelsto upper ofthe This article isThis article by protected copyright. All rights reserved. continental marginPalaeoproterozoic meta and sequence areexposed thethat along f GeeRoberts, Solli,2013 & published as basement andcover of structure WGR are Proterozoic window &Zachrisson, Stephens, tectonostratigraphic level Scandinavian Caledonides, Proterozoic become 2008 Grenville lev thincrustal Lundin Bi orogencollisional formed during Theorogens. Sveconorwegian deeply 2012 am (dry), The metamorphic stateof plate theIndian lower Ti and southern 2009) al., McKenzie, lower (Searle, Sequence bythepresencecorroborated ofleucograniteand migmatite in Gre the meltUnsworth etal.,2005),and interpreted as melt Schulmann, dynamic ofentire orogens evolution & Wernicke properties Himalaya thermalthe andrheologyofmiddle state anddeep crust sentenceThe introductory ofSchulte (Schulte beneath the Himalaya and Tibetan the plateau.” “The rocks of Indian subcontinent the are last oftheGangesbefore seen south 1 | ngen, Accepted Article INTRODUCTION els exposed. ). ; Hetényial.,2007; et plate is

, 2015 eroded Precambrian shieldsoffer

- detached, thrust, detached, Andersson, Andersson, in the hinterland in the Pelkum etal. phibolite , . G

O

and of however - & Priestley

rogen, andshare skinned nappes have been excised nappeshavebeenexcised skinned and leaving eroded, mid the rocks , 2011 2011). Seismic low eophysical dataeophysical Figures 1 Figures the the ). Theremnants ofthisorogenare present in a upper 500 kmbelt, inwhich wide In collisional orogens, In collisional orogens, the upper exposeWhile youngorogens thickorogenicprismsfar and interpreted as Tibet

bet isbet essentially (Zhao, intact WGR is Th Indian lower crust

that - Cottle, Streule, ), because - e Sveconorwegianorogenic

, weakened crust capable of highlweakened crustcapableof (wet), oreclogite ,

Söderlund, &Möller units not coherent must be

, w

, 2004

and 2005)

ere complex with

1985) s and inserted intotheand inserted and famous for its eclogiteand famousoccurrences, forits (

cf. and in and in ) 4 inKrogh Schulte

ront zoneront

. deeply buriedduring rigid, supporting elevationthe of(Jackson Tibet s

indicate that the plateIndian lower beneath the Himalayan prism

t ;

assessed byindirect methods, i.e. he Similarly i similar first m Jackson, . The Western Gneiss Region Gneiss . TheWestern O - aps

- velocity regions under the the plateauregions havebeenvelocity under Tibetan rogen in the Baltic inthe Shieldrogen (Scandinavia) anexample is ofa deep

enhanced exhumationmid of the with the the a & -

Pelkum etal. are compile

Waters - (e.g., Jamieson(e.g., - 1 Gaassembly of form facies Pelkum (2005) illustrates etal. that

, Kamo, Terry, Robinson,, Kamo, &Kwok Terry, crust crust llochthon the underthrusting the continentalplatelower tectonic tectonic topics oflong McKenzie, Priestley,McKenzie, ‘ n the basement access to innermost, the access deep , 2008 - order architecture (

an imbricate thrust stack an imbricate

control , d by (very high

20

Grenville Nelson, orogenic prism. Forexample i

parts evolution waswith coeval ofthe that repetition andfoldingtight of a 10). contrast,underthrusting Indian In the ou

; al.,Li et 2008 has , Arne Solli, Arne Solli,

Caledonian Caledonian 20 ’ s s

occurs y ductile y ductile al.,1996; flow et (Nelson

, of

pile pile mechanical behaviour and

05 been alternately interpreted asgranulite Unsworth, Harris, RosenbergUnsworth, Harris, -

standing - & the lower lower the ). density; the the , O

(Gee in this case - Project INDEPTH Team, 1993).

igneous rocks rogen

both in supercontinent Rodinia (

Geological Geological Survey ofNorway (WGR) , Kumpulainen, Roberts, & Emmerson, Möller et et Möller al., 2015 collision -

crustal rocksappears discussion (Copley, geophysical surveying , Craig, Craig, ; Möller, ; Möller,

continental t

he

is dominated by windows

composed , structurally lowest units structurally lowestunits the the the largest the . ater Himalayan - Copley,

- seated levels Large partsofthe

Indian plate beneath

and deep crustal and deep - ( , 2011 Andersson, Dyck, & travelled nappes, in youngorogens e.g.,

at low at 2008; Nábělek et 2008; Nábělek , plate n the 0.5 n the intercalated intercalated Austrheim,

Bethune & they plunge they of a of a & affect ; Robinson,

; Rivers, . The internal basement Jackson, may , & Avouac, Figure 1;

of to be to be s –

. the 0.4 T he

Ga

, -

This article isThis article by protected copyright. All rights reserved. of an MZ,hasyielded the age of 0.99Gafor the 2002 S datedterrane, at 2015 approximately coeval ( high et (Bingen al., Laurent 2008b; etal.,2016 Bamble an et (Bingen al., In 2008b). duringlevels subsequent et (Engvik pressure The oldest metamorphic in event is recorded Kongsberg,Idefjorden, Bamble, and lithotectonic bound segments shearzones: terranes the byductile or Eastern Segment andthe subduction beneaththedipping western Sveconorwegianterranes. Theorogencomprises five or al.,2015,Figure1b) etet accretionary (Coint al., hasbeensetting interpreted as assemblyduring of supercontinent Rodinia al., the (Figure 1a;Liet 2008).Thetectonic The Sveconorwegian 2.1 | 2 | a behave as The metamorphic recordof metamorphic inalowercontinental zoning plate involved i paper presents this andcontinentarc collisional known systems are Earthacross the (Johnson ofbehaviour continental lower plates atorogenic depths migmatite Himalayas. The metamorphic field gradient, the deformation andthe state, distribution of ~ corresponding to deep on structures metamorphismSveconorwegian anddefor Shield ofthe parts Baltic underthrusting intotheincorporated orogenicprism, Eastern the Segment 1c) underthrusting continental plateofthe Sveconorwegian 1995; Davidson, 1997; Bingen et Bingen et al., Söderlund, 2008b; 6 egment

Accepted Article5 REGIONAL .

In contrast - km de ly buried The Sveconorwegian The ). Aneclogite ). pressure amphibolite Rivers etal.,2012

, knownastheMylonite Zone granulite

pth and eclogite provide key dat providekey and eclogite reference d Kongsberg, al., 2016)

distinctly

approaching This paper reportsThis paper onthe Younger metamorphism, deformation, andmigmatization intheIdefjorden metamorphicWhile the characteristics ofprisms orogenic zone insubduction

) crust consistscrust

,

plate to demonstrating

c. Brown, vanGool, &Rivers, 199 Calon, CONTEXT ~

- basement

, to ourknowledge,

- 35 0.98 Ga, have and amphibolite bearing in Eastern terrane the Segment, situated

. itself –

O The differe with 1.07 4 rogen isthe tectoniccounterpart totheGrenville 5

) metamorphismmigmatization at tookplace and

orogenesis . form . km the the

- Bamble Kongsberg and the the The Eastern Segment The Eastern andits continuation in unmetamorphosed

and high O

the Eastern Segment Eastern the of high that nt metamorphic system t ) Telemarkia and Idefjorden terranes, rogen

deep

and either either dou a 200 km transition a 200 –

ha

1.02 Ga granite 1.02 Gagranite magmatismin been identified along Hellström, &Kamo an bly continental thickened crust - s - - seated seated

- facies metamorphismfacies anddeformation grade gneisses hi with since remainedsince they bylater metamorphism unaffected been collisional (Bingen,&Viola,collisional 2008b; Nordgulen, Möller pressure granulite pressure Telemarkia terranes Telemarkia Bingen terranes al(Figure 1c; et eclogite

metamorphic zoningand the firstthe ( MZ ). Eastern parts of parts record Idefjorden). Eastern terrane the detached from underthrust the mation boundary

in the - bearing terrane

Figure 1c;Andersson, documentation eclogite Bamble Kongsberg and a for interpretation ofa forinterpretation the and rheology demonstrates

to high

, terranes probablyterranes resided upper at crustal

from astate 2015), involving east2015), involving of o , 2008a). , 2008a).

- its tectonic contact the with E water the overlyingthe plate. faciesmetamorphism at1.05 O

w

- 1

metamorphism grade rogen ; gh hich represents n continent Indares, 1995; - -

saturated pressure granulite pressure (

~18 kbar,corresponding to

of large that that Th normally inaccessible. are : Telemarkia ( metamorphism andductile essentially unaffected by

properties across across properties the the Easternthe Segment

situated comparable to the is lower in the immediate footwall metamorphism was

an exposureofthe Möller - - continent collision systems. scale coherentin situ ing

O (Möller et et (Möller al., 2015; terranes 1.05 - continental plates dipping ordipping west on either sideon either of Indares Indares & Rivers, rogen andformedrogen &

The at at plate

, Coint et al., Harley, Harley, 2012), – c. & Johansson 1.00 Ga

formerly

1.14 Ga (

, as high 9 and ., – 2008a). 11 kbar, – astern

1.02 Ga (Figure (Figure

-

. -

, –

This article isThis article by protected copyright. All rights reserved. side 1c)(Figure shear.facies Thecorridor immediately west oftheS depth, likely within deformation zones deformation Front Sveconorwegian rocks rocks in remnants ofsedimentary continent >200 km east, asevidenced farther bysub orogeny, Sveconorwegian DeformationFrontal Wahlgren, Zoneof Cruden, andStephens (1994)] alongthesteeplywestlocated At 2.2.2 Johansson, ( metamorphismpressure southernmost Shield, Baltic including southernSegment, the Eastern also records ( gabbro Andersson, 2015). Mesoproterozoic intrusions are subordinate Baero mafic andsubordinate monzodiorite, and rocks meta composed granite (dominantly), to of granodiorite Belt Igneous The Eastern Segment is 2.2.1 2.2 | 2009).Brueckner, ofgranite, norite,plutons andanorthosite ( Ga emplacementterranes, offerroan granites initiated 0.99Ga,andculminated at 0.95 (Söderlund et intrusions al., 2005;Mölleret al., 2007).the Sveconor In western thisShield, Ga. extension doubling, commenced Andersson(Möller, deformatioductile was coeval with high terranes.Sveconorwegian 2015). al., collision, therecorded in Eastern Segment interpretedas hasbeen lower E S Tual, Pitra, 2017)& Möller, Brander, Brander, Brander egment astern astern

Accepted Article, the presentthe level,the erosion

- In the EasternSegmentIn the anditsunmetamorphosed continuation eastward the in Baltic coeval coeval with intrusion

up and top The Eastern Segment Eastern The

| | - , (Drake crustal ( nappe

Sveconorwegian Sveconorwegian p The , and 1.47 & Hanse S . It . It is thus interpreted to havebeenderived edge from leading the ofthesubducted & egment or Appelqvist, Cornell, In eithercase, i , fanis a

& extension Söderlund, 20Söderlund,

alternatively

in the Proterozoic in the re , (Figure 1c)(Figure

Whitehouse Tullborg, &Page, Tullborg, - - n, Sveconorwegian to –

following crustal doubling,back and beenthrust crustal tohave itafollowing over as large

1.38 Gaand1.24

- n, andmigmatization section oftheinternal of 2011; the developed upper within the , Lundqvist, & Hellström - 1 shaped, - op. cit. 0

pressure granulite - is manifested by0.97 – east kinematics andamphibolite marks 2 , partial melting,partial and , mainly . Thismagmatic beltformed an in metamorphism anddeformation metamorphism Petersson 5

as due to as due of 0.95 , 2002; t testifies totheEastern Segment 09;

Partial exhumationPartial oftheeclogite however, upper crustal nappesandhowever, upper sediment km, bedrock wherethe by responded non

). , thereby itsmetamorphic linking evolution vertical tosteeply west

Söderlund et al., 2005,Söderlund etal., Söderlund - the eastern limit eastern of the The eclogite dipping & bedrock

composed of rocks composed

eastern boundaryofeastern ductiledeformation Sveconorwegian is 2009; Saintot – at 0.97 at

Ulmius Andersson (Rodhe, 1987) continent Baltica continent 0.93 Ga dolerite dykesand Gadolerite 0.93 0.93 , Scherstén, Andersson, intracontinental thickening to related collision (Mölleret – 1.18 Sveconorwegian Front [Figure1c; Sveconorwegian

– - (Wahlgren al.,1994). et

, Andersson, & Möller & , Andersson, 0.96 Ga across 0.96 Gaacross and upper amphibolite Ga - see see compilation byBinge – faci , 0.94 Gaorogen , granite, monzonite, gabbrogranite, andanorthosite

leucogranitic

2012; 2007; Möller al.,2015). Möller et 2007; , -

es metamorphism doubling andcrustal

Stephens, Viola, to midto and fracture fillings discrete discrete

quartz of - Söderlund, -

veconorwegian dipping - greenschist facies deformation structures volcanic slivers(

the 1.86 the - - crustal basement at facies parageneses (Andréasson

the orogenthe either an -

monzonite east & Möller

dyke Andean underthrusting

- - deformation parallel pegmatite anddolerite bearing bearing terrane 0.98 at - - vergent, thrust 1.66 GaTransscandinavian and include Möll , 2015 -

& These sparse and narrowThese sparse and intrusion facies metamorphism, & the the

‘India

– Ask, 2006 - , lasting least until at 0.92 Nordgulen, 2011). The 0.92 Gapost type andis orogen , 201 F n et al.,n et 2008b - er, Andersson,

Eastern Segment and penetrative greenschist in Proterozoicigneous ront ) Nolte, Kleinhanns . . At the time. Atthe of the s -

to ofthe that E

covered thecovered style’ continental Following 3 quartz

, the front, the zone, west with at 1.47 at ;

the westernthe an unknown 1.57 Stephens Stephens ). - sense, sense, ductile The - wegian – - – 1.56 Ga orogenic 1.38 Ga low ;

al wedge – crustal 0.97 Ga & – - 0.92 astern astern

& ,

-

-

This article isThis article by protected copyright. All rights reserved. of Fe intheEastern oflocations thousands Segment, andaselectionof Data ha 3 | are 956between ±7and934 ±6Ma of and974 of±25 Ma baddeleyite) metagabbro inother parts oftheEasternSegment ha toprograde restricted and eclogite 2;(Figure Table 1including U references). migmatit U 2.2.3 | terraneIdefjorden aboveandtheEasternSegment below partsouthern b contact Wahlgren, Weijermars, overlying Idefjordenterrane and high migmatization exhumation, during andtheeclogites record partialre temperature mylonitic in footwall, unit the 2015;Tual,al., foreland itsinto presentposition of~65 2017).a depth km etal., (Tual T recumbent fold. migmatitic orthogneiss derived from Eastern the Segment ( ofthe part internal section both felsic andmafic rocks. metamorphosedare high and to grade transitional a over 1c) amphibolite arepenetrativelyrocks ductilely deformedmetamorphosed and recumbent over fromchange a fewkilometres non Rodhe Fig –

Acceptedmafic and both Article METHODS Pb

between - is defined ure - penetrative. - pressure

Ti

ages ofmetamorphicages metabasic zirconin rocks , Timing ofmetamorphism Timing

1 ve 1990; - - c; et Möller al., 2015). E ic varieties,ic richmetagabbro etween Eastern the Segment western andthe Sveconorwegianterranes directed

ly been retrieved from documentation field investigation andpetrographic of -

c. facies conditions.facies folded

In the In the sectiontransitional Post The An eclogite with Wahlgren al.,1994); et deformation and by the appearance by the granulite

940 and 900 Ma (Page, Möller, & 1996).940 and900Ma(Page,Möller, Johansson, Pinan Eclogite metamorph Younger

extrusion - eclogite

felsic felsic migmatites between fall 976±7and 968 ±13Ma distance ofa kinematic cross late foliations, a and

date metamorphismdate Segment 1.00 Eastern between inthe and0.96Ga -

Llamas, Möller & rocks Sveconorwegian -

& at (35 ~10kbar and upper amphibolite and upper the base ofthe base the eclogite -

- nappebearing o was used

brittle Cruden bearing nappe occurs structurallybearing nappeoccurs beneath the ofthe contact (Johansson, Lindh, & Möller, 1991; Lindh,&Möller, (Johansson, Wang1996).& Lindh, , and . The rocks in the . Therocksinthe High Farther west kilometre. bout

.

– i

of

the clogite and clogite retro s structurally concordant with surroundingrocks - Well ductile (n=7) , - granulitepressure -

facies cutting granite 1996) subvertical granitic granitic leucosome for thedefinition ofmetamorphic zones. 1 Zones

crustal ism at~870Cand18kbar, corresponding took place to gently eastgently

- generally generally

constrained . – (Fig he eclogite , 2015) high

40 40 km depth) during40 kmexhumation, partial depth) caused and brittle . The Mylonite Zone. TheMylonite zircon in ccurs ccurs at contact the A To the west, withinTo thewest, internal the – , - ure r

Pb zircon datesolder than0.98 (sofar) Gaare scale the – - grade gneissicstructures 39 eclogite

- shear zones . Its 1

- Ar coolingages ofhornblendeandmuscovite - facies facies conditions. penetratively boundary bearing nappebearing dipping dipping c

gressed - Mylonite ZoneMylonite Fig (MZ, )

pegmatite dykes - , eclogite. eclogite.

ages ofzirconcrystallization ages in leucosome bearing nappe wastectonically emplaced contact is outlined by gneissan augen fault west of - s facies facies rocks occurin westernmostthe

and felsic yielded -

metamorphic rec bearing in felsic rocks in felsic s

fold (Andersson et 2002) al.,

eclogite , are with

are contained

to the frontal wedge, frontal the M

axes also localizedalso inthis zone. with upright, orupright, inclined, deformed, with ages of ages etamorphic zircon in etamorphic zircon marks the

nappe underwent syntectonic nappe underwent is the internal the section

under gneisses, including

a thrust 2 , withcountryrock

(Möller al.,2015) et 76 the the Idefjorden have yielded ageshave yielded

-

; this is boundary

equilibration 970 ± 7 Ma (breakdown970 ±7Ma locations andsampleslocations intermediate on side,either rystallization wa main litho

within a within zone of

ure section (n =7).

leucosome

1 structures , c; c; in the

. high Terrane , the rocks major

Stephens (Möller et under tectonic tectonic (Figure

–

in the 6 are 6 are -

. Here, s

in by ,

This article isThis article by protected copyright. All rights reserved. pyroxene.pseudomorphs after rich and(pyroxene plagioclase) (Fig respectively ofthetexture plagioclase, Fe types rock the ofgabbroand intrusions syenitoids. Transscandinavian Igenous Belt afewdecimetresthan anastomosing submitte state metamorphic Sveconorwegian deformation zonesoccur, butm ofzoneEast 1 4.2 olivine d the zones grade quartz than with garnet amphibolite and 8 assemblagethe 6 are emplacement ages assemblages Eight 4.1 | F investigatedthe metamorphic map inFigure presented presented The 4 | from University. research 1:250 000and1:50 geoc during thecourseretrieved beginning of30years, in198 identification ofmegablasticminerals leucosome. in observations andField samples were onpetrographicmicroscopy, andbased 7andmacroscopic zones 8on andmicroscopic igures 4 igures

Accepted Article REGIONAL deformation zones |

ure

metamorphic in hronological hronological studies, coupledwithbedrockmapping later

Metamorphic zones 1and2 Metamorphic D ata set minute grains spinel inplagioclase

SGU are shownin Figure SGU are tracked inmetagabbro devoid of m are

efinition efinition

blue

was discounted etamorphic zonesetamorphic 4 - d targeted mappingtargeted

b, –

monitored ). below . 8 given are in S Table c).

. - Where deformed, The geographical distributionThe geographical of bedrock maps observationsavailable and points

, green amphibole green around pyroxene igneous Similarly

in F show Zone 1ischaracterized by abundant

deformed rocks , in Undeformed Undeformed amphibolite -

Ti in non of metamorphic zones ; metagabbro

e METAMORPHIC ZONING METAMORPHIC assemblages of the the - - characteristics ofth

. oxide, withtitaniteand/orepidot andbiotite, locally between Ti that the that Most by differen - eastern , orthopyroxene

richmetagabbro, - , wide

migmatized metagabbro which become (i.e. - by bearing metagabbro bearing

metagabbro small samples contain in -

, butne facies ( igneous igneous , the GeologicalSurveythe of Sweden gabbroic ( 1 1:10scale 000

lack the Eastern Segment Figure samples .6 frontal wedge , Fe

with

S1 ost of the bedrock the ost of hasrem t and , - 1

peritectic mineralperitectic Ti intercalated of the different deformation width,in ofvariable most zones less places . . : ar

-

protoliths were blue lens 1 4 rich chemical (Fig Complete m rocks retainrocks primary igneous deformation they zones have a) .0 Ga is

e investigated area inthe Eastern Segment occurring exclusivelyoccurring more close leucosome 3

. a widespread protolith withthreeorfour

shown in - . Th - appears to ures me shaped shaped An overview green hornblende ) . is deformation , sparseand

tagabbro C by ; one sample such

1c hanges in hanges in metavolcanic slivers,

equilibrat zone

the Department ofGeology atLund

does not changedoes not

and aggregates of etamorphic recrystallizationrestricted isto

. ly towardswest spaced the Figure

are N s In zone 6 In zone and higher

s have originally

- in leucosome

3 are are

S striking andsteeply dipping consist defined basis onthe ofmetamorphic ;

map , or more or less complete, ormore Wahlgren et 19al., ion narrow greenschist metamorphic

summarized Table in stabilize S 8

2 ained in a pristine ina orp ained igneous affect

with metamorphic and on thinscale the section . of t of

s ±garnet

with Geographic Geographic coordinates amounts of quartz. amounts ofquartz.

of blue medium (SGU)

plagioclase from was he . s

in d

I s 1.9 nstead geographic distribution

texture and minerals

either either

orthopyroxene

in and therefore pseudomorph , and, beginning in, and,beginning 2010, 2003 , - –

green hornblende, assemblage Fe in - 1.

e

to coarse to younger (westernmost areas 7 . - the frontal the frontal wedge ,

developed developed Ti

T

changes Ga to 94; Ulmius al., et and dark mineraland dark - he - facies rich migmatitic

2016 at scales 2016 atscales and all transect excluded rocks ofthe rocks anastomosing 2 , and the M - 1.6 are are s s after grained

in in 7 zones etagabbro in zones

) – coronas

. lower

1.2 Ga for

f

rom

re

of

- ) s, of

1

,

– This article isThis article by protected copyright. All rights reserved. clinopyroxene o plagioclase, garnet, zonesthroughout 6. 4to rare undeformedeven in andoriginally coarse assemblage. zone 6,~ sub additionbut in contains epidote of byminute“dusted” Fe clinopyroxeneigneous even moderately The are bodies migmatitic andmigmatitic arepresent varieties in someother whereas mafic bodies, large small foldedlocally associated (Fig by is characterized The internal section orthopyroxene 4 is pyroxene co metagabbro 6 biotite, deformed Beckman assemblages lack with complete amphibolite In t 4. similar tothose T garnet in metagabbro .4 – he metamorphic minerals 3

ronitic ronitic rocks 7 Acceptedolive Article

he sectiontransitional - | | . ure

granoblastic neoblasts mm in leucosome

- signs partialmelting of Metamorphic zones Metamorphic Metamorphic L - grained scale foldsscale ocal

Fe - and 6a green hornblende 20 , Möller, Söderlund, Söderlund, Möller, & Andersson , - and

– ly, either with Ti

diameter c – . deformed -

titanite blue

) facies conditions.facies P 30 Garnet istypicallyGarnet located the domains at borderofplagioclase i and are and are - . N metagabbro ofinThe presence garnet defines The metamorphic assemblages ofmigmatitic amphibolite appear similar 4, In zone to , dilational netveins, rutile rutile oxide lagioclase lagioclase mostin rocks

recrystallized Fe metamorphic recrystallization . -

, in a ofrange free in km ccurs In somemetagabbroof coronitic the relict coarse - on , non green

as well as zone 1

- . the presencethe of , and locally the , farther farther migmatitic felsic andmafic rocks is present insubordinate amounts biotite, zone . In zone5, metagabbroic rocks

- variably beginning . textureCoronitic is migmatitic or is located is located bodies bodies - Most migmatitic amphiboliteMost

(Fig Ti oxide grainsTi oxide ( in colour. internal section the metamorphicassemblage m M

3 ( , plagioclase, biotite,andFe garnet, (Figures etamorphic clinopyroxenetamorphic , deformation structures, 4 Figure : , igmatitic igmatitic amphibolite

west ure

Fe

and – . C other thangarnet green hornblende+green - small leucosome 6 grained andcoronitic ( transected by foliated - : s 6e, ompetent rocks, e.g. ompetent rocks, gabbro, In the metagranitic d rocks, ~ Ti -

~ , o garnet with olive Ti as close western tothe of border 10 km farther west, 10 kmfarther west, epidote 50 km

-

4 oxide andplagioclase - rthopyroxene

clear rims o rich gabbro 1c d) leucosome f) texture penetratively . The relict . Therelict igneous pyroxene is .

and and/ is Figure west of

and/or

occur occur as completely recrystallizedtogranoblastic aggregates abundant

- 3

grainedmetagabbro; remnants ofprimary laths or lineated vein ) , amphibolite faciesamphibolite , 2017 , and deformation structures

of major minerals5a, (Figure rocks patches. patches.

in n

is greenhornblende 6 s,

titanite (Fig

the S the and the relict relict the e

garnet both is and veins parallel and veins to the ). migmatized. - undeformed ). Thecharacteristicassemblage in including - green hornblende,green cl

e in undeformed deformed weakly or textured dominated byolive we

s , typically assmall the the assemblage isthe same 4, inzone as commonly antiperthite s veconorwegian

;

, amphibole coronas in aroundigneous are in in metagabbro inzones4 are also granitic and re Gradual transitions non between Fig , –

non in quartz leucosome metamorphosed rich ingarnet

igneous clinopyroxene grains. ure eformation ure the

locally locally zone 2 rocks - stromatic migmatitic m

- 6e). 6e).

the frontalthe present (Figure 6d)(Figure Ti

shear zonesshear 5 transitional section d - oxide, – with remnants of The . gabbroic , f

preserve igneous ) The plagioclase ; garnet locally locally ; garnet reaches

F characteristically .

fabrics are gneissose are fabrics y

ront veins, . - Leucosome ,

green hornblende,

Garnet occursin Garnet r first appearance clear, clear, light green, generally inopyroxene, and ange from wedge (

under in zone 2 in zone axial planes ofaxial

etagabbro consists consists etagabbro to weakly or to weakly ; locally ; locally b), but theb), but rocks (Fig (

join Fig compositions which are which are n ure ure – , garnet,

the

intermediate the 6. Figure without

s

se is

5

are fine coarse coarse

1c c

–

e and -

- ;

3 In of and

)

are are .

3 ) ,

This article isThis article by protected copyright. All rights reserved. completely recrystallized inthe wedge,frontal Asarule, igneous plagioclaseundeformedpyroxene. in iswellmetagabbro accompanied by minerals (Beckman al.,2017). et undeformed andcoarse igneousPristine are rocks 1and2. foundonlyinzones 4. gneisses ribbon and coarse locally orthoclase occurigneous regional, Sveconorwegian the metamorphic orthogneiss in offelsic zonessections 8,t 7and bearing, metagabbro strong hasa deformation defined fabric byhigh coarse metagabbro havegrains grown inmelt omphacite, but the melt;tonalitic 3 garnet amphibolite, butalso local cm indiameter. megablastic garnet hornblende hasacharacteristiccoronaorthopyroxene offine commonand is inleucosomeorthopyroxene ( phasesperitectic inleucosome 6. in zone In section internal 4 metagabbro, and R mineralsof peritectic cm orthopyroxene inthe zone The maximum sizeofgarnet increases from leucosome at . etrograde etrograde minerals 6 cm long 5

Accepted Article 7andzones 8(

Varberg charnockite) | |

Recrystallization zones Metamorphic - grained metagabbro hast occur as in zones7 is

There and almostand skeletal

grey microperthite ( in many places Figure Wh highDespite metamorphic temperature7 zones in I the firstthe appearance parageneses n

Figure (zones 1 (zones

in Rare p the the porphyroclast

is, an ereas include titanite - Figure zones zones 7 and8

textural textural

and lens ( – however, 7a), increasing degreeincreasing of recrystallization of plagioclase igneous and westernmost ( areas Figure

8 are moreare commoninmigmatiticamphibolite than in non

7c). Th and

t eritectic eritectic clinopyroxene felsic orthogneisses inzones 1

- hey are – trend

grained gabbro metamorphic hasthin around coronas igneous the that

2) s . 3), n

is tonalitic incomposition, . T in both generations of in both are presentare 7 strongly gneissic

partly preservedpartly inthe transitional sect 7b) association - hese ‘dry’hese metamorphic assem – retains shaped quartz shaped likely is 8

on a , , . Figure s across zonesacross 1 : peritectic orthopyroxene and

rich in antiperthite in migmatitic in W also texture bemistaken canpotentially fordecompressed reaches geographically wrapped by highest -

, hick garnet coronas (Figure (

migmatitic metagabbro ofthesame consists as assemblage

The metamorphic ly migmatiticin gneiss, felsic and ith the the ith formed of expense the at Figure of

developed textural remnants ofigneous clinopyroxene pyroxene

leucosome 7a

in composite

with - ) appears ) appears 4 zone 8,

grade (possible) both

3 cm ; Hansen et al., 2015; Hansenetal., , aggregates

, and locally mesoperthite thin thin leucosome

~ deformation (Fig fabric or more or – garnet amphibolite. - 1.7 Ga during 0.5 cm0.5 olive inthe bearing. 8 zone occurs systematic

~ wo ( trails Figure - orthogneiss; orthoclaseorthogneiss; igneous plagioclase 1 ~90 grained garnet, clinopyroxene,and 10 - exception of garnet s

p temperature increase

6

. L yroxene and

cooling. cooling. – km from consist . in km –

of recr 6 are typically hornblende6 are Metamorphic feldspar In 8

In zone 3,even demonstrates ocally 6c; zone 8 .

1.4 Gaorthogneiss

west of west ~ Likewise difference inthe

blages blages Fe 4 olive - 0

ing 7d) ystallized metamorphic feldspar grade mineral aggregates. + quartz - -

% oftheinvestigated thin Ti oxide giant garnetgiant megablasts are and garnet ). This ). This the the . It occurs . It megablastic –

. of plagioclase and quartz - - 8

As arule, fine M the S the typically define green hornblende zone green hornblende zoneto , non ion S ,

egablastic forms veconorwegian igneous pyroxene . ure

that c that these

megablastic inclusions (zone 3) , veconorw ,

-

the bestpreserved, leucosome devoid is

migmatitic and epidote 7

- across across in e, bearing poikiloblasts distribution of f) - leucosome in

preserved in the garnet ( . Remnant

the the latter in ‘dry’ the - 0.5 , and migmatitic . Originally . Originally - zones 1

grained e

( linopyroxene -

grains – inferred gian gian a

and biotite 6

.

F

in cm ront

F is

the being being , upto – ront

8 4 ) .

). 2 is 2 0 ,

- This article isThis article by protected copyright. All rights reserved. reported ~ 7and zones to peritectic8, needed produce pyroxene Gorbatschev, Möller, & Rodhe, temperature 1998;Möller, anddecompressedgranulite eclogite are metamorphicthe assemblages the method for suitable s of uplift the block.western This wherein southern areas, acrosscoherence granulite pressure temperature acrossEastern Segmentsection the The systematicchangemetamorphic in assemblage of 5.1.1 | 5.1 5 | amphibolite to kbar free (Fig well is a assemblages to the in The m folds,upright eclogitized terrane. Theterrane arecumbently occurs as foldednappe,refolded byyounger M with T most ( by in detail The 4. highestgradethe zones section the characteristically ‘dusted’ bytiny preservedbetter 2015, 2017) ystematic 850 he southernmost part ofhe southernmost north thedomain part isa 7 igmatization anddeformation

Acceptedintermediate Article INTERPRETATION AND

previously estimated range pressure of9 | | , 2 ure -

setting, andpetrology geochronology oftheeclogite The eclogite The may ( high and growth zoningingarnet recordsaprograde evolution at peaking preserved arepresent: eclogite kyanite

parts ofparts eclogite the °C Figure x 1

ylonitic The

8c

estimates for the westernmostthe for zones, 7and8 .5

- expos be explainedby be ). T mylonitictemperature gneiss ; the

estimat km metamorphic Möller Möller s -

from to east west facies conditions abundantfacies in is the

. Abriefdescription is givenbelow 8 around Quantification andEclogite retro extures its d WangLindh, 1996) & assemblages are - se sized sized ), after which ), after the rocks underwent near ed pressure granulite

in lower grade zones.in lower grade structure outlinedby deformed 1.4Ga

zones 1 - - oxide inclusions . es bearing facies conditions underthrusting continental underthrusting plate

( the 1998, 1999 , 630 l

using aninternally consistent thermodynamic set data and assemblages ayered mafic body the enclosinggneisses outside the

. range in in range temperature

the the – - °C bearing domain, arestromatic orthogneisses 8 late field gradient

terrane , without major, without tectonic breaks.

metamorphic of metamorphic the conditions w , . -

ere

from Early ), gressed and high 2004). took place duringtook place DISCUSSION

Johansson al. et , presumably

-

obtained foroneobtained locality in zone3(Söderlund facies conditions.facies in relict igneous clinopyroxene

post qualitativeprovides evidence for a - in zones5 low .

pressure granulite pressure P P

T – in t ressure W eclogite occureclogite - and T

extural remnantsextural ofigneousclinopyroxene, – 68 metamorphic faulting frontal wedge, alongthe

in the in the

middle amphibolite ater

estimates hese rocks data suggest that 0 - – retro bearing Mg ( ; yetthis hasnot been performed – Hansen et al.,Hansen et 2015 11 kbar for11 kbar zones - 770 undersaturat – s of 10

- exsolved, exsolved, basal shearzone. Twotypesofcomparably 8

dipping basal zoneshear . pervasively .

-

eclogite boudinseclogite ( This °C east 2001

based on based geothermobarometry

Further Further retrogression

, – and demonstrate

as indicate 12 kbar - Fe - - pattern vergent exhumation partial ofthe

isothermal decompression isothermal decompression ), augen - and eclogite - Al layers andlenses in orthogneiss. In -

opaque in

bearing 8 Möller al. et Ti ed meltingpartial ofmetagabbro in – -

zone across zones 1 across zones An exception to this coherenceAn exception tothis 11 kbar 11 kbar rich - upper amphiboliteupper migmatitic parts nappe. ofthe - rich facies inzonesfacies 1

s temperatures orthogneiss i ( suggests an an structuralsuggests overall possibly an 5 , s 2 )

– domain and Fe , i.e. higher, i.e. than metagabbro terrane

8 appear that they typically becomein coarser ( clusions, – Figure (Johansson al., et 1991; 4

are ( migmatite gradually 2015 - . , up to4 kmwide,

Ti ha

The largest eclogiteThe largest missing ~

– unde s 8b) - n the footwall.n the over

870 8 ve were rich consistent or a occur ), and

. at oraboveat requires

along a1 along

.

N - been described been described and 2 r facies, - , nother °

evertheless, evertheless, ,

estimate lower

C and18

increasing increasing eclogite plagioclase Söderlund, (

the the

under Figure ( throughout Tual et Tual et al., of Figure

to high

mafic

similar w 2 with

0 km ith high )

8a). 8a).

and 3)

is -

- . -

This article isThis article by protected copyright. All rights reserved. amphibolite minerals in migmatitic rocks, and pathwaysinducing for fluids meltingpartial is gneissesLeucosomein felsic amount structures. and instead withassociated foliation and folding,forming dilation, stromatic, and patch, net & Hansen, al.,Hansen et 2015; (Fig migmatization variations observed in mineral assemblageand (‘wet’ variationsor ‘dry’) the in syn Sveconorwegian state fluid Sveconorwegian (fluid deficient, CO ( highe 4 zones andarerocks spatially associatedwithdeformation ( zones such hydrouswere for fluids necessary metamorphic recrystallization of andmafic felsic Sveconorwegian during deformation (Beckman Whitehouse, (Harlov intrusions areasMoreover, in western local whereas minerals, hydrous e.g.sliversofmeta orogeny. Manyoftheintrusi Sveconorwegian Probably, someof fluids. differences hydrous these were of present already prior tothe of andThe presence assemblages ‘dry’ ‘wet’ the in same area 5.1.2 ultra paperthis The assemblages Barrovian and pressures thesimultaneously with emplacement oftheeclogite deformation andmetamorphiczoning but thickenedknown howmuchthecrusthad before emplacement ofthee at that this terrane wastectonically emplaced The eclogite ~ Hansen et Hansen et al., 2015) 18 kbar and18 kbar 870

hornblende quartz in Accepted Article~

10 kbar the the ure - high temperature metamorphic conditions st | Fluids andpartial melt Fluids - s 6 s main deformation ductile recrystallization, corr and – grade zones

5 the presence of fluidsa hydrous of ,

field gradient and G define

2015). , i.e. garnet growthgarnet prior to -

at approximately at samethe arnet 2007). H facies assemblagesfacies and subsequent their granulite Pressures distinctly higherPressures distinctly than theelsewhere in Segment, Eastern at peaking In situ Th temperature

7; thewithin internal section (zones 4 was dominant in was dominant in in interiorofadoublethe crust (Möller e metamorphic field gradient

Andersson recorded by - a ° , L bearing leucosome widespread is garnet in amphibolite

C (Tual et 2017),C (Tualet al., been have estimated eclogite forthe Johansson, den van Kerkhof,&Förster metamorphic fieldgradient eucosome is leucosome Möller et.Möller 2007, al, 2015;Pinan hydrous have fluids to beeninterpreted - . metamorphic 2 It is hypothesized that the O - monzonitic monzonitic migmatite

in the Scottish Highlandsin the - rich fluidrich was, s

( , Söderlund from , is 2) Fe

s , however, is present in both in throughout felsicandmafic rocks is present

felsic rocksare - hornblende and biotite as hornblende andbiotiteas the dominant ferromagnesian generally absentgenerally in undeformedweakly deformed rocks and enrichment Ti ~ 3) and during 550 550 infiltration of hydrous -

rich the firstthe illustrated illustrated in

location. location. ° , Johansson, &Möller however, demonstrably drygabbro introduced into C metagabbro

generally devoidof phases peritectic ssisted andenhanced to as anappeorthrust sheet of CO of appearance ~ . partial melting in the Eastern Segment ve protoliths volcanic volcanic rocks may hydrated. been have

850 Field Field relations . that approaches, but 2

:

et al., et - combin

1) dominated

– (Barrow ° 2 8). F the associationwiththe deformation - C - - igures 3 igures rich fluidrich Llamas in bearing nappe.

,

2017) and

, ed the Eastern Segmentthe Eastern

1998; et Möller 2015). al., of

fluids

, ,

primary Figure esponding the to regional have originally low

~ , leucosome 2006 19 . control typethe of

,

9 or H in differentrocks

I

and Andersson , – suggest n the n the lower zones grade 1 s reflects an reflects an uneven distribution 1

-

1999, 1

facies overprintfacies

2 is partial meltpartial contributed 1 ; ; Vorhies &Ague,2011

2

9, tookplace

associate 4a). O Rimsa kbar igneous igneous - does

dominated) the and into present its p Andersson etAndersson al., ing represents represents

In the c ) in felsic gneiss and in felsic

logite than classic the , ,

not reach quite into, that that , Möller Johansson, Johansson,

but t d ing, and in the ing, andinthe

and

both , - higher with 1.4Ga

bearing nappe. - water d bearing nappe,

are ocumented ; contents more orless partial partial melting he relative demonstrate pre higher an ,

to the Johansson,

not known. - - - exception It isnot zones 4 present grade , & osition osition 2002;

– of 3 ) .

,

in

–

6

This article isThis article by protected copyright. All rights reserved. terrane witnessbear of The d 5.2. 5. demonstrated casebe the M associatedwithtight fabrics ofthe parts migmatite at0.98 betweenbracketed zircon ofeclogitization dates 0.99Gaandmeltat in crystallization section,internal emplacement oft penetrativethe metamorphic layering andtight foldswasbroadlycoeval patternairborne magnetic sheared fold limbs been have developed 2015; Pinan folds etal.,2015) (Möller bodyoutliningaugen gneiss boundary ofthe the eclogite concordance layerin airborne magnetic ductile highly 3 penetrative manner The deformationpattern 5.1. excepted). mixing meltand of different implicitly sources, meltmobility, wasrestricted(pegmatites 1.7 where partialmodified bySveconorwegian melting rocks the in Eastern the Segment are not varieties undersaturated and garnetpyroxene giant ingarnet amphibolite interpreted are migmatite migmatization inzones4 than 7e, assemblages (Figures 2 at~650ºC) (roughly Acceptedetamorphic isograds Article , 1.4

1 | 3

The tectonic context tectonic The , and | | isparate pre

it The The Deformation s g

and

, with , were not w

throughout the Segmentthroughout the Eastern .

by as parallel

Migmatitic Migmatitic g relation in underthrusting plate - 1.2 Ga

Llamas al.,2015 et with the with the regional Sveconorwegian fabric produced. Z produced.

In zones 7 In zones The metamorphic assemblages B later generationslater ofuprightfolds

in detail the metamorphic mapthe here presented (Figure 3) and penetrative transposition of

ulk partial melting.partial its roleasits a in the general presence ofpartial melt. Th - he eclogite – in 1.00 anomaly 0.97 Ga( to , chemical

beginning inzone~ 1,at beginning

. respectively their present positiontheir present between the

The gneissic layeringThe gneissic wasfolded the fold of axes .

are therefore expected to crossthe and higher, Ga evolutions orogenic on eitherside of – arnet arnet amphibolite is shows f) and 8 felsic gneisses the more commonly ircon ircon inheritance in leucosome ofwithin avariety rocks (

Figure c pattern pattern

Table 1 Table - (D2) data . bearing fold nappe, - ly out, 1.00

– early structures structures andearly

6; l are on are average

that that ; Tual et al.,; Tual et 2015

deformed ; op. cit.) pointstoaninsitusource,which indicates that behaved of orthogneiss felsic

lower upright to recumbent 9

from ocally in Ga crustal amalgamationGa crustal zone. ). ( ). the underthrusting plate Figure the transiti the In the e T arly generation arly ogether, ogether, t

outcrop tokilometreoutcrop the and upper plate and upper , restitic

in a highlyin a ductile manner. s . clinopyroxene (

prior to This is evidenced both evidenced byf This is Swedish Ge

9) transitional and 55 . R abundant in deformed rocks .

less affected bySveconorwegian The record rocks n ( 0 ather

Andersson et 1999; al., onal andinternalsections, and – he under ). 600 rock contactsrock 1.00 se data Linear were not ,

es melt tohave appears . , and º

folds

C into Rock aresemiunits ological Surveydatabase ological highly conditions and ductile

folding oftheregionalgneissosity , Ga

. At - occurs in both

s bearing nappe regional gneissosityregional e timing deformation ofthis is

demonstrate ~

occurrences occurrences of

km includes

(D2, op.cit) internal

started started to deform E the the

, depleted or

migmatitic and non –

- have but scale recumbent andinclined scale W stretching structures to have can be the MyloniteZone the

temperatures attained inzone scale into concordance ear

E granitic remains be to

: pyroxene viden

sections -

penetrative gneissic ,

ield ield also in seen the linked toaxial

that Möller al., et . places,In several formed by

is stillrecognizable with tectonic

significantly ce that the ce that the western –

data megablastic - the the largely largely granodioritic granodioritic coherent, e.g. the the , development of -

; in a semiin a b rocks wererocks

this appears to earing and the deeply buried )

- ( record

migmatitic

or near protoliths water remained ( Figure , in the 2007, - planar -

- tha

. an

the 1)

t

This article isThis article by protected copyright. All rights reserved. compression andby steep decompression beneath the heatedpreviously metamorphic amphibolite earliest metamorphic ~65 Segment and Baltica Baltican above) toaplate attached convergent phase metamorphism anddeformation, 2015). etal., 13 inMöller weuse(2009), name wester the for Sveconorwegia SveconorwegianBaltica andthewestern terranes west of The differencesoutlinedabove(1 5. contemporaneous dykes pegmatite in internal sectionofthe the Eastern Segment post SegmentEastern (Fig terranes Ga and (4) 2017 km and depth isa terrane (3) metamorphism anddeformation reaching is prograde c. main Sveconorwegian Segment (2) orogenesis overprint alkali 1.52 calc Scherstén, Bingen,Petersson, Gerdes, tectonothermalSveconorwegian evolution (1)

2. Accepted Article50 M P The occurrenceof the The Crustal blocks 2

- - – km beneath depth alkaline formed belts, the during andvariouslyreworked 1.64 re ). collisional - | 1.47 GaTelemarkian

calcic r Tectonic Tectonic

-

rather suggest westrather suggest at 1.0at Gacausedthoroughreworking andhigh a 0.9 Sveconorwegian and post

oceanic andcontinental lithosphere. ed by eclogit are different distinctly together withtogether magmatism, granite the

5 (Ulmius al.,2015) et metamorphosed ofthe slice Eastern Segment metamorphism - doubly – ure facies 0.92 Ga, respectively, suggests 0.92 Ga,respectively, The main in phase Sveconorwegian the adjacentthe ocks ofthe1.86 stage stalled stalled

1.47

0.9 e 1; interpretation -

- and the eastern continuationof eastern and the Balticcrust collisional magmatism

facies could Sveconorwegia on either ofthe side MZdiffer inprotolith age

at theat present

e.g 7 conditions may reflect – thickened chain mountain – 1.38 Ga metamorphism1.38 Ga at 40 km depth stage 0.92 Gadolerite dykeswarm . Sveconorwegia stage Brueckner, 2009)

have been caused byeast have been at at evolution 0.99 Gaeclogite basal levels of

-

, , 0.99 in eclogite

dipping subduction recorded ingarnetcoresofeclogite orogeniesaccretionary (Bingenet 2008 al.,

beginning at –

correspond 1.66 GaTrans

underthrusting . Ga. ThroughouttheEastern Segment theregional .

is west of Sveconorwegia, W including n crust –

s 4, 5.2.1)section justif dated at0.98 hereas the westernhereas

of westernSveconorwegian the terranes the and Eastern within

( & Whitehouse, at at c

. . . In in the western Sveconorwegian terranes western in the

Svecon 0.99 Ga ing

100 1.05 R paths -

(Andersson et (Andersson et al., 2002; Petersson bearing

apid apid tectonic b migmatization the orogen

contrast, significant and associated and associated magmatism s to an geotherm elevated , 0 The f candinavian candinavian Igneous Belt

followed byrapidexhumation, and heating Ga (Bingenet al.,2008 and underthrusting Ma first record – (Fig orwegia 0.97 Ga - (Möller etal., Tual(Möller al., 2015; et Sveconorwegia dipping of subduction oceanic lithosphere ; Andersson inal inal intruding nappe ure

analogous magmatism isabsent - terranes 2015). West2015). mainly oftheMZare

grade metamorphism theEastern of n Sveconorwegian terranes (cp. f (Möller et al.,(Möller et 2015 collision

8d) mantle involvement under the .

y

that that but the geological data but thegeological data

(Fig the the Eclogite , j

urial

the the betweendistinction continent ust theMZbelow of and formation granite of orogeny . :

In the In the E during MZ. Following Brueckner Baltic was partly was partly exhumed from magmatic activity is limited to ure

, Tual,&Möller, w to eclogite ,

of with Sveconorwegia ere took place under ,

2; at 1.05 at composition

– beneath Sveconorwegia by record Eastern Segment t

a

1.52 GaGothian Table 1 with references). metamorph n . –

b

crust in W extension This earliest This earliest a ) , in t

). during Hallandianduring

– and s the - 1.02 Gainvolved

East ofthe East MZ are ; Tua facies depthsfacies burial he south he south beneath Eastern Segment progressing for (Fig

et al.,et are ,

osed and pre l et al., l etal., 2015,

2017 (points 1 . .

ure

of Baltica

at 1.0at suggested 20 This ,

2013

17

, and during 1 locally here are here

)

and se , in t )

) 7 . This - . igure igure ~ –

; T 65 – 1.02 he

he 4

at

al a

a

This article isThis article by protected copyright. All rights reserved. orogenic centre, m corresponds orogenicto the wedge ThrustCentral inthe Himalayas ( inferred comparison,t Sveconorwegian eastern the (dashed blue exposure line in Himalaya inFigure Profiles 5.3.1 5.3 terranes.Sveconorwegian forelandof orogenandits ( the atExtension 0.9 anorthosite collisional ofWestward subduction beneath crust thewestern Sveconorwegian terranespost induced metamorphic terranes P western Sveconorwegianterraneszone, the represent theupper plate scrapedcover off, extruded (thrust Almesåkrathe u Front Sveconorwegian preserv Segment (i.e.of Segment the Baltica above Eastern andeastwards) tectonic settingits asthe plate lower of orogen. acollisional penetrative deformation oftheEastern Segment. Magmatism was absent, in accordance with underthrusting, 0.99Gaeclogitiza Himalayas, present doublycontinentalrequiring thickened crust. Thecollisioncaused crustal Sveconorwegian during orogeny upper Sveconorwegian valueGa, this confirms ofcrustal thickness exposed originated bedrock the that as & Stephens Andersson Eastern the Segment is38 tectonically principally buried, crustallower portions Johansson, remnan of continental no relic nder sub nder ossibly Acceptedetamorphi Article

|

L

|

ower ower Overview c ed. ts of igneous olivine,igneous pyroxenets of t s of or UHP assemblages , Sveconorwegia to be ,

– - west

greenschist conditions Tibetan R unpublished data) sm continental continental emnants sediment ofclastic EasternSegmentWhile the represents ofaconti the lower plate is It The bedrockin exposed the internal section Segmen ofthe Eastern he location oftheS

approximately equivalent tothebasement subduct

rocks, rocks, t of Sveconorwegian the Front and associated deformationand associated )

7 the Easternthe Segment

eastwards –

likely that there 10 and removed byerosion. and removed

0.92 Ga caused intrusion ofamajor0.92 Gacausedintrusion intheeastern mafic dykeswarm part omparison withomparison theHimalayas and theSveconorwegian

allow

– ion the into mantle have beentectonicallyjuxtaposed bothbyshortening andextension from beneath Sveconorwegia he , , –

mangerite in Almesåkra the Group 2 mid plate behaviourplate

015 once is

– 4

a comparative a comparative during during the progressionof collision, continental the the remnant ofanorogenic plateau dle 4 O ). As no tectonic thickening has). Asnotectonic affected theafter bedrock 0.98

Figure are possiblare - km (Grad rogen

Figure present Sveconorwegian

in situ crust. crust.

veconorwegian veconorwegian would have – Figure (Rodhe, 1987 Mg tion, and0.98 once charnockite

20

and the orogenic prismand the accessible in Himalayanthe 10

-

, at , at ( By implication, – 1a), and 1a), readjustment along deformationzones between Cr peridotite

Figure and amphibole ( 40 km farther towards40 km foreland the farther b) was supracrustal cove was supracrustal , Tiira, &

ary ary 10 y . A ~ ,

overview 40 kmdepth. Present tectonic intercalations ofwet mantle fragments mak

)

of , and

rocks

O few occurrences (Fig s approached 80km, avalue similar tothatofthe

rogens the – 3 ; cp.alsoRodhe ing granite magmatismgranite 2009). (Brueckner, – , –

F 0.97 Gahigh ure and the 9

the location Groupthe oftheAlmesåkra

ESCWorking Group lower continentallower plate closer to are ront

) the lower lower the continental plate , , at the same the , at scale,

fragments .

took place 3) .

, however,

the total crustal orogenic thickness O

, (greenschist C.

ne orogenic prism is too deepfor at 10 at se

. The e Möller,

major difference rocks

– r abovethecrystalline basement of - which 15 km depth

grade metamorphismgrade and , in which in which following significant -

ultramafic rocks carrying rocks ultramafic present xposure 1988 day crustal thickness day crustal thickness beneath

were J. - facies conditions) Andersson would be a clear would beaclear in the hinterland. )

. folded andthrusted between the the between , any tobe cover W

must east ofthe 2009

high level ith the exception the of ith .

Sveconorwegian Sveconorwegian unconsolidated unconsolidated beneath beneath the Main is

nental collision - ; cp. have been

accessible in the levelof the of Eastern the and low ,

t was &

f

the p L. igure re

- signal is -

grade grade

. 13 of - For . or

This article isThis article by protected copyright. All rights reserved. recrystallizatio plate underthrusting the ductileresponding by highly deformation atanadvanced stage ofcollision, of alarge tract recrystallization experience theshow that metamorphism characterize herein 1998(Möller, surroundings, interior zone, deeper not ofthecollision records tectonometamorphiconly a break ofdisruption competent atthe30 structural state was widespread and Scandinavian Caledonides (e.g., been has in rocks documented thrust sh thethroughout collisional 0.99 stageat Ga. metastable, ineitherpristine a igneous apre or Although amphibolite highestin the M preserved 1996& Lindh, metagabb infiltration of hydrous fluids a distinct event ofmetamorphic recrystallization0.98 at ofWith the exception the 5.3.2 bein well a metastable unmetamorphosed 200 state Thrust km oftheMain Frontal north wedge hot partially molten crust ( deforming.ductilely nappebearing hadjust been partially crust exhumed, the mowas hot,partially and plate metamorphic zoning completion. Theairborne magnetic anomaly map oftheEastern Segment Himalayanthe comparison difficult is of that and continental underthrusting cp.

Accepted in etamorphic zircon Article

i the the Searle

ntru at 0.98 at | The lower continental plate: lowerThe a distinctmetamorphicsystem continental from Eastern the Segment that suggest the the India (Lesser and rheology ofthelower plate. Although syntectonicpartial mel ded bygranite roic rocks rocks roic

present in metagabbroin

, PhillipsElliott, a –

more extended

0.97 Ga Collectively the Collectively The eclogite The Eastern Segment alsoprovides information behaviourofpartial melt onthe

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This article isThis article by protected copyright. All rights reserved. Austin Andréasson, P. Andersson, J., Tual,L., Andersson, C., J., Möller, Andersson, J., Söderlund, U.,Johansson,L REFERENCES Insightful acknowledge as University, 30 Sweden opportunity the toparticipatein bedrockthe mapping program of the RoyalSwthe of GeologicalSurvey the Sweden (2004 by fromsupported grants order) (inchronological the SwedishResearch (1990’s), Council Thirty ACKNOWLEDGEMENTS tectonic ‘dry’between andhydrousultimately bedrock affect isexpectedreaction in ‘dry’ wedges, subduction(orogenic zones) athroughout mineralsof usedfor metamorphicalso reactions andmicro met differences system of witness progression metamorphismof equilibrate sedimentary zones wedgesandsubduction 1993) suggestingdata s

Acceptedwith Article Förhandlingar southern Sweden;Vättern, reinterpretation. a August 2017 orogen Sveconorwegian metamorphic evolution of crust eclogitized Shield.Baltic the along Mylonite Zone amajor (S.Sweden): Sveconorwegianterrane boundary in the Research Shield:Baltic constraintsfrom graniteintrusion. aMesoproterozoic Grenvillian) deformation,metamorphism formation andleucosome SW SW in Sweden, Support for extensiveSupport terrane. an eclogite in centralEclogites the part of the SveconorwegianSegment Shield: Eastern oftheBaltic years years amorphosed crust amorphosed .

years of r

Hegardt, E.A., Cornell,D.,Claesson, L.,Simakov,S S., that is that MSc atthe andPhDstudents Department ofGeology, LundUniversity.

in SW Sweden systems with manywith colleagues

reviews byR that continental and re between ‘dry’between andhydrous crust at otheruniversities, and at ,

P edish Academyedish Science(2014) of 98 H

every quite differentquite fromwed orogenic – - ydrous fluidisabundant ydrous . G., , 151 T esearch , but also how how , butalso

To besubmitted tructural coherence Precambrian ResearchPrecambrian

- , path path equilibrate beginning comparably at low

112 one & Rodhe,A. age determination –

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, toomany name to we should The data data The

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scale processes in processesscale in the rocks the Indian plate beneath Indian plate Himalayasthe the (Zhaoetal.,

. Geology of Protogine zonesouthof the Lake e.g. – i , . L. reported above th

n mostmetamorphic systems, e.g.metamorphosed

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, and igneous

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here ; Gerbi Pb and REE zircon record zircon Pb andREE ofthe the the Zircon Zircon chronology ofmigmatite gneisses 147. Assumption of continuous equilibration

- not only would not have been possible without beenpossible would nothave saturatedmetamorphic environments not only the improved paper. the , 221 metamorphic ,

from t origin at theat Department ofGeology, Lund

igneous

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a metamorphica records

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se large , 2010)

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bear bear -

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This article isThis article by protected copyright. All rights reserved. Table S1 AcceptedDataset.xls/x Figure S2. ofdatabase Geological SurveyofSweden. the Figure S1 this Additional Supporting Information maybefoundonlinein the supp SUPPORTING W.,Zhao, K.D., Nelson, Wang, X. Wang, X.D., Wahlgren, C. S., Vorhies, & A Unsworth, M.J.,Jones, A.G.,Wei,W., G., J.E, Marquis, Gokarn,S.G.,Spratt, C., Ulmius, Möller, J., ArticleUlmius, Andersson,J., J., Tual, L.,Pitra,P., Tual, L.,Pinan Tual, L.,Pinan M.B.,Wahlgren,Stephens, C. M.B.,Stephens, Söderlund, U., Isachsen, C.A.,G.,Heaman, P.J.,Vervoort, Bylund, Patchett, J.D. L., evidence forevidence continental underthrusting southern Tibet. beneath Precambrian Research, 92 hig Southwestthe Swedish Region. Granulite Sweden. partstructure in theeastern oftheSveconorwegian Orogen,BalticShield, south Barrovian zones, Scotland. frommagnetotelluric data. INDEPTH JunePrecambrian Research 2017 acrossthegeochronology southernmost SveconorwegianProvince. ofSveconorwegian reworkingboundary Baltic Shield, inthe defined by SWgneisses, Sweden. 1.45Gainat continent P Baltica: orogen, SWSveconorwegian Sweden. Precambrian Research, 265, s Precambrian Research, 265 s southwesternShield, Sweden. transpressive deformation its tectonic and implications, Sveconorwegian orogen, Baltic Sweden. orogen, intra Contributions Mineralogy to andPetrology maficconstraining repeated magmatism from FennoscandianShield 1.6to0.9Ga. inthe Andersson, U.B. hear hear hear article. h - - pressure granulite

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& - eographic eographic location eographic - H., Cruden, A.R., MT team - - Llamas, C.(2015). A.,&Möller, Llamas, C.(2015). A.,&Möller, Lindh, A. - & gu INFORMATION arc spreadingarc asubduction in above boundary a 2.0 & Andersson, J. Andersson, e, J.(2011).Pressure e e ( Precambrian Research,264 Precambrian clogite clogite Möller, C. 2005 Page, L., Johansson, L.,&Ganerød,M. Page, L.,Johansson,

distribution pointsof available maps bedrock in observations and ( & 2005 ) - Precambrian Research, 265 ( & .

1996 and upper and upper Project INDEPTH Team - - U b b Möller, C. ns illustrated oftherocks in F , 319 earing earing – - Nature ) Journal GeologicalJournal SocietyofLondon,168 of the H., Weijermars,H., R., . Crustal rheology of HimalayaTibet andsouthern the inferred , 104 Pb baddeleyite agesPb baddeleyite sand

) (2017). 104 & map

: Temperature ( Precambrian 79 Research, 2015 – Stephens, M.B. Stephens,

339. – – ; – f f

, 120. 120. T evolutionandSIMS U of s revision almostrevision beresubmitted completed, soonto old old

amphibolite facies rocksfrom SW Sweden 4 , 67 ) 38 ( P . Migmatization related tomafic and underplating –

2015 amples ofFe – n n temperature evolution andthermal regimes in

Journal ofJournal Geology Metamorphic , 78 T evolutionof Precambrian inthe eclogite appe, Sveconorwegian appe, Sveconorwegian – 91. European JournalofMineralogy ) –

. , – 81.

Hallandian Hallandian metamorphismhigh temperature 150 pressure of investigation the of southern part , 235 High High

& ( , 174 1994 ( – Cruden, A.R. 1993 - , 10 - - 257. Ti t t emperature emperature – Hf ) -

. 194. – richmetagabbro ) Kinematics ofamajor fan

39. – igures 4 . DeepSeismic reflection , 261 Nd isotope isotope chemistryNd –

( Pb zircon agesofPb zircon aluminous submitted U – o o 279. – Nature rogen, Sweden. rogen, Sweden. rogen, ( – orting orting information tabfor d d Pb andSm 199 – 8. eformation the in eformation the in 1.8 Gaaccretionary Submitted to

6 ) , ). . Left .

366 , 35

40 The eastern Ar/ , & –

, 557 , 493 - 8 , 1147 Nd dating of Nd dating lateral 39 . , 51 the Ar - central – – – - 559. & 515 67. like like – b b

1166. . asal asal as

.

al al

This article isThis article by protected copyright. All rights reserved. (olive Zonegranite. (c)Migmatitic 5(Cpx). garnet amphibolite withtonaliticleucosome. 4 Zone at976dated Zone ±7Ma. (b)gneiss, 5(Cpx). granitic Migmatitic protolith is1.39Ga migmatitic gneiss Figure 6. amphibolite, of consisting greenhornblende, garnet, metagabbro. Deformedgarnet (e) gneissose.strongly (c)Well weakly deformed K mm,20 for scale Figure 5. w biotite; small garnet euhedral crystals, toosmall largelygrains replaced byblue metagabbro (zone the reflects origin as coarse blue (zone 1). (zone feldspar Figure 4. deformation andmetamorphicrecrystal Front marks(SF)Sveconorwegian theeasternlimit ofnon orange)(shaded SegmentEastern andthe westgently ENE;aretowards zones preliminary extrapolated toareasnorth metagabbrorich to~850°C°C intheeast west. inthe zonesare Metamorphic onassemblages based inFe softened contrast).Zones1 airborne magnetic anomaly map ( Figure 3. anomalymap ( Eastern the Segment inTable (sources 1),overlain onsoftened Figure 2. in Fig sectioncross eclogite (2015); schematic cross etal.,2016 Laurent Survey (source: NASA).Tectonic map (c). orogen(based oftheSveconorwegian onGeological from etal. (2015). Compos Möller positions inset to scale subdivisions reconstruction byCawood, orogeny Sveconorwegian Figure 1. FIGURE CAPTIONS ANDTABLE

Accepted amphibole ith in outermostthe Article - green hornblende (Am), biotite, plagioclase (Pl), andFe 2

ure Hbl). Metagabbro partlypreserved(d) with clinopyroxene igneous grains and (dark), ). (c) Thin section ofdeformed andmetamorphosed consisting (zone 1) gabbro of s - of Sweden andNorwaydatabases megacrystic granite transected byN

s 2 (b) Deformedmetagabbro, plagioclase

in Metamorphism anddeformation 4 zones in Metamorphism anddeformation section) zone3(the transitional in Metamorphism anddeformation 1and2(thefrontalwedge).(a)K zones in Metamorphic oftheSegment zones Eastern overlain 1c), ongreyscale Figure (cp. Location Tectonic Plate andregionalsetting. reconstructionat (a) -

, a collisional a collisional orogen dipping dipping

following 3 and9. (lower right), and (lower the orogenic reconstruction in Fig ( transparent with white Sveconorwegian the orogen inpink) differential field; - - section. subdivision Internal positioned bearing nappe i . (n=

(c with amphibolite 1.68layers. Protolith is Ga granite,migmatization is 2), with relict igneous textureand plagioclase laths, andpyroxene igneous s ), withthe - )

2 Mylon feldspar augengneiss. Lightfeldspar granitic reddish gneiss,recrystallized and of U –

76 (

f) are parts ofthef) are same Rivers Rivers (2008) ) – of weste [ Pb dates of Sveconorwegian metamorphic ofSveconorwegian Pb dates migmatite and zircon in unpublished compilationunpublished byB.Bingen, based

– ite Zone ite (MZ, line) red isthe l - Nemchin, Prave, Strachan, structurally

- to medium 8 represent gradually increasing metamorphic from grade, ~550 a preserved coarse ~ Eastern Segment in medium violet to shades grey anda dark - 75 kmwide prof green amphibole. Fe rn Sveconorwegian terranes, : India n darkest violet. markRed bars source: Geological ofSweden). Survey part part pyroxene.of pseudomorphsafter the - differential field; rich ite

] satellite photographsatellite ofAsia inorthographic projection . (b) Schematic Schematic representation. (b)

- metagabbro. (f)Thinsectionofgarnet -

style lization. immediately grained gabbro. (d) (d) gabbro. grained ; d versus –

istribution of1.05 - of the Eastern Segment

S grained gabbro. (d)Garnet metagabbro body.metagabbro Recrystallized (a) and -

ile betweenthe areasile coastal and130 km - striking, steeplyductileshearstriking, dipping zones to be seen in to in overview, beseen this occurtogether rich rich in the top upper

source: source: intracontinental underthrusting -

plagioclase, biotite above theEastern Segment. Ti – 6 (thesection).(a)Stromatic internal & - oxide aresurroundedby grains

Kra ithotectonic boundary between the - penetrative Sveconorwegian penetrative Geological Survey ofSweden; Thin section with - bbendam, Ti – greyscale greyscale airborne magnetic

the the location of schematic the - and south 1.02 Ga granites from1.02 Gagranites oxide. The domain texture

ure the the TerraneIdefjorden the endthe of Grenvillian the of 10b.marks Box area the et Möller al. after part of photo the continent Baltica (

and Fe 2007)

- on the of undeformed , rich coronitic

of profile. this The at

- ; two alternative two alternative porphyroblastic

; metamorphic (a) - Ti – . Modified (e) coin, (e) coin, oxide. -

,

- Ti – This article isThis article by protected copyright. All rights reserved. Sveconorwegian Figure 10. south the represent Front)of is Sveconorwegian the line,and e black the TerraneIdefjorden andtheEastern Zone, Segment Mylonite isoutlined (the MZ) byasolid fold folds withsubhorizontal NE polyphasally recumbent folds folded byearly with E Figure West(cp. 1c). frontal ofthe wedge whiteline dashed A rocks. Transscandinaviandeformed) is the area Igneousand associated Belt Survey ofSweden), illustrating large the Figure 9. exhumation.partial conditions, before tecto garnet cores P symplectite rimson the of a clinopyroxene, corundum,sapphirine, anorthit and equilibrated decompression, during which formed symplectitic (sy) reaction rims of zone. (c) Th nappe.bearing High (b) folded stromatic leucosome boudin thepart in internal of andamphibolite eclogite the Figure 8. assemblage age 1.7Ga) rich in metamorphic clinopyroxene, definedand foliae bythe samemi oxide, plagioclase (partly antiperthite), microperthite, andquartz. (f) Felsicgneiss(protolith clinopyroxene charnockite (protolith age1 clinopyroxene grains characteristicall 8, with melt) inclusions blast in migmatitic garnetcharacteristic amphibolte, of zone8.(c) Inclusion leucosomeand feldspar s quartz) Thin coronas ofclinopyroxene (green), hornb Orthopyroxene Figure 7. Zone 6(Opx). (brown), with Cpx),biotite Fe intergrown clinopyroxene garnet (green), red), plagioclase(light (white),orthopyroxene (reddish coarse relict (white), and green).Zone6 Thinsectionoforthopyxene (reddish me(Opx). (f) metamorphicgrained clinopyroxene (reddish), (green), garnet antiperhiticplagioclase metagabbro withremnants ofigneous clinopyroxene (centresof domains), green rich in fine clinopyroxene andplagioclase.Zone Thinsection 5(Cpx).(e). ofmoderatelydeformed plagioclaseigneous laths. isrich (red)and Therock in garnet contains metamorphic –

AcceptedT Article

hinges, hinges, betweenstrainentrained high limbs.

path recorded by the eclogites recordedbytheeclogites Pitra,&Möller,path (Tual, ; small patches of ; small patches in leucosome relict originally coarse ~

Airborne magne The eclogite Metamorphism anddeformation 7 zones in 20 in clinopyroxene the blast Vertical sectionsVertical acrossthe front

in section ofin section kyanite as in -

and the first ofSveconorwegianmetamorphism,and the record amphibolite at grained igneous texture, completely bymetamorphic replaced minerals: km wide

, orthopyroxene, garnet, olive, orthopyroxene,garnet, - megablast (dark,

O the ) is by ) is transected , occurring lo , occurring

rogens, portrayed the at same andvertical horizontal scale. Violet=

the the Phanerozoic Tornquist clogite

Varberg charnockite

-

corridor (the wedge)frontal we bearing Easternbearing terrane Segment. Migmatitic inthe (a) gneiss with hornblende nic burialat nic eclogite - tem tic tic anomalymap - .39 Ga) with foliae defined foliae .39 Ga)with by bearing nappe – perature mylonitic mafic gneiss with perature basal boudins inthe shear SW andN - grained texture igneous andremnants ofigneous cally 8 inzone -

shown urround orthopyroxene the blast brownish weathering) in leucosome amphibolite. garnet of , rutile

e aroundkyanite, orthopyroxene+plagioclase± N are also presentare also – are are y dusted byy dusted Fe S

- – in trending non -

composite S trending foldS trending axes. and corundum scale deformation The pattern. easternmost -

, (e). (E) light yellow. light Ti

the the nd plagioclase expulsion informernd plagioclaseexpulsion omphacite. (d) of the Eastern Segmentof Eastern the ( - - al parts oftheHimalayaal green hornblend - facies depth.

oxide (black), and lende (black), and garnet lende andgarnet (black), to (red, next shaded white Z

gneissic foliation isnear in garnet one The lithotectonic boundary the between . plagioclase (inferred +quartz tonalitic - (d) Garnet coronitic(d) metagabbro inzone with – - Ti – penetrative steeply di W fold axes upright trending andlater st oftheSveconorwegian Front (SF 8 (western internal ( section). - oxide. (e) Gneissicoxide. (e) The NW - bearing eclogite, bearing eclogite, re partly

porphyroblastic amphibolite.

Permian dykes. diabase

D1/D2 Sveconorwegian metamorphicSveconorwegian 2017). . The Almesåkra Group(A;east e, reddish browne, reddish biotite, Fe

Note the presence of isolated presenceofisolated Note the hornblende green). (olive –

. 10 (b) megablast cm garnet mark SE SE D i

– s represents inclusionsrepresents in

striking striking ource: Geologicalource: Tibetan and Tibetan 1. - deformation during deformation during - rich 9 penetrative and – 1.7 Gaigneous pping foliation pping foliation Varberg Varberg

clinopyroxene lineaments in tagabbro with tagabbro

amphibole - neral - facies a ) (less (less - - green, green, The

- Ti ;

- This article isThis article by protected copyright. All rights reserved. Accepted Article Table 2. quoted age intervals in the the headings or in main text. analytical the spots; latter are referred Ga. toin >20Ma Ages witherrors not are included in inMa,given 6dates except based onlower that are discordia orintercepts than onless four meltingpartial Eastern Segment inthe Figure withnumberedreferences asin 2.Ages are Table 1. Zone.Mylonite 1c.Extruded eclogitFigure marks ofthepresent approximate depth the erosional surface along profile the marked in Sveconorwegian Thrust; MFT=Mai boundary Chung (2011).STD=SouthTibetan Detachment; Thrust; MCT=Main Central MBT= Main acrosssouthernsection the Himalayan Red dashedline underthrusting

Metamorphic assemblages inFe 1.U Table continental crust; light yellow

= 55km where depth O rogen at the rogen atthe completion of at collision – Pb zircon dates ofPb zircon metamorphic Sveconorwegian recrystallization and e - n Fronta bearing darknappe in violet;SF= Sveconorwegian Front;MZ= l Thrust – mafic rocks N transformeclogite. into (a): Tibetan Tibetan - Ti - = orogenicprism; orange= . (b):E rich metagabbro, 1 zones O rogen after Elliott, after rogen Phillips,Searle, and – W cross

c . 980 Ma. The blue dashed . 980 dashed line Ma. Theblue - section across the eastern –

8. overriding continent.

– S cross - This article isThis article by protected copyright. All rights reserved. * 13b 19 8c 18b 4c 11c 11b dykes: 0.96-0.93and veinsGa granitic and pegmatitic Post-kinematic 18a 17 16 15 10c 14 rocks:felsic Ga0.96 deformed (unclassified) in zircon Metamorphic 13a 8b 12b dykes: 0.96-0.95and veinsGa as syn-kinematic melt of Crystallization 20 12a 11a 10b 10a 9b 9a 8a 4c gneiss Granitic 7b 7a 3b Garnetamphibolite of Crystallization 6 5 4b 4a Eclogite 3a 2 1 garnet- amphibolite Amphibolite 1.00-0.97 Ga gabbro: of recrystallization Metamorphic rocktype and 1 Figure in ID text. headingsmainthe theor inin are referredquotedlatter areerrorsincludedinwiththeMa agenot >20 intervals Ages Ga. in spots; four thanto analytical less areoron basednumbered onlower that intercepts aredates discordia6 given references Ages Figure in except 2. as Ma, in 1. Table Accepted age evaporation Pb-Pb Article Undeformeddyke pegmatite dyke pegmatite cross-cutting Post-kinematic dyke pegmatite cross-cutting Post-kinematic dyke granitic Post-kinematic gneiss migmatitic in leucosome Post-kinematic dyke pegmatite cross-cutting Post-kinematic dyke pegmatite cross-cutting Post-kinematic aplite-granite dyke Gneissic Foldedandboudinaged dyke pegmatite orthogneiss granitic Migmatitic orthogneiss granitic Migmatitic deformedFolded andstrongly pegmatite eclogite deformedin Strongly dyke felsic amphibolite-gneisscontact at mobilisate Leucocratic fillingboudinagedin Pegmatitic amphibolite pegmatite kinematic Late orthogneiss migmatitic Stromatic gneiss granitic Veinedleucocratic migmatite stromatic in leucosome Syn-kinematic quartofeldspathic gneiss Migmatite quartofeldspathicSillimanite-bearing gneiss migmatite orthogneiss migmatitic Eclogite-bearingstromatic augen gneiss migmatitic Stromatic augen gneiss Migmatitic orthogneiss bearing stromatic Eclogite garnet amphibolite Migmatitic garnet amphibolite Migmatitic Veinedgarnet amphibolite (retrogressedAmphibolite eclogite) andFe-Ti-rich eclogite Kyanite eclogite melting Layered Fe-Tiincip. eclogite, Fe-TiIsotropic eclogite Garnetamphibolite Garnetamphibolite garnetFoliated amphibolite U-Pb zircon dates ofwith SegmentSveconorwegian dates Eastern U-Pbzircon the inand partial melting recrystallization metamorphic in situ in partial melt: 0.98-0.97 Ga melt: partial Överlida GällaredN Vistbergen Mårdaklev Oxanäset Stensjöstrand Stensjöstrand skog Skene Tångaberg Byasjön Målsryd Stensjöstrand Stensjöstrand Buskhult Viared Ammås Bollebygd Bollebygd Kånna Herrestad Åker Locality Kullaberg Stensjöstrand Sundhult GällaredS Kornarp Högabjär Högabjär GällaredS Glassvik Våxtorp Söndrum Stensjöstrand Ammås Kullaberg

1000-970 9787 ± 9854 ± 97425± 9707 ± 100668 ± Ma in Age 9346 ± 946+6/-4 947±12 9567 ± 9567 ± 9457 ± 9527 ± 980 96927± c. c. 9587± 96322± 9616 ± 95421± 96113± c. Ga0.97 c. 9767 ± c. 9705 ± 96913± 96813± 99224± 9766 ± 9684 ± 9704 ± c 93640± . 0.97 Ga0.97 . 0.97 Ga0.97 Ga0.97 Ga0.97 Ga0.97 ± 4 * Andersson et al. (2017) al. et Andersson (2015) al. Mölleret (2015) al. Mölleret (1998) al. et Wang (2017) al. et Beckman (2004)Söderlund al. et Söderlund et al. (2008b)Söderlund al. et Christoffel(1999) al. et (1999) al. et Andersson Söderlund Möller& (1997) (2015) al. Mölleret (2007) al. Mölleret (2007) al. Mölleret (2002)Söderlund al. et Söderlund(1996) Lundqvist(2007) al. et (2007) al. et Rimsa (2015) al. Piñan-Llamas et (2001) Johanssonal. et (2008b)Söderlund al. et (1999) al. et Andersson (2002)Söderlund al. et (1996) al. Connelly et (2002)Söderlund al. et (2007) al. Mölleret (2015) al. Piñan-Llamas et Pi (2002) al. et Andersson (2002) al. et Andersson (1999) al. et Andersson (2015) al. Mölleret (2015) al. Hansen et (2015) al. Hansen et (1998) al. et Wang (2005)Hegardt al. et Austin ñ an-Llamas et al. (2015) al. an-Llamas et

This article isThis article by protected copyright. All rights reserved. Table 2. Table AcceptedGarnet,4-20 cm Clinopyroxene,0.5-3cm Orthopyroxene,2-10 cm Garnet,0.5-2cm amphibolite garnet migmatitic in blasts leucosome in Mineral ArticleOrthopyroxene Antiperthite Clinopyroxene Rutile Olive-greenhornblende Greenhornblende Garnet Fe-Ti-oxide Plagioclase Titanite Epidote Blue-greenhornblende metagabbro non-migmatized in assemblages Metamorphic Metamorphic assemblages in Fe-Ti-richin assemblages Metamorphic metagabbro, 1–8. zones Zone

X X X X X 1 X X X X X X 2 (X) X X X X 3 X X (X) (X) X X X X X X 4

(X) X X X X X X 5 (X) X X X X X X X X 6 (?) X X X X X X X X X 7 (X) X X X X X X X X X X X 8

This article isThis article by protected copyright. All rights reserved. Accepted Article

This article isThis article by protected copyright. All rights reserved. Accepted Article

This article isThis article by protected copyright. All rights reserved. Accepted Article

This article isThis article by protected copyright. All rights reserved. Accepted Article

This article isThis article by protected copyright. All rights reserved. Accepted Article

This article isThis article by protected copyright. All rights reserved. Accepted Article

This article isThis article by protected copyright. All rights reserved. Accepted Article

This article isThis article by protected copyright. All rights reserved. Accepted Article

This article isThis article by protected copyright. All rights reserved. Accepted Article

This article isThis article by protected copyright. All rights reserved. Accepted Article