Evolution de la température de la transition fragile-du tile ave la profondeur 174

de ette étude. Il est évident qu'une unité issue d'une zone de subdu tion va présenter, omme 'estla as pour l'unité Adula [Daleand Holland,2003℄,un gradient de pressionde son frontvers sazonede ra ine.Dans e as, lepi de pressionmétamorphiqueleplus pertinent est lavaleur la plusélevée depressiontrouvéeaufrontdel'unité.Apartirdu modèle,ilest possiblede onstruire des aba s présentants la profondeur minimum d'é aillage en fon tion de l'angle et de la vitesse de subdu tion (gure 11.10). En replaçant sur de tels aba s des valeurs de pi de pression bien

Fig. 11.10  Profondeur mini-mum d'é aillage.

La profondeur minimum d'é aillage est al ulée en fon tion de l'angle et delavitessedesubdu tion.

ontraint spatialement,l'angle et lavitesse de lasubdu tion, au moment de l'indivdualisationde l'unitéd'où provientlamesure thermobarométrique,peuvent être estimées. L'évolutiond'un slab an ien peut don être retra ée en disposant des valeurs de pression au front des unités é aillées ( hapitre12).

11.8.2 Evolution de la température de la transition fragile-du tile ave la profondeur

L'étudedel'évoltionthermiqueetrhéologiqueenfon tiondel'angleetlavitessedesubdu tion amontréquel'individualisationenprofondeurd'unité rustaleau oursdelasubdu tion ontinen-taleétaitdéterminerparlatransitionfragile-du tile.L'évolutiondelatempératuredelatransition fragile-du tile en fon tion de la profondeur a don été al ulée pour les trois rhéologies utilisées dans la roûte : 1-Plagio lase anhydre, 2-Quartz hydraté et 3-Granulite ma (tableau 11.11 et gure11.12).

Latempératurede latransitionfragile-du tilediminueave laprofondeur quelquesoitla rhéo-logie. Cette tendan e tend à limiter l'eet de la vitesse d'enfouissement qui régie la profondeur d'é aillage.Eneet, plus l'angleetlavitessede subdu tionsontgrands, plusl'évolution est adia-batique et onduità un é aillage plus profond. La diminution de la température de la transition fragile-du tileave laprofondeur tend à diminuer laprofondeur minimum d'é aillage.

A

(

M P a.s−1

)

Q

(

kJ.mol−1

)

n

Réferen e 1

3, 2.10−4 238, 0 3, 2

Ranalli2003 2

3, 2.10−4 156, 0 2, 4

Thullis1980 3

1, 4.10+4 445 4, 2

Wilks 1990

Fig. 11.11 Paramètres rhéologiques utilisés 1-Plagio laseanhydre,2-Quartzhydratéet 3-Granulite

ma

Fig. 11.12  Evolution de la transition fragile-du tile.

explique l'impa te de la rhéologie sur l'évolution de l'individualisation notament on ernant la profondeur minimum d'é aillage.

11.9 Perspe tives

Le modèle présenté dans et arti le asso ie une modélisation thermique 2D lassique et une étude de for e à l'équilibre. Cette asso iation présente l'avantage de modéliser onvenablement le plan de subdu tion, assimilé à une faille, e qui est a tuellement impossible ave les modèles thermomé aniques.Enrevan he,l'in onvénientinhérentàl'absen ededéformationdanslemodèle provientdeladi ultéàestimerleseuilde déta hement del'unité:dans notreétude,nousavons supposé que l'unité avait la possibilitéde s'é ailler si larésistan e était inférieure à la ontrainte appliquée et que l'unité se déta hait probablement lorsque la ontrainte appliquée était dix fois supérieure à la résistan e. En réalité, seule une étude en déformation de e gradient inverse de résistan e pourra déterminer la valeur ritique à partir de laquelle l'é aillage est possible, ette valeur étant ertainement ontrlée par lavitesse de subdu tion.

Impli ations géodynamiques  Arti le 3 :

Signi ation des variations latérales du pi

de pression métamorphique

Ce hapitre orrespond àun arti leen préparation,il est don rédigé en anglais.

Sommaire

12.1 Introdu tion . . . 178 12.2 1D model: inferred burial velo ity from peak pressure . . . 181 12.3 2Dmodel:inferredsubdu tiondipangleandvelo ityfromsta kunit

length . . . 182 12.4 Impli ationfortheEo enekinemati sand3DgeometryoftheAlpine

slab (45-35 My) . . . 183 12.5 Con lusion. . . 184 Lamodélisationdelasubdu tion ontinentale d'unemargepassivemontrel'impa tedel'angle d'enfouissement et de la vitesse de subdu tion sur les dimensions et la profondeur des unités individualisées au ours de ette subdu tion (Chapitre 11). Cette variabilité de la profondeur d'individualisationen fon tionde la dynamique etde lagéométrie de la zone de subdu tion doit permettre, à partir des mesures de pi de pression, d'estimer l'angle et la vitesse d'une an ienne subdu tion.C'est equenousproposonsd'étudierdanslasuitede e hapitreàpartirdel'exemple des unités internes Briançonnaises (Alpes).

Cette partie est rédigée sous forme d'un arti le (en préparation) dont une version vulgarisée est disponible en Annexe 2 (Arti les vulgarisés).

Signi an e of lateral variation in peak metamorphism within modern orogens In prep. N. Carry

1

1 , F. Gueydan

1

,J.P. Brun

1

, D. Marquer

2

1

EquipeLithosphère,Géos ien esRennes(UMR-CNRS6118),UniversitédeRennes1,F-35042RennesCedex,Fran e.

2

Géos ien esEA2642,UniversitédeFran he-Comté,16routedeGray,F-25030Besançon.

Abstra t

HP/UHP and LTmetamorphism is often observed in the inner partof modern orogens. These grades of meta-morphismindi ate ontinental subdu tion responsible for deep burial of ontinental units that are subsequently exhumed.Beyondthedebate ofmetamorphi ro kexhumation,workneedto bedoneto quantify in 3Dthe geo-metryandkinemati sof ontinentalsubdu tionsu haslateralvariationsofpeakpressurewithinanorogen.Using numeri als modelling we show that during the subdu tion of Briançonnais terrane in the Alps, the subdu tion dip angle and velo ity were larger in the southwest part (

α = 40o

− 50o

, Vc = 2− 3cm.y−1

for Dora Maira) than in the northeast part (

α = 20o

, Vc = 0.5− 1cm.y−1

for Suretta) with onsistently average value between (

α = 30o

, Vc = 1− 2cm.y−1

for Gran Paradiso). This lateral variation of geometry and kinemati s of the sub-du tion quantied for the Eo ene time explains the lateral variations of peak pressure observed in the internal rystallinemassifs oftheAlps.

12.1 Introdu tion

HP/UHPand LTmetamorphismisoftenobserved intheinner partofmodernorogens. These gradesofmetamorphismindi ate ontinentalsubdu tionresponsiblefordeepburialof ontinental units that are subsequently exhumed. A lot of studies have fo used on pro esses responsible for exhumation of HP/UHP metamorphi ro ks, and these remain a matter of great debate. Beyond the debate of metamorphi ro k exhumation, work need to be done to quantify in 3D the geometry and kinemati s of ontinental subdu tion. For example, lateral variations of peak pressure of metamorphi ro ks withinan orogenare ommonbut stillrelatively poorlydis ussed and onstrained. To illustrate that point, we have hosen the Alpine example . The so- alled Briançonnais units from south tonorth Dora Maira, Gran Paradiso and Suretta belong to the InternalCrystallineMassif(ICM, gure12.1b).Theseunitshavenomajorlithologi aldieren es andare originallyfromthe distalpart ofthe European margin(Figure12.1a).Althoughthesame originalpositionoftheseunits inthe subdu ted passive margin,large dieren es inpeakpressure are observed. The peak pressure (gure 12.1 ) de reases fromUHP inDora Maira(37-47kb and 700-750

oC

[S hertletal.,1991;Hermann,2003℄)toHPinGranParadiso(17-20kband500-550

oC

[Le Bayon and Ballevre, 2006℄) and nally MP in Suretta (10-13 kb, and 400-450

oC

[Nussbaum etal.,1998℄).Theagesofthepeakpressurein reasesfrom38MainDoraMaira[Tiltonetal.,1991℄ to43Ma inGran Paradiso[Le Bayonand Ballevre, 2006℄and 46Ma inSuretta[Challandes etal., 2003℄.This non- oevalpeakpressure forunit atsamestru tural position inthe European margin an be explained by dierent length of Liguro-Piemontais o eani lithosphere (gure12.1a). The Liguro-Piemontais o eans was indeed larger in the southern part of the Alps, requiring a larger

1

time ne essary for o eani losureto o ur. In ontrast, the Liguro-Piemontaiso eanwas narrow inthe entralAlps,leadingtorelativeshort losuretime[Stampiand Borel,2002℄.Despitethese dieren es intheages ofpeak pressure,wewish toquantitativelyunderstandthe ausesofstrong lateral variationsin HP/UHP re ordin the ICM.

To that end, we have used simple 1D thermal modelling of prograde PT path in order to quantify the burial velo ity from PT onditions. We dis uss variations in both subdu tion dip angle and subdu tion velo ity to explain lateral variation in peak pressure. Further onstraints are given by a 2D thermal analysis that relate the length of deta hed unit from the subdu ted margin with the subdu tion dip angle and velo ity. The ombination of these two approa hes allowus to onstrain the lateral variationsin subdu tion geometryand kinemati s atthe time of HP/UHP metamorphism.These ndingsallowus then to onstru t a3D stru ture of the Alpine slab at Eo ene time.

Fig. 12.1  a-Palaeogeographi map of the Liguro-Piemontais o ean at Eo ene time by Stampi [Stampi and Borel, 2002℄. b-Map of the internalpart of the Alpsmodied after S hmid [S hmid et al., 2004℄. PT onditions for Briançonnais units are from Baudin and Challandes for Suretta [Baudin et al., 1993; Challandes et al., 2003℄, Le Bayon for Gran Paradiso [Le Bayon and Ballevre, 2006℄ and from S hertl and Hermann for Dora Maira [S hertl et al., 1991; Hermann, 2003℄. Ages are from Challandes, Le Bayon and Tilton [Challandesetal.,2003;LeBayonandBallevre,2006;Tiltonetal.,1991℄respe tively. The length of the units are measured from the map and orre ted to a ount for post-sta king thinning. Theamountofthinningwasassumed tobearound1.5. LengthsofSuretta, Gran Paradiso and Dora Maira at the time of the sta king are thus 25-30km, 35-40km and 37-42km, respe tively. -PT diagram with peak onditions for the three onsidered units and isolinesof

Vb

omputedby1Dthermalmodellingofsubdu tion.Seetextforfurtherdetails.

12.2 1D model : inferred burial velo ity from peak pressure

A rst order insight to the ee ts of variations in subdu tion velo ity and dip angle an be a hieved through a 1D thermal model of prograde PT path. The 1D model orresponds to a transient ondu tive modelof athinned ontinentallithosphereundergoing subdu tion. Constant mantle heat ux is applied at the bottom while a top temperature is applied at the top of the subdu ted lithosphere.The top temperature isevolvingthrough time asfollows. At a given time t,the burial depth

zb

of the top of the subdu ted lithosphere is dire tly related to the burial velo ity

Vb

(

zb = Vbt

). The top temperature isthen the temperature given by a steady geotherm at the burial depth. The top temperature thus in reases with time as a fun tion of

Vb

. Starting from a steady state, the temperature prole within the subdu ted lithosphere evolves through time be ause of the in rease in top temperature, dening lassi al reversed temperature prole. The temperature of a rustal pie e initially at 15 km depth within the subdu ted lithosphere is followed through time, dening the prograde path. When the rustalpie e rea hed its maximum burial depth, the parti le is assumed to remains at that depth during a ertain time interval, dening the residen e time. During that residen e time, the temperature of the rustal parti le tendstowardsitsthermalequilibriumand thusin reases.Foragivenburialvelo ities,severalruns are performed at dierent maximum burial depths in order to onstru t the isolines of verti al burial velo ities (Figure 12.1- ). Note that these isolines are not prograde PT paths be ause of heating during residen e time. The

Vb

isoline is older for larger burial velo ity

Vb

, be ause the faster a rustalpie e enter subdu tion, the moreadiabati isits transienttemperatureevolution. Readers are referred toGueydan etal., inprep. for further details.

From these results, peak pressure and related temperature (end of burial)for the three onsi-dered units an be used to onstrain their burial velo ities. The dieren es in peak pressure are then likely related to variations in burial velo ity. Burial velo ities are thus in reasing from Su-retta (

Vb = 0, 2 − 0, 4cm.y−1

) to Gran Paradiso (

Vb = 0, 4 − 0, 6cm.y−1

) and is maximum for DoraMaira(

Vb = 0.6 − 2.0cm/yr

).Notethat the largeun ertainties inthe value ofpeakpressure for Dora Mairaindu esun ertainties inburial velo ity. The inferred variation in burialvelo ities

Fig. 12.2  PT datas interpretation

Vb = Vcsin α

. Assuming a given subdu tion velo ity of

0.5cm.y−1

[S hmid et al., 1997; Stampi andBorel,2002℄, the in rease in

Vb

fromSureta toGranParadisoand Dora Maira an berelated to an in rease in sudbu tion dip angle (Figure 12.2-a). The estimated dip angle is

20 − 50o

for Surettawhileitis largerthan

50o

forGran Paradiso.However, large values of

Vb

forpart ofGran Paradisoand forDora Mairayieldsunlikelyestimated subdu tiondip anglesthat are larger than

90o

. The assumed subdu tion velo ity is thus not large enoughto explain largevalues of

Vb

. The other assumption to explain variation in

Vb

is thus variation in subdu tion velo ity

Vc

at onstant subdu tion dip angle (set here to

α = 40o

, Figure 12.2-b)). This assumption yields sudbu tionvelo ityaround0.5

cm/yr

forSurettaandaround0.8

cm/yr

forGranParadiso,whi h is onsistent with known onvergen e velo ity between Afri a and Europa (S hmid, 1997). In ontrast, estimated subdu tionvelo itiesfor DoraMairaare signi antlylarger, rangingbetween

1and 3

cm/yr

.

This1D modellingofprograde PT path thus onstrainsthe subdu tionvelo ityand dipangle for Suretta nappe. In ontrast, no unequivo al on lusion is obtained for Gran Paradiso and morespe i ally for DoraMaira. Results however likelyindi ate largersubdu tiondip angle and velo ity for Dora Maira. More generaly, in rease in burial velo ity

Vb

seems to be related to a oupled in rease in subdu tion dip angle and velo ity. In order to obtain further onstraints on subdu tion dip angle and velo ity,we propose to use ase ond type of modellingthat allowus to relatethe lengthof the sta ked nappes with

Vc

and

α

.

12.3 2D model : inferred subdu tion dip angle and velo ity from sta k unit length

A 2D ondu tive model of ontinental lithosphere has been developed in order to ompute transient temperature and strength evolution within the subdu ted margin (gure 12.3 - left). Boundary onditions are the same as the 1D model. The interest of the 2D modelling is rst to introdu e independently the dip angle and the subdu tion velo ity and to obtain 2D imaging of the strength evolution through time of the margin. A omparison of the margin strength with the a ting stress along the subdu tion plane allow us to predi t sta king (gure 12.3 - left). For further details,see Carry etal.,in prep.

A rustalpie eisassumedtodeta hfromthesubdu tedlithospherewhenitsstrengthbe omes lower than the a ting stress. The strength is shown rst to in rease with burial depth be ause in the early stage of burial history, the material remains brittle. Then, the above heating is su ient enough to indu e thermal weakening and the subdu ted material be omes du tile and its strength de reases with in reasing burial depth. A riti al burial depth an thus be dened at whi h the margin strength is lower than the a ting stress. Below this riti al depth, sta king isalways possible. This 2D modellingdenes potential sta king areas withinthe subdu ted plate and thus the dimension (length and thi kness) of the future deta hed unit. Figure 12.3 (right) shows numeri alresults presented as estimatedlength of sta ked unitsas afun tion of the burial depthfor 7dierentvalues of(

α, Vc

).Notethatbasedonthe above1D modelling,wehave hosen to in rease both

α

and

Vc

for the dierent 2D models. For a given value of (

α, Vc

), the length in reaseswith in reasingburialdepth.This featureo urs be ausethe riti alburialdepthbelow whi h sta king o urs does not hange with time. As a onsequen e, the length of the material below this riti al depth in reases through time be ause of downgoing subdu tion and thus the length of the future sta ked units in reases. An in rease in (

α, Vc

) yields a de rease in the unit length for the same burial depth be ause it favors adiabati evolution of the margin and thus redu es above heating. Usingthis 2D sta king analysis, the length of the three natural examples anbe omparedtothe numeri alresultsin ordertobetter onstrainthe valueof (

α, Vc

) forea h

Fig. 12.3  Left, the 2D results of temperature and sta king (logarithm ratio between a ting stress and strength

log10(σa/τ )

) at 7My is presented. The dash line orrespond to the presumed sta ked area. Right, Length evolution of deta hed unit as fun tion as burial depth,subdu tion dip angle and onvergen e velo ity.

nappe.

Length of Alpine units have been measured on the map and orre ted to a ount for post-sta kingthinningby afa torof 1.5.The omparisonof thenaturaldatawiththe modellingyields the following results.Surettats with adip angleof 20

Dans le document De la subduction continentale à l'exhumation dans les Alpes Penniques. Modélisations thermo-mécanique et paléogéographique. (Page 175-184)