The architecture of the European-Mediterranean lithosphere:
A synthesis of the Re-Os evidence
Jose
M. Gonzalez-Jimenez, Carlos Villaseca, William L. Griffin, Elena Belousova, Zoltan Konc , Eumenio Ancochea,
Y. O'Reillv , Norman J. Pearson, Carlos J. Garrido, and Fernando Gervilla
Suzanne
accessory metasomatic minerals (amphibole,
ABSTRACT
(TRD)
of sulfides in peridotite xenoliths from the subcon­
apatite, calcite). Interstitial glass commonly sur­
tinental mantle beneath central Spain (the Calatrava volcanic field) reveal that episodes of
rounds these metasomatic minerals and contains
Rhenium-depletion model ages
mantle magmatism and/or metasomatism in the Iberia microplate were linked to crustal
relics of them as well as incompletely reacted
growth events, mainly during supercontinent assembly and/or breakup at ca. 1.8, 1.1, 0.9,
primary silicates and newly fonned clinopyrox­
0.6, and 0.3 Ga. A synthesis of available in situ and whole-rock Os-isotope data on mantle­
ene, olivine, and spinel (Villaseca et al., 2010).
derived peridotites shows that this type of mantle (maximum
TRD of ca. 1.8 Ga) is widespread
in the subcontinental mantle of Europe and Africa outboard from the Betics-Maghrebides­
Appenines front. In contrast, the mantle enclosed within the Alpine domain records
TRD as old
Sulfides (1-500
J.Ull)
were identified in pol­
ished thin sections; they are enclosed in olivine
and pyroxenes, rarely at the triple junctions
as 2.6 Ga, revealing a previously unrecognized Archean domain or domains in the central and
between the main silicates, and more commonly
western Mediterranean. Our observations indicate that ancient fragments of subcontinental
in the interstitial glass. Major-element analysis
lithospheric mantle have played an important role in the development of the present architec­
by electron microprobe shows that all the sul­
fides are Fe-rich monosulfide solid solution,
ture of the Mediterranean lithosphere.
with Fe >38.9 wt% and Ni contents >9.93 wt%.
western Europe and Africa allows us to examine
There is no difference in comIX'sition between
Until now, the timing of formation and the
the evolution and architecture of the European­
included and interstitial sulfides.
evolution of the Iberian microplate has been
Mediterranean mantle, revealing a heteroge­
constrained mainly from U-Pb ages of mag­
neous mantle structure across the region and
matic zircons, Hf model ages of inherited zir­
indicating the presence of a previously unrecog­
cons, and whole-rock Nd model ages of crustal
nized Archean domain.
INTRODUCTION
igneous and metamorphic rocks. However, there
RESULTS AND INTERPRETATION
In Situ Re-Os Model Ages on Mantle
Sulfides
has been little robust information on the age of
GEOLOGICAL SETTING AND SAMPLE
the lithospheric mantle beneath this continental
BACKGROUND
The Os-isotope comIX'sitions of over 800
individual sulfides �SO J.Illl were rreasured in
crust; it is the missing key for a full understand­
The Calatrava volcanic field is an intracon­
ing of the geological framework of the Iberian
tinental zone within the Central Iberian Zone
of Excellence for Core to Crust Fluid Systems!
microplate. This gap has now been filled by
of central Spain, where upper crust only from
GEMOC (Macquarie University, Australia) fol­
determining the Re-Os systematics of sulfides
Neoproterozoic time has been preserved. The
lowing the procedures described by Pearson
in peridotite xenoliths that represent samples of
volcanic field comprises -200 small monoge­
et al. (2002). In our data set, only grains with
this mantle. Because Re and Os preferentially
netic volcanic centers. An initial minor ultra­
187Rej1880s < 1.2 were selected, thus ensuring
situ using LA-MC-ICPMS at the ARC Centre
concentrate in mantle sulfides, unlike those
IX'tassic event at ca. 8.7-6.4 Ma was followed
an accurate correction of the isobaric overlap of
lithophile elements commonly used in other
by the eruption of alkali basalts, basanites, and
187Re on 1880s. In our analysis we disregarded
isotopic systems in the earth sciences, their iso­
olivine nephelinites and melilitites from 3.7 to
grains with superchondritic 1870s/1880S (>0.1281;
topes are uniquely useful in tracking events of
ca. 0.7 Ma that entrained abundant deep-seated
Walker et al., 2(02) unsupported by their low
mantle melt depletion and refertilization.
xenoliths, dominantly spinel lherzolites of the
Re/Os, which yielded geologically unreason­
In this work we use in situ laser ablation­
Cr-diopside suite (after Wilshire and Shervais,
able future Re-Os model ages. Additionally, to
plasma­
1975), and wehrlites and pblogopite-rich clino­
ensure
mass spectrometry (LA-MC-ICPMS) to study
pyroxenites of the Al-augite series (Ancochea,
we used grains only with propagated 2 S.E. ana­
the Re-Os isotopic comIX'sition of sulfides
2(04). These xenoliths record different types
lytical uncertainties on 1870sJ1880s of <.0.2 Ga
in xenoliths from the Calatrava volcanic field
of metasomatisrn including carbonatitic, silica­
(fable DRI in the GSA Data Repository').
multicollector-inductively
coupled
in central Spain. The Calatrava volcanic field
undersaturated alkaline, and subduction-related
contains a suite of peridotite xenoliths from
styles (Villaseca et al., 2010; Bianchini et al.,
the lithospheric mantle underlying the crust of
2010; 0' Reilly and Griffin, 2012).
the Iberian microplate. Our results suggest that
The xenoliths studied here come from the El
the mantle and crust constituting the Iberian
Aprisco (38°S0'OS"N, 3°S0'OO''W) olivine meli­
microplate have coexisted since at least Paleo­
lite maar (Villaseca et al., 2010). They are nine
zoic-Proterozoic time. The comparison of our
coarse-grained lherzolites and two wehrlites that
data with Os-isotopic data from mantle-derived
equilibrated in the spinel facies (1.S-0.7 GPa)
materials from other localities in central and
at temperatures of 1120--940 °C and contain
high-precision
model-age constraints,
The 68 sulfides from El Aprisco that meet
these criteria have subchondritic 1870sJ1880s
(0.1147-0.1265) with 187Re/1880s varying from
subchondritic
«0.358)
to
suprachondritic
(0.432-0.572) (Fig. DR l in the Data Repository;
Table DRl). Only those sulfides with 187Rej1880s
< 0.07-0.08 may preserve undisturbed isotopic
signatures representative of mantle melting
andlor refertilization events (Griffin et al., 2004).
Only 12 of our sulfides display 187ReJ1880s <
0.08 (italic font in Table DRl). A screening of
the other 56 sulfides with 187Re/1880s > 0.08 in
Re-Os isotope plots reveals that many of the sul­
fide grains show the effects of recent Re addi­
tion, probably associated with the magmatic
activity that brought the xenoliths to the surface
at ca. 2 Ma. As little or no 1870S ingrowth has
occurred since this recent Re enrichment, the
TRD of these sulfides (calculated assuming Re
=
o ppm) still provides useful minimum estimates
of the timing of mantle events. For grains with
187ReJ1880s > 0.08 but uncorrelated Re-Os, we
have constructed two cumulative plots of Re­
depletion model ages: one uses
T RD ages of sul­
fides with "undisturbed" 1870sj1880s (grains with
187ReJ1880s < 0.08 as well as with 187ReJ1880s >
Figure 1. Cumulative­
probability plot of Re-de­
pletion model ages (T )
RD
for El Aprisco (Spain)
mantle sulfides of the
Calatrava volcanic field
(black solid line) com­
pared with age intervals
corresponding to events
recorded in crust of cen­
tral Iberia (see references
in the text) and major
events of supercontinent
growth (P-Pangea, G­
Gondwana, R-Rodinia,
C-Columbia; see refer­
ences in the Data Repos­
itory [see footnote 1D.
Events of amalgamation
or breakup of supercon­
tinents recorded in the
Iberian lithosphere are
�D Model age (Ga)
shown as gray or white
dotted columns, respectively. A cumulative-probability curve of T model ages for mantle­
RD
derived materials from both sides of the Mediterranean realm in central and western Europe
and North Africa (gray dashed line) has also been included for comparison (see details in
text and in the Data Repository for localities and references). Note that only positive T are
RD
plotted, and in the case of whole-rock (or mineral-concentrate) results, only data compared
against AI203 or other melt depletion indicators (e.g., Rudnick and Walker, 2009) were con­
sidered. To ensure comparison among all localities, T were calculated with reference to
RD
Enstatite Chondrite Reservoir (Walker et al., 2002) and an uncertainty of 0.1 Ga was assumed
for all single data points.
0.08 lying on horizontal trends in Re-Os plots);
the other uses only those grains with 187Rej1880s
> 0.08 and uncorrelated Re-Os (Table DR1).
Zone (Villaseca et al., 1998) and Hf model ages
1.0--1.2 Ga inherited zircon in Hercynian gran­
The two plots produce identical distributions of
(1.6--1.8 Ga) of inherited zircons from Hercyn­
ulites (Villaseca et al., 2011a), Hf model ages
age peaks. Therefore the
TRD
obtained from all
ian granulites (which have lower Paleozoic to
of 0.9-1.2 Ga in magmatic zircons, and the Nd
the 68 sulfide grains selected here can be used to
Neoproterozoic meta-igneous and metasedi­
whole-rock model ages of 1.0--1.3 Ga in the
unravel the evolution of the lithospheric mantle
mentary protoliths) sampled in rnigrnatite ter­
Hercynian gabbros (297-306 Ma) that intruded
beneath Iberia.
ranes and lower crustal xenoliths from the Cen­
the Central Iberian Zone (Fig. 1; Orejana et al.,
tral Iberian Zone (Villaseca et al., 2011a). The
2009; Villasecaet al., 2011b).
Origin and Evolution of the Iberian
corresJX)ndence of mantle and crustal ages sup­
The alkaline (silicate to caroonatite) meta­
Lithosphere: A 1.8 b.y. History of Mantle­
JXlfts the suggestion that primary mantle differ­
somatisrn observed in some xenoliths of the
Crust Interactions and Supercontinent
entiation and crustal growth in the Iberian litho­
Calatrava volcanic field in the Tertiary may be
Assemblies
sphere took place ca. 1.6-2.0 Ga. Reworking of
resJX)nsible for the negative model ages of sul­
Figure 1 shows a strong coincidence between
this ancient lithosphere in the Neoproterozoic
fides with highly radiogenic 1870s/1880S unsup­
the five peaks (at 1.8, 1.1, 0.9, 0.6, and 0.3 Ga)
and Paleozoic may explain the four younger
JXlfted by low Re/Os ratios; these were excluded
in the distribution of
TRn
model ages of the El
peaks in the sulfide
T RD
model ages. Thus, the
from this analysis.
Aprisco sulfides and the timing of well-con­
mantle event at ca. 0.6 Ga correlates with the
Figure 1 shows that the formation of the
strained magmatic events recorded in the over­
0.48-0.58 Ga mafic-to-silicic magmatism in the
Iberian lithosphere at ca. 1.6--2.0 Ga coincides
lying crust of Iberia. Most of the ages are older
Central Iberian Zone associated with the Cado­
with the first-order event of mantle-crust differ­
than the eXJX)sed crust in the irrnnediate area,
mian orogeny (Pereira et al., 2010; Bandres et
entiation that occurred during the assembly of
implying the JX)ssible existence of older crust
al., 2004). The involvement of the mantle is
the supercontinent Columbia at 1.8-1.5 Ga. The
at depth. Interestingly, the three main peaks in
evidenced by juvenile Hf isotopic signatures
1.3-0.9 Ga timing of magmatic events recorded
the El Aprisco sulfides at 1.8, 0.6 and 0.3 are
(EBft up
for ooth crustal and mantle materials in Iberia
consistent with
TRn
ages obtained for mantle­
derived materials of comparable mantle suites
to +9.7) of inherited zircons (U-Pb age
0.5-0.7 Ga) in the Hercynian granulites. Exten­
coincide with the amalgamation of Roclinia at
sional decompression associated with delamina­
ca. 1.25 Ga and its breakup at ca. 0.75 Ga. The
on both sides of the Mediterranean reahn (cen­
tion of lower-crustal rocks may have promoted
peak in T
tral and western Europe and North Africa). The
upwelling and melting of the mantle following
ning of continental collisions to form Gond­
RD at 0.6 Ga correlates with the begin­
TRD
smoother curve for the synthesized European­
the Hercynian collision (Orejana et al., 2009).
wana (ca. 0.65 Ga), whereas the
Mrican mantle data largely reflects the num­
This would explain the correlation between the
at 0.3 Ga may be correlated with JX)st-tectonic
ber of intermediate model ages produced by
magmatic event at 0.3 Ga recorded in mantle
stages and the initiation of the breakup of Pan­
the mixing of sulfide JX)pulations in individual
sulfides and the silicic and mafic magrnatism of
gea recorded in the Central Iberian Zone at
whole-rock samples (Fig. 1).
ooth crustal and mantle origin recognized in the
ca. 0.26 Ga (Orejana et al., 2008).
The oldest Paleoproterowic event (1.8 Ga)
seen in the
TRn
age peak
Central Iberian Zone at 0.28-0.32 Ga (Feman­
model ages of the El Aprisco
dez-Suarez et al., 2(00). Melt production in the
Implications for the Architecture of the
sulfides (Fig. 1) correlates with whole-rock Nd
mantle beneath Iberia at 0.9-1.3 Ga is reflected
European-Mediterranean Lithosphere
model ages (1.7-2.0 Ga) of Neoproterozoic
in
sediments (ca. 560 Ma) of the Central Iberian
fides, positive
TRD
model ages of 0.9-1.1 Ga in mantle sul­
tHft
signatures (up to +12.8) of
Figure 2 shows that mantle-derived rocks on
ooth sides of the Mediterranean realm (central
n::11
... Cenozoic volcanic field
, Peridotite massif
.., East-dipping Subduction
_A... West-dipping Subducton
� Original Archean SCLM ?
_
these continental riboons and the subcontinental
Archean-Paleoproterozoic mantle widespread
through
the
Betics-Magbrebides-Appenines
front may be the fragmented reIIlllants of an
Archean microcontinent within the inner Medi­
terranean area. The repetition of model age
peaks at
ca.
0.9-1.2, ca. 0.4-0.7, and
ca.
0.3 Ga
in the mantle both within and outside the cen­
tral-western Mediterranean reahn (Fig. 2) sug­
gests that this microplate was strongly modified
and fragmented (but survived) during supercon­
tinent assembly-disruption cycles since Paleo­
proterozoic times.
In the context of convergence of Africa
and Europe during the Tertiary, dismembered
blocks of this ancient microplate could have
spread, colliding with passive margins (Iberia,
Magrhebide, Adria), thus contributing to the
development of subduction-related volcanic
arcs within the inner Mediterranean (Faccenna
et al., 2004; Booth-Rea et al., 2007; Garrido et
al., 2011; Canninati et al., 2012). We suggest
that these major tectonic events have stripped
Figure 2. Cumulative-probability plots for Re-Os model ages of sulfides, platinum-group
minerals, mineral concentrates, and whole-rock samples of xenoliths from Cenozoic vol­
canic fields and massifs in the central-western Mediterranean region (age peaks are in Ga;
whole-rock ages are minimum ages). Gray fields refer to inferred original Archean subconti­
nental lithospheric mantle (details in text). SCLM-subcontinental lithospheric mantle. Note
that in all cases, only positive Re-depletion model ages (TRO) are shown, except for Beni
Boussera (Morocco), for which the Re-Os model age presented is TMA• Whole-rock and min­
eral-separate Os data were screened following the same criteria as in Figure 1. References
for each locality are given in the Data Repository (see footnote 1).
off most of the old continental crust, leav­
ing behind residues of ancient subcontinental
mantle. This mantle, buoyant relative to the
asthenosphere, would have continued to ride
over the small-scale convective cells detected
by seismic tomography at depths >200 km
(O'Reilly et al., 2009; Faccenna and Becker,
2010), then become part of the oceanic basin
and serve as the basement for the accumulation
of oceanic basalts and sediments. An analo­
gous process has been described in detail from
and western Europe and North Mrica) yield
oldest whole-rock model age
(TMA)
of 2.3 Ga
the Internal Ugurides, where a typical Meso­
TRn � 1.8 Ga, whereas those from the
obtained by Pearson and Nowell (2004) for
zoic
inner Mediterranean region show ooth younger
pyroxenites of the Beni Boussera Massif in
overlies the Archean mantle peridotites (Ram­
JXlne et al., 2(05). It is important to note that
maximum
oceanic
volcanic-sedimentary
section
and older (up to 2.6 Ga) ages. Many sulfides
northern Morocco and the 2.4 Ga peak in pri­
in xenoliths from the mantle beneath western
mary magmatic sulfides from peridotites of the
some JXlrtions of the Archean subcontinental
Europe (Calatrava, Languedoc, and Massif Cen­
internal Ligurides (Italy) (Alard et al., 2005).
lithospheric mantle within the inner Mediterra­
tral) show a common oldest peak at 1.8 Ga. This
A slightly older peak at 2.6 Ga has recently
nean were refertilized (Mg# = 89-90 of olivine
peak is also recognized in whole-rock samples
been relhlfted by Konc et al. (2012) in sulfides
in peridotite) by the passage of subduction­
from the Pyrenees (France) and Azrou (North
from mantle xenoliths from the Tallante volca­
related fluids in the Cenozoic. However, these
Mrica) but is slightly older than the oldest peaks
nic field in southern Spain. These ages clearly
fluids were not able to erase the old Archean
at <1.4-1.3 Ga found in whole-rock samples
identify an older lithospheric mantle fonned
Re-Os signatures preserved in some sulfides
from central Europe (Bohemian and Rhenish
near the Archean-Paleoproterozoic ooundary at
(Marchesi et al., 2010).
Massifs). Nevertheless, although these whole­
ca. 2.2-2.6 Ga, sitting within the more recent
rock ages were screened against indices of melt
Betics-Magbrebides-Appenines front (Fig. 2)
depletion in the rock (e.g., Al103; Rudnick and
generated during the Alpine-Betic orogeny.
ACKNOWLEDGMENTS
We acknowledge William Collins, two anonymous
reviewers, and Lukas: Ackennan for comments that
Walker, 2009), they must been seen as a guide
Seismic, gravity, and heat-flow data suggest
and can only be regarded as minimum values
that the structure to 70 km beneath the Medi­
as they may integrate multiple generations of
terranean Sea consists of ribbons of continen­
Centre of Excellence for Core to Crust Fluid Systems,
sulfides (e.g., Alard et al., 2002; Griffin et al.,
tal lithosphere (Valencia throu gh the Balearic
Villaseca Gonzalez' grant from Fundaci6n Caja Ma­
2004). All these data are consistent with the
promontory, the Sardinia-Corsica block, and
existence of a common Paleoproterozoic man­
the Hyblean Plateau beneath Sicily) separated
tle on ooth sides of the Mediterranean realm,
by areas of thinned subcontinental lithosphere
formed ca. 1.8 Ga as recorded in the other parts
or new oceanic crust (the Alboran, Uguro­
significantly improved the first version of this manu­
script. Financial support was provided by tre ARC
drid convocatoria 2010, the Spanish "Ministerio de
Ciencia e Innovaci6n" grant CGL201O-14848, tre
Junta de Andalucia research grants RNM-131 and
2009RNM4495, and the International Lithosphere
Program (CC4-:MEDYNA). The analytical data were
Provenr;al, Vavilov, and Marsili Tyrrenian sea
obtained
In contrast, Os-bearing minerals from xeno­
basins) (e.g., Gueguen et al., 1997; Booth-Rea
Systemic Infrastructure Grants, ARC LIEF, NCRIS,
liths and peridotite massifs from the inner Med­
et al., 2007). In the riboon beneath Sicily, xeno­
iterranean region (Sicilian Hyblean Plateau,
lith data suggest that thinned Archean continen­
Kraubath ultramafic massif) show a common
tal crust overlies subcontinental mantle of the
.au) and contribution 860 from the GEMOC National
same age (Sapienza et al., 2007). Thus all of
Key Centre (www.gemoc.mq.edu.au).
of the European basement.
oldest
T RD
peak at ca. 2.3 Ga, identical to the
using instrumentation
funded by DEST
industry partners, and Macquarie University. Tbis is
contribution 234 from the ARC Centre of Excellence
for Core to Crust Fluid Systems (www.ccfs.mq.edu
REFERENCES CITED
the Kaapvaal Craton: Re-Os systematics of
shear zone, SW Iberian Massif): Tectonothennal
Alard, 0., Griffin, W.L., Pearson, N.l., Lorand, l.­
sulfides in mantle-derived peridotites: Chemi­
analysis and U-Th-Pb SHRIMP in situ zircon
P, and O'Reilly, S.Y., 2002, New insights
cal Geology, v. 208, p. 89-118, doi:1O.1016/j
geochronology: Gondwana Research,
into the Re-Os systematics of sub-continental
.chemgeo.2004.04.007.
p. 440-460, doi:1O.1016/j.gr.2009.1O.001.
v. 17,
lithospheric mantle from in situ analysis of
Gueguen, E., Doglioni, c., and Fernandez, M., 1997,
sulphides: Earth and Planetary Science Letters,
Lithosphere boudinage in the Western Mediter­
ardo, G.B., and Hofmann, AW., 2005, Chro­
v. 203, p. 651-663, doi:1O.1016/S0012-821X
ranean back-arc basin: Terra Nova, v. 9, p. 184-
nology, petrology and isotope geochemistry
187, doi:10.1046/j.1365-3121.1997.dOl-28.x.
of the Erro-Tobbio peridotites (Ligurian Alps,
(02)00799-9.
Rampone, E., Romairone, A, Abouchami, W., Picc­
Alard, 0., Luguet, A., Pearson, NJ., Griffin, W.L.,
Konc, Z., Marcresi, c., Garrido, c.J., Gonzilez-Ji­
Italy): Record of late Palaeozoic lithospheric
Lorand, J.-P., Gannoun, A, Burton, K.W., and
menez, JM., Griffin, w.L., Alard, 0., Hidas, K,
extension: Journal of Petrology, v. 46, p. 799-
O'Reilly, S.Y., 2005, In situ Os isotopes in abys­
O'Reilly, S.Y., and Pearson, N.J., 2012, Prov­
sal peridotites bridge the isotopic gap between
enance and evolution of the western Mediterra­
Rudnick, L.R, and Walker, RJ., 2009, Interpreting
827, doi:1O.1093/petrology/egiOOl.
MORBs and Heir source mantle: Nature, v. 436,
uean lithospheric mantle beneath tre eastern Bet­
ages from Re-Os isotopes in peridotites: Lithos,
p. 1005-1008, doi:10.1038/nature03902.
ics (S. Spain): InsiglIs from in-situ analyses of
v. 112, p. 1083-1095, doi:1O.1016/j.lithos.2009
Ancochea, E., 2004, La regi6n volcan:ica del Campo de
Os isotopes and platinum-group elements in sul­
.04.042.
Calatrava, in Vera, l.A., ed., Geologia de Espaiia:
phides from the Tallante mantle xenoliths: Geo­
Madrid, Geological Survey of Spain (IGME)­
physical Research Abstracts, v. 15, EGU12929.
Sapienza, G.T., Griffin, WL, O'Reilly, S.Y., and
Morten, L., 20CJ7, Crnstalzircons and mantle sul­
Geological Society of Spain (SGE), p. 676--677.
Marchesi, c., Griffin, WL, Garrido, c.J., Bodinier,
Bandres, A., Eguiluz, L., Pin, c., Paquette, J.L.,
J-L., O'Reilly, S.Y., and Pearson, N.J., 2010,
beneath
fies: Archean to Triass:ic events in the lithosphere
Ord6iiez, B., Le Fevre, B., Ortega, L.A, and
Persistence of mantle lithospheric Re-Os sig­
p. 503-523, doi:1O.1016/j.lithos.2006.11.007.
south-eastern Sicily: Lithos,
v.
96,
Gil Ibarguchi, J.I., 2004, The northern Ossa­
nature during asthenospherization of the sub­
Morena
Mas­
continental lithospheric mantle: Insights from in
Crustal origin of Hercynian peraluminous gra­
sif): Magmatic arc origin and early evolution:
situ isotopic analysis of sulfides from the Ronda
nitic batholiths of central Spain: Petrological,
Cadomian
batholith (Iberian
Villaseca, c., Barbero, L., and Rogers, G., 1998,
International Journal of Earth Sciences, v. 93,
peridotite (Southern Spain): Contributions to
geochemical and isotopic (Sr,Nd) arguments:
p. 860-885, doi:1O.1007/s00531-004-0423-6.
Mineralogy and Petrology, v. 159, p. 315-330.
Lithos,
Bianchini, G., Beccaluva, L., Bonadiman, c., Nowell,
O'Reilly, S.Y., and Griffin, WL, 2012, Mantle meta­
v. 43, p. 55-79, doi:1O.1016/S0024
-4937(98)00002-4.
G.M., Pearson, D.G., Siena, F., and Wilson, M.,
somatism, in Harlov, D.E., and Austrheim, H.,
Villaseca, c., Ancochea, E., Orejana, D., and Jeffries,
2010, Mantle metasomatism by melts of HIMU
eds., Metasomatism and the Chemical Trans­
T.E., 2010, Composition and evolution of tre
piclogite components: New insiglIs from Fe­
formation of Rock: Lecture Notes in Earth Sys­
lithospheric mantle in central Spain: Inferences
lherzolite xenoliths (Calatrava Volcanic District,
tem Sciences: Berlin, Springer-Verlag, p. 467-
from peridotite xenoliths from the Cenozoic Ca­
central Spain), in Coltorti, M., et al., eds., Petro­
528, doi:10.1007/978-3-642-28394-9_12.
latrava volcanic field, in Coltorti, M., et al., eds.,
Petrological Evolution of the European Litho­
logical Evolution of the European Lithospheric
O'Reilly, S.Y., Zhang, M., Griffin, WL, Begg, G.,
Mantle: Geological Society of London Special
and Hronsky, J., 2009, Ultradeep continental
spheric Mantle: Geological Society of London
Publication 337, p. 107-124.
roots and their oceanic remnants: A solution to
Special Publication 337, p. 125-151.
Booth-Rea, G., Ranero, C.R, Martinez-Martinez,
the geochemical "mantle reservoir" problem?:
J.M., and Grevemeyer, I., 20CJ7, Crustal types
Lithos, v. 112, p. 1043-1054, doi:1O.1016/j
Villaseca, c., Belousova, E., Orejana, D., Castiiiei­
ras,
and Tertiary tectonic evolution of the Albocin
.lithos.2009.04.028.
Palaeoproterozoic and Archean components in
P, and Perez-Soba, c., 2011a, Presence of
sea, western Mediterranean: Geochemistry Geo­
Orejana, D., Villaseca, c., Billstrom, K, and Pat­
the granulite-fac:ies rocks of central Iberia: T re
physics Geosystems, v. 8, Ql0005, doi: 10.1029
erson, B.A, 2008, Petrogenesis of Permian
Hf isotopic evidence: Precambrian Research,
12007GCOO1639.
Carminati, E., Lustrino, M., and Dogiloni, c., 2012,
alkaline lamprophyres and diabases from the
v. 187, p. 143-154, doi:1O.1016/j.precamres
Spanish Central System and their geodynamic
.2011.03.001.
Geodynamic evolution of the central and west­
context within western Europe: Contributions
ern Mediterranean: Tectonics vs. igneous petrol­
to Mineralogy and Petrology, v. 156, p. 477-
RA, Perez-Soba, c., and Jeffries, T.E., 2011b,
ogy constraints: Tectonophysics, doi:1O.1016/j
500, doi:10.1007/s00410-008-0297-x.
U-Pb isotopic ages and Hf isotope composition
.tecto.2012.0l.026 (in press).
Villaseca, c., Orejana, D., Belousova, E., Annstrong,
Orejana, D., Villaseca, c., Perez-Soba, c., L6pez­
of zircons in Variscan gabbros from central
Faccenna, c., and Becker, T.W., 2010, Shaping mo­
Garcia, J.A, and Billstrom, K, 2009, The
Spain: Evidence of variable crustal contamina­
bile belts by small-scale convection: Nature,
Variscan gabbros from the Spanish Central
tion: Mineralogy and Petrology, v. 101, p. 151-
v. 465, p. 602-605, doi: 1O.1038/nature09064.
System: A case for crnstal recycling in the sub­
167, doi:1O.1007/s0071O-01O-0142-6.
Faccenna, c., Piromallo, c., Crespo-Blanc, A, Jolivet,
L., and Rossetti, F., 2004, Lateral slab defonna­
continental lithospheric mantle?: Lithos, v. 110,
p. 262-276, doi:1O.1016/j.lithos.2009.01.003.
Walker, RJ., Horan, M.F, MOl-gan, J.W., Becker,
H., Grossman, J.N., and Rubin, AE., 2002,
tion and ne origin of ne western Mediterranean
Pearson, D.G., and Nowell, GM., 2004, Re-Os and
Comparative lSlRe_1870s systematics of chon­
arcs: Tectonics, v. 23, TC1012, doi:1O.1029
Lu-Hf isotope constraints on the origin and age
drites: Implications regarding early solar sys­
I2002TCOO1488.
of pyroxenites from the Beni Bousera peridotite
tem processes: Geochimica et Cosmochimica
Fernandez-Su;lrez, J., Dunning, G.R, Jenner, G.A,
massif: Implications for mixed peridotite-pyrox­
Acta, v. 66, p. 4187-4201, doi:1O.1016/S0016
and Gutierrez-Alonso, G., 2000, Variscan colli­
enite mantle sources: Journal of Petrology, v. 45,
sional magmatism and defonnation in N\V Ibe­
p. 439-455, doi:1O.1093/petrology/eggl02.
-7037(02)01003-7.
Wilshire, H.G., and Shervais, J.W., 1975, Al-augite
ria: Constraints from U-Pb geochronology of
Pearson, N.J., Alard, 0., Griffin, w.L., Jackson, S.E.,
granitoids: Journal of the Geological Society,
and O'Reilly, S.Y., 2002, In situ measurement of
rocks from western United States: Physics and
v. 157, p. 565-576, doi: 1O.1144/jgs.157.3.565.
Re-Os isotopes in mantle sulfides by laser abla­
Chemistry of the Earth, v. 9, p. 257-272.
Garrido, c.J., Gueydan, F, Booth-Rea, G., Precigout,
tion multicollector-indnctively coupled plasma
J., Hydas, K, Padr6n-Navarta, J.A, and Mar­
mass spectrometry: Analytical methods and pre­
chesi, c., 2011, Garnet lherzolite and garnet­
liminary results: Geochimica et Cosmochimica
spinel mylonite in the Ronda peridotite: Vestiges
Acta, v. 66, p. 1037-1050, doi:1O.1016/S0016
of Oligocene backarc mantle lithospheric exten­
-7037(01)00823-7.
sion in the western Mediterranean: Geology,
Pereira, M.F, Apraiz, A, Chichorro, M., Silva, J.B.,
v. 39, p. 927-930, doi:10.1130IG31760. 1.
and Annstrong, RA, 2010, Exhumation of
Griffin, W.L., Graham, S., O'Reilly, S.Y., and Pear­
high-pressure rocks in northern Gondwana dur­
son, N.J., 2004, Lithosphere evolution beneath
ing the Early Catboniferous (Coimbra-Cordoba
and Cr-diopside ultramafic xenoliths in basaltic