Deep in the Heart of Dixie: Pre-Alleghanian Eclogiteand HP Granulite Metamorphism in the Carolina Terrane,South Carolina, USA

J . W. SHERVAIS,1 A. J . DENNIS,2 J . J . MCGEE3 AND D. SECOR3

1Department of Geology, Utah State University, Logan UT, 84322, USA (shervais@cc.usu.edu)2Department of Geology and Biology, University of South Carolina, Aiken SC 29801, USA3Department of Geological Sciences, University of South Carolina, Columbia SC, 29208, USA

ABSTRACT The central part of the Carolina terrane in western South Carolina comprises a 30 to 40 km wide zone ofhigh grade gneisses that are distinct from greenschist facies metavolcanic rocks of the Carolina slate belt(to the SE) and amphibolite facies metavolcanic and metaplutonic rocks of the Charlotte belt (to theNW). This region, termed the Silverstreet domain, is characterized by penetratively deformed felsicgneisses, granitic gneisses, and amphibolites. Mineral assemblages and textures suggest that these rocksformed under high-pressure metamorphic conditions, ranging from eclogite facies through high-Pgranulite to upper amphibolite facies.Mafic rocks occur as amphibolite dykes, as metre-scale blocks of coarse-grained garnet-clinopyroxene

amphibolite in felsic gneiss, and as residual boulders in deeply weathered felsic gneiss. Inferredomphacite has been replaced by a vermicular symplectite of sodic plagioclase in diopside, consistent withdecompression at moderate to high temperatures and a change from eclogite to granulite facies con-ditions. All samples have been partially or wholly retrograded to amphibolite assemblages. We infer thefollowing P-T-t history: (1) eclogite facies P-T conditions at ‡ 1.4 GPa, 650–730 �C (2) high-P granulitefacies P-T conditions at 1.2–1.5 GPa, 700–800 �C (3) retrograde amphibolite facies P-T conditions at0.9–1.2 GPa and 720–660 �C. This metamorphic evolution must predate intrusion of the 415 MaNewberry granite and must postdate formation of the Charlotte belt and Slate belt arcs (620 to 550 Ma).Comparison with other medium temperature eclogites and high pressure granulites suggests that these

assemblages are most likely to form during collisional orogenesis. Eclogite and high-P granulite faciesmetamorphism in the Silverstreet domain may coincide with a �570–535 Ma event documented in thewestern Charlotte belt or to a late Ordovician-early Silurian event. The occurrence of these high-Passemblages within the Carolina terrane implies that, prior to this event, the western Carolina terrane(Charlotte belt) and the eastern Carolina terrane (Carolina Slate belt) formed separate terranes. Thecollisional event represented by these high-pressure assemblages implies amalgamation of these formerlyseparate terranes into a single composite terrane prior to its accretion to Laurentia.

Key words: amphibolite; Carolina terrane; southern Appalachians; eclogite; HP granulite.

INTRODUCTION

High-pressure granulites, characterized by the ortho-pyroxene-free assemblage Grt + Cpx + Pl ± Qtz,comprise a newly recognized subfacies transitionalbetween plagioclase-free eclogites and orthopyroxene-bearing granulites (Pattison, 2003). O’Brien & Rotzler,2003) distinguished two varieties of high-P granulite:ultra-high temperature assemblages with melt reactiontextures, and medium-T, high-P assemblages (700–850 �C, 1.0–1.4 GPa) that overprint former eclogitefacies assemblages. Like medium temperature (MT)eclogites (Carswell, 1990), the medium-T, high-Pgranulite subfacies is typically associated with colli-sional orogens, which form in tectonically thickenedarc or continental crust, typically in response to theattempted subduction of an arc or continental margin

during collision (e.g. Carswell, 1990; O’Brien & Rot-zler, 2003). In many areas, these rocks are commonlyassociated with retrogressed felsic gneisses that wereoriginally cofacial with the enclosed eclogites (e.g.Cuthbert & Carswell, 1990; Cuthbert et al., 2000;O’Brien et al., 1990).The eastern margin of North America in the

southern and central Appalachians comprises a tec-tonic collage of terranes that formed in exotic locationsduring the late Neoproterozoic through early Palaeo-zoic, and were subsequently accreted to Laurentiaduring the mid- to late Palaeozoic (Williams &Hatcher, 1983; Secor et al., 1983; Horton et al., 1989,1991; van Staal et al., 1998). These exotic terranesevolved independently of Laurentia for much of theirexistence, and preserve evidence of orogenic andmagmatic events that are not observed in Laurentia.

J. metamorphic Geol., 2003, 21, 65–80

� Blackwell Science Inc., 0263-4929/03/$15.00 65Journal of Metamorphic Geology, Volume 21, Number 1, 2003

One of the most extensive of these exotic peri-Gondwana terranes is the Carolina terrane, whichcomprises a large portion of the southern Appalachianorogen east of the Blue Ridge province (Secor et al.,1983; Fig. 1). The Carolina terrane is an exoticAvalonian terrane that originally formed adjacent toGondwana in the late Neoproterozoic, and was notaccreted to Laurentia until the mid- to late Palaeozoic(Secor et al., 1983; Williams & Hatcher, 1983).We have recently re-examined a little known

occurrence of high-P granulite and amphibolite, withan inferred MT eclogite precursor, within the centralpart of the Carolina terrane (Dennis et al., 2000).These rocks, which were originally interpreted aspyroxene-bearing garnet amphibolites, contain relictgarnet-pyroxene-plagioclase assemblages that record apreviously unrecognized episode of eclogite trans-itional to medium temperature HP granulite faciesmetamorphism within the Carolina arc terrane. Thisevent has broad implications for the evolution of thesouthern Appalachians, and for models of metamor-phism and exhumation in accreted arc terranesin general. We present here a first look at thesenewly discovered high pressure rocks, their inferredP–T–t history and some tectonic implications of theiroccurrence.

ECLOGITES AND GRANULITES OF THECAROLINA TERRANE

Regional Setting

The Carolina terrane in the southern Appalachians is a calc-alkalineisland arc that is exotic to Laurentia and does not share a commonhistory with North America until the late Palaeozoic Alleghanianorogeny (Fig. 1). It is largely Neoproterozoic in age but includessections of early to middle Cambrian age (Secor et al., 1983; Samsonet al., 1990; Shervais et al., 1996; Dennis & Shervais, 1996; Wortmanet al., 2000). Recent field and geochronological studies showthat the Carolina terrane formed during two major episodes of arcmagmatism at �620 Ma and �550 Ma (Dennis & Wright, 1997;Heatherington et al., 1996).

The Carolina terrane has been divided into three belts with dif-ferent metamorphic and petrological characteristics: (1) the KingsMountain belt, which consists of greenschist facies mafic metavol-canic rocks and forms the north-western margin of the Carolinaterrane; (2) the Charlotte belt, which consists largely of lower tomiddle amphibolite facies, dominantly mafic metavolcanic and meta-plutonic rocks; and (3) the Carolina Slate belt, which is dominated bylow-grade (greenschist to subgreenschist) felsic metavolcanic rockswith subordinate mafic lavas and mudstones (Fig. 1).The Carolina terrane was metamorphosed and ductilely deformed

during the latest Neoproterozoic to early Cambrian (Dennis &Wright, 1995, 1997; Hibbard & Samson, 1995; Barker et al., 1998).Metamorphism and ductile deformation resulting from the Alle-ghanian (�320 Ma) collision of Laurentia and Gondwana isrestricted to narrow shear zones which separate broad zones con-taining older fabric and mineral assemblages (e.g. Secor et al., 1986;Dallmeyer et al., 1986; Horton et al., 1989; Horton & Dicken, 2001).The Charlotte belt was intruded by a suite of undeformed Devoniangabbros and granitoids (�400 Ma; McSween et al., 1991) that cross-cut regional foliation and mark the upper age limit of penetrativedeformation within most of the terrane.The exotic nature of the Carolina terrane is shown clearly by the

occurrence of a diverse Middle Cambrian peri-Gondwanan trilobitefauna in the Carolina Slate belt (Samson et al., 1990). In addition,combined field-geochronological studies have shown that metamor-phic fabric in most of the Carolina terrane formed prior to 535 Ma,approximately coeval with the rift-drift transition on the Laurentianmargin (Dennis & Wright, 1995, 1997; Hibbard & Samson, 1995;Barker et al., 1998).

Field Occurrence of High-Pressure Rocks

The boundary between the Charlotte belt and the Slate belt in centralSouth Carolina comprises a 30-km wide zone of high grade gneissesthat are distinct from less highly deformed amphibolite facies(dominantly) mafic rocks of the Charlotte belt (to the northwest) andlow-grade felsic metavolcanic rocks of the slate belt (to the south-east; Fig. 2). This region, termed the Silverstreet domain, consists ofhigh-grade felsic biotite gneisses, granitic gneisses, and amphibolitesthat form the SE margin of the Charlotte belt (Secor et al., 1982,1988; Halik, 1983; Hauck, 1984). The Silverstreet domain is intrudedby the undeformed early Devonian Newberry granite (415 ± 9 Ma;Fullagar, 1981; Samson & Secor, 2000), which cross-cuts regionalfoliation and includes xenoliths of sheared and foliated country rock.The age of this pluton represents an uppermost age limit forformation and deformation of rocks in the Silverstreet domain.The Silverstreet domain is bounded to the north and south by

shear zones. A variety of field studies have demonstrated that the

Fig. 1. Regional geology of the southernAppalachians, showing principal sub-divi-sions, including the Carolina terrane (palegrey), the Blue Ridge terrane (dark grey), theInner Piedmont terrane, and the AtlanticCoastal Plain. Rocks of the Inner Piedmontterrane (including the Chauga belt) and theCarolina terrane (including the Charlottebelt, the Carolina Slate belt, and the KingsMountain belt [KMB]) are all exotic toNorth America.

6 6 J . W . S H E R V A I S E T A L .

boundary between the high-grade gneisses of the Silverstreet domainand the Carolina Slate belt is a fault over much of its length, but itsgeometry and kinematics are not known (e.g. Dennis et al., 2000;Offield, 1995; Offield & Sutphin, 2000; Secor et al., 1988, 1989). It isinferred to be a normal fault in part because it juxtaposes high-gradeCharlotte belt rocks against low-grade Slate belt rocks. Locally,however, it can be demonstrated that most recent ductile motionalong the Stony Hill orthogneiss was right lateral, based on com-posite planar fabric and asymmetric porphyroclasts (Dennis et al.,2000). The northern margin of the Silverstreet domain is a 10-kmwide, E-W trending ductile shear zone (Beaver Creek shear zone)with dextral shear sense indicators that separates it from lessdeformed rocks of the Charlotte belt (West, 1998).Mafic rocks in less deformed parts of the Silverstreet domain form

amphibolite dykes up to �20 cm thick that are oriented parallel toregional foliaton. In more deformed areas, isolated metre-scaleblocks within felsic gneiss are interpreted to represent boudinagedmafic dykes (Fig. 3). In many areas, these blocks form residualboulders that have weathered out of the felsic gneisses; where theseoccur in flat upland terrain they are interpreted to be approximatelyin place.Retrogressed eclogite and high-P granulite assemblages commonly

are preserved in the cores of these isolated blocks. Blocks with relicthigh-pressure assemblages are found within the Beaver Creek shearzone along the north side of the Silverstreet domain and as residualboulders near the centre of the terrane, south of the Newberrygranite, and clearly outside of the Beaver Creek shear zone (Fig. 2).Foliation in the shear zone wraps around the eclogite blocks andclearly postdates eclogite formation.

Mineralogy and Mineral Chemistry

Mafic rocks that preserve high-pressure assemblages are modallydiverse with �20–40% pink garnet, 20–60% green, diopsidic clino-pyroxene, 15–45% hornblende, up to 10% plagioclase, and 3–5%ilmenite, with accessory rutile, epidote, apatite, zircon, titanite andcalcite (e.g. Libby & Carpenter, 1969). Relict garnet and pyroxenegrains are up to 1 cm diameter, but typical grain size for relict phasesis �1–3 mm (Fig. 4). In thin section, hornblende, plagioclase andilmenite replace clinopyroxene, while garnet is replaced along itsmargins by kelyphitic intergrowths of plagioclase with hornblende

and minor epidote. Calcite forms irregular veins and patches. Epi-dote, quartz, plagioclase, hornblende and oxides are also found asinclusions in garnet, with epidote being the dominant inclusionphase. Representative electron microprobe analyses from one sampleare presented in Table 1; these data are presented graphically inFig. 5. Analytical methods are presented in Appendix A: Methods.Where it has been well preserved, diopside is characterized by a

vermicular symplectite of sodic plagioclase (An15)22) that we inferrepresents the breakdown of omphacite; this is clearly shown by bothBSE images and high-resolution X-ray composition maps of thesymplectites (Fig. 6). The diopside contains about 15% jadeitecomponent, but modal reconstruction (see Appendix A: Methods)suggests that primary omphacite contained �30% jadeite. Thereconstructed omphacite is presented in Table 1.The breakdown of omphacite to diopside + plagioclase sym-

plectite is commonly observed in high-P granulites after a medium

Fig. 3. Field photo of eclogite block in felsic gneiss of BeaverCreek shear zone. Block is about 1.5 m across, with a trapezoidalshape; foliation in the shear zone wraps around the block. Thisand other blocks were sampled using portable core drill.

Columbia

Lake Murray

L. Greenwood

Clinton Joanna Newberry NW BlairWhitmire S

Cross Hill Bush River

Good Hope

Newberry W

Saluda N

Pomaria

Chappells

Jenkinsville

DysonLittle Mtn ChapinSilverstreet Prosperity

DelmarDenny

Newberry E

Whitmire Reentrant: Inner Piedmont

Wateree L.

Carolina slate belt and Kiokee belt

82¡W

34¡N

34¡30'N

81¡W

Salem X-roads

Beaver Creek shear zone

E

?

Stoney Hill orthogneiss

Clinton

Winnsboro granite295 ± 2 Rb-Sr w.r.

Newberry granite414 ± 8 Ma U-Pb z.

Little Mtn metatonalite 550 ± 4 Ma U-Pb z.

E

E

E

E

E

E

High grade Silverstreet domain: eclogite, high-P granulite and enclosing felsic gneisses

c. 414 ± 8 Ma (U-Pb z) Newberry granite

c. 295 ± 4 Ma (Rb-Sr w.r.) Winnsboro granite

Little Mountain metatonalite orthogneiss

E known eclogite - high P granulite localities

area of Secor and others (1982) investigation outlined in dash

Mesozoic brittle faults

Orientation of some major structuresin Carolina slate belt and Kiokee belt

7.5' quadrangles indicated and named in SE corner. This report focussed on quadrangles shown in bold.

++

+++

Fig. 2. Geological map showing location of eclogite ⁄high pressure granulite-bearing Silverstreet domain of the Charlotte belt relativeto the Carolina Slate belt and the Whitmire reentrant of the Inner Piedmont. Capital �E� shows location of known eclogite ⁄ granuliteblocks.

D E E P I N T H E H E A R T O F D I X I E 6 7

temperature eclogite assemblage, and is consistent with decompres-sion at moderate to high temperatures (e.g. Elvevold & Gilotti, 2000;O’Brien & Rotzler, 2003). The inferred primary assemblageomphacite + garnet ± rutile is consistent with formation undereclogite facies conditions, whereas the observed assemblage diopside+ plagioclase + garnet represents high pressure granulite faciesconditions (Galan & Marcos, 2000; Cooke et al., 2000; Pattison,2003; O’Brien & Rotzler, 2003). The breakdown of diopside andgarnet to form amphibole + plagioclase + epidote + ilmeniterepresents final equilibration under amphibolite facies conditions.Formation of amphibolite occurred in two stages. The first is rep-resented by aluminous pargasite and relatively calcic plagioclase(An26)53), which replace diopside + sodic plagioclase symplectites;the second is represented by magnesian pargasite and more sodicplagioclase (An17)22) which replace both diopside and garnet. Cal-culated hornblende-plagioclase temperatures (next section) suggestthat the aluminous pargasite-calcic plagioclase pairs formed at highertemperatures than the magnesian pargasite-sodic plagioclase pairs,and that they are closely associated with the high-P granuliteassemblages.High resolution X-ray composition maps of garnet show two

distinct growth zones (Fig. 7). The inner zone is enriched in Mn andFe, the outer zone is enriched in Ca and Mg. The Ca and Fe X-raymaps show a sharp interface between the inner core and the outermantle, while Mg and Mn show smooth, continuous zoning profiles(Fig. 7). Note that these garnet are generally not symmetricallyzoned: the centre of growth typically lies close to one edge of thegrain. In the example shown here, several small spessartine-richgarnet cores (seen as high Mn spots in the X-ray maps) have beensubsumed by the garnet mantle as it grew.Compositional profiles selected to traverse from the true core to

rim confirm these trends. A 1500-lm traverse of the grain mapped inFig. 7 shows smooth profiles for pyrope (Prp) and spessartine (Sps),and sharp steps in profiles for grossular (Grs) and almandine (Alm;Fig. 8). Profiles for three additional garnet are shown in Fig. 9,scaled to percentage of total grain radius. Although these threegrains vary somewhat in their innermost core compositions (Grs,Sps), they display consistent profiles for all elements, with (a) an

inner zone (0 to 55% of radius) that is low in Grs and Prp, and highin Alm and Sps, and (b) an outer zone (60 to 100%) that is higher inGrs and Prp, and lower in Alm and Sps (Fig. 9). All grains exhibit asharp increase in Grs and decrease in Alm at the transition (c. 60% ofgrain radius) that implies an abrupt change in growth history.

RESULTS

Geothermobarometry

We infer from the data presented above that the garnetcores formed during prograde metamorphism atgreenschist or amphibolite facies conditions, followedby growth of the garnet mantles at eclogite (Grt-Omp-Rt) and then high-P granulite facies conditions(Grt-Di-Hbl-Pl-Ilm); retrograde metamorphism in theamphibolite facies resulted in the breakdown of garnetand formation of the late Hbl-Pl-Ilm assemblage.Because these rocks experienced a range of metamor-phic conditions, a number of assumptions are made indetermining which compositions to use for thermo-barometry.We assume that the reconstructed omphacite was in

equilibrium with the more Mg-Ca-rich mantles of thegarnet, and that the diopside-plagioclase symplectiteswere in equilibrium with the more Mg-Ca-rich,Fe-poor outermost rims of the garnet (e.g. Fig. 9). Forpurposes of calculation, three garnet mantle composi-tions were used: (a) an average of all garnet mantlesfrom the profile shown in Table 1a (b) an average of allgarnet mantles in Fig. 9, from 65 to 99% of grainradius, and (c) the garnet mantle farthest from the

Fig. 4. Probe mount (2.5 cm diameter) ofeclogite ⁄ granulite from central Carolinaterrane, sample NEW-1–3. Pink ¼ garnet,pale green ¼ pyroxene and pyroxene-plagio-clase symplectite, brown ⁄ darkgreen ¼ hornblende, clear ¼ plagioclase orcalcite, black ¼ ilmentite or Fe-oxides. Noteplagioclase-rich kelyphite rims on garnet.

6 8 J . W . S H E R V A I S E T A L .

Table 1a. Garnet analyses, profile of single large garnet crystal in sample NEW-1. Garnet formulae per 12 oxygen.

Distance from

Centre lmCore

1

Core

51

Core

204

Core

255

Core

306

Core

508

Core

559

Core

610

Core

762

Core

813

Core

863

Core

914

Core

1016

Mantle

1117

Mantle

1168

Mantle

1270

Mantle

1371

Mantle

1472

SiO2 37.54 37.48 37.64 37.67 37.35 37.42 36.94 36.89 37.28 37.27 37.10 37.54 37.39 37.21 37.24 37.81 37.81 37.86

TiO2 0.11 0.10 0.09 0.12 0.12 0.10 0.10 0.07 0.13 0.10 0.12 0.07 0.11 0.07 0.17 0.08 0.09 0.17

Al2O3 21.37 21.40 21.59 21.37 21.54 21.71 21.46 21.44 21.32 21.25 21.30 21.30 21.27 21.46 21.27 21.49 21.46 21.31

FeO 29.37 28.82 28.86 29.07 29.00 28.93 28.88 28.82 28.97 28.93 29.05 29.17 28.46 27.69 27.27 27.20 26.68 26.53

MnO 1.60 1.49 1.27 1.14 1.07 0.81 0.75 0.68 0.47 0.37 0.38 0.32 0.20 0.12 0.12 0.13 0.10 0.12

MgO 2.41 2.33 2.36 2.39 2.40 2.38 2.39 2.48 2.62 2.68 2.76 2.93 3.09 3.34 3.25 3.33 3.39 3.47

CaO 8.62 9.28 9.34 9.41 9.44 9.73 9.87 9.92 9.88 9.84 9.79 9.64 9.90 10.38 10.73 10.71 11.10 11.10

Na2O 0.03 0.03 0.03 0.03 0.04 0.03 0.03 0.00 0.01 0.02 0.04 0.00 0.02 0.05 0.06 0.04 0.02 0.04

K2O 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00

Cr2O3 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.01 0.00 0.00 0.00 0.00 0.00 0.03 0.01 0.00

Sum 101.03 100.94 101.19 101.20 100.94 101.11 100.42 100.30 100.68 100.46 100.54 100.98 100.43 100.31 100.12 100.81 100.65 100.59

Si 2.968 2.963 2.965 2.969 2.952 2.949 2.937 2.936 2.951 2.956 2.943 2.959 2.957 2.941 2.947 2.964 2.964 2.969

Ti 0.006 0.006 0.005 0.007 0.007 0.006 0.006 0.004 0.007 0.006 0.007 0.004 0.007 0.004 0.010 0.005 0.005 0.010

Al 1.991 1.995 2.004 1.985 2.006 2.017 2.011 2.011 1.989 1.986 1.991 1.979 1.982 1.998 1.984 1.985 1.983 1.970

Fe2+ 1.942 1.906 1.901 1.916 1.917 1.907 1.920 1.918 1.918 1.918 1.927 1.923 1.882 1.830 1.805 1.783 1.750 1.740

Mn 0.107 0.100 0.085 0.076 0.071 0.054 0.051 0.046 0.031 0.025 0.025 0.021 0.013 0.008 0.008 0.009 0.006 0.008

Mg 0.284 0.275 0.277 0.281 0.282 0.280 0.283 0.294 0.309 0.317 0.326 0.345 0.365 0.394 0.383 0.389 0.396 0.405

Ca 0.730 0.786 0.789 0.795 0.799 0.821 0.841 0.845 0.838 0.836 0.832 0.814 0.839 0.878 0.910 0.899 0.932 0.933

Na 0.004 0.005 0.005 0.004 0.006 0.004 0.005 0.000 0.002 0.003 0.005 0.000 0.003 0.007 0.010 0.006 0.003 0.005

K 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000

Cr 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.002 0.001 0.000

Pyrope 9.3 9.0 9.1 9.2 9.2 9.1 9.1 9.5 10.0 10.2 10.5 11.1 11.8 12.7 12.3 12.6 12.8 13.1

Almandine 63.4 62.1 62.3 62.5 62.5 62.3 62.0 61.8 62.0 62.0 62.0 62.0 60.7 58.8 58.1 57.9 56.7 56.4

Spessartine 3.49 3.26 2.79 2.48 2.31 1.76 1.65 1.48 1.00 0.81 0.80 0.68 0.42 0.26 0.26 0.29 0.19 0.26

Grossular 23.8 25.6 25.9 25.9 26.0 26.8 27.2 27.2 27.1 27.0 26.8 26.2 27.1 28.2 29.3 29.2 30.2 30.2

Table 1b. Pyroxene (6 oxygen), hornblende (23 oxygen), and feldspar (8 oxygen) analyses from eclogite ⁄ granulite sample NEW-1.

Di Di Omp Hbl adj Hbl adj actinolite Pl in Di Pl in Di Pl in Di Pl in Di Pl in Di Pl in Di Pl in Di Pl in Di Pl in Di Interstitial Pl Interstitial Pl Interstitial Pl Interstitial Pl Interstitial Pl Interstitial Pl

SiO2 50.64 51.66 51.50 42.17 41.52 48.42 62.16 63.60 64.75 63.57 63.85 63.78 64.11 64.65 63.81 59.76 58.52 60.83 60.06 58.82 54.44

TiO2 0.32 0.18 0.26 1.11 1.11 0.73 0.51 0.02 0.00 0.02 0.00 0.02 0.01 0.03 0.08 0.04 0.06 0.00 0.00 0.00 0.00

Al2O3 4.2 3.47 9.36 11.95 12.72 6.20 22.55 22.36 22.41 23.09 22.50 23.06 22.68 22.41 22.63 25.27 26.32 25.55 25.19 26.31 28.75

FeO 11.85 11.03 9.61 18.90 18.87 15.63 0.33 0.23 0.25 0.38 0.25 0.26 0.30 0.24 0.28 0.18 0.21 0.26 0.09 0.16 0.28

MnO 0.1 0.07 0.08 0.07 0.08 0.06 0.00 0.02 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00

MgO 11.45 10.69 9.21 9.46 9.34 13.01 0.01 0.01 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00

CaO 19.45 20.27 16.51 11.53 11.26 11.89 4.25 3.19 3.14 3.63 3.23 3.77 3.29 2.94 3.43 6.46 7.51 5.81 5.89 7.35 10.34

Na2O 1.42 1.74 3.47 1.93 2.08 1.01 8.24 9.10 9.00 8.87 9.06 8.83 8.89 9.29 8.91 7.39 6.87 6.92 6.75 6.42 5.22

K2O 0.05 0.01 0.07 0.36 0.43 0.19 0.08 0.09 0.12 0.11 0.07 0.09 0.13 0.10 0.10 0.03 0.05 0.07 0.04 0.04 0.01

Cr2O3 0.01 0.00 0.01 0.00 0.01 0.02 0.00 0.00 0.00 0.00 0.01 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00

Sum 99.43 99.10 100.00 97.48 97.41 97.14 98.14 98.61 99.66 99.67 98.97 99.80 99.43 99.65 99.24 99.13 99.54 99.43 98.02 99.09 99.04

Si 1.917 1.958 1.937 6.400 6.311 7.172 2.796 2.838 2.854 2.812 2.838 2.815 2.836 2.851 2.830 2.678 2.621 2.703 2.705 2.638 2.473

Ti 0.009 0.005 0.007 0.127 0.127 0.081 0.017 0.001 0.000 0.001 0.000 0.001 0.001 0.001 0.003 0.001 0.002 0.000 0.000 0.000 0.000

Al 0.187 0.155 0.415 2.137 2.278 1.083 1.196 1.176 1.165 1.203 1.179 1.200 1.183 1.165 1.183 1.335 1.390 1.338 1.337 1.390 1.539

Fe2+ 0.375 0.350 0.302 2.399 2.398 1.936 0.013 0.009 0.009 0.014 0.009 0.009 0.011 0.009 0.010 0.007 0.008 0.010 0.004 0.006 0.011

Mn 0.003 0.002 0.003 0.009 0.010 0.008 0.000 0.001 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000

Mg 0.646 0.604 0.516 2.140 2.116 2.871 0.001 0.001 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000

Ca 0.789 0.823 0.665 1.874 1.834 1.887 0.205 0.153 0.148 0.172 0.154 0.179 0.156 0.139 0.163 0.311 0.361 0.277 0.284 0.353 0.503

Na 0.1042 0.128 0.253 0.568 0.613 0.290 0.719 0.787 0.769 0.761 0.781 0.755 0.763 0.794 0.766 0.642 0.596 0.597 0.590 0.559 0.460

K 0.002 0.001 0.003 0.070 0.083 0.035 0.005 0.005 0.007 0.006 0.004 0.005 0.007 0.005 0.006 0.002 0.003 0.004 0.002 0.002 0.001

Cr 0.000 0.000 0.000 0.000 0.001 0.003 0.000 0.000 0.000 0.000 0.001 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000

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centre of the grain in Table 1a (but not the rim), cor-responding to the analysis at 1371 lm. For the garnetrim compositions, we used the garnet rim fromTable 1a (at 1472 lm) and the average rims of thethree garnet shown in Fig. 9. Garnet-pyroxene tem-peratures were calculated using the calibrations of Ellis& Green (1979) and Powell (1985).Because there is no indication of primary plagioclase

in equilibrium with omphacite, only minimum pres-sures are estimated for the inferred eclogite assemblageusing the plagioclase in diopside symplectite as aproxy, using the diopside-plagioclase-garnet-quartz(Newton & Perkins, 1982; Powell & Holland, 1988;Moecher et al., 1988), and albite-jadeite-quartz geo-barometers (Holland, 1980). For the high-P granuliteassemblage, we used diopside-plagioclase-garnet-quartz (Newton & Perkins, 1982; Powell & Holland,1988; Moecher et al., 1988) to estimate pressure, andthe jadeite content of clinopyroxene geobarometer ofCarswell & Harley (1990), to give a minimum pressurefor the eclogite assemblage.For hornblende-bearing assemblages, the garnet-

hornblende (Graham& Powell, 1984) thermometer andgarnet-plagioclase-hornblende-quartz geobarometer(Kohn & Spear, 1989, 1990), were used, taking only the

Table 1c. Hornblende-plagioclase pairs from retrograded eclogite ⁄ granulite sample NEW-1.

Sample# Hb-1a Hb-2a Hb-2b Hb-3a Hb-4a Hb-5b Hb-6a Hb-6c Hb-8 Hb-8a Hb-9 Hb-10 Hb-11 Hb-12

SiO2 39.97 37.91 39.84 42.00 40.88 40.82 40.65 42.44 42.57 43.46 39.38 40.76 42.99 40.97

TiO2 1.28 1.28 1.45 0.87 1.31 0.54 0.88 1.32 1.41 1.33 0.88 0.96 1.11 1.00

Al2O3 13.58 16.39 14.33 11.69 12.54 13.80 13.16 10.33 11.03 10.22 14.98 13.43 11.04 12.97

Cr2O3 0.02 0.01 0.01 0.01 0.02 0.01 0.02 0.02 0.00 0.00 0.00 0.00 0.00 0.00

Fe2O3 6.01 6.19 5.56 6.26 6.30 6.72 6.84 5.77 5.13 5.05 7.02 6.75 5.27 6.52

FeO 12.56 11.83 11.86 12.34 12.97 12.95 13.96 14.21 11.81 11.42 12.28 11.44 12.31 11.93

MnO 0.04 0.05 0.05 0.04 0.03 0.08 0.08 0.06 0.03 0.01 0.05 0.00 0.04 0.02

MgO 9.27 8.64 9.65 10.01 9.42 8.88 8.48 9.50 11.03 11.52 8.74 10.01 10.68 9.87

CaO 11.61 11.72 11.65 11.72 11.55 11.63 11.67 11.42 11.44 11.83 11.54 11.97 11.79 11.85

Na2O 2.09 2.22 2.17 1.85 2.04 2.00 2.03 1.89 1.93 1.75 2.15 1.99 1.80 1.99

K2O 0.55 0.66 0.54 0.38 0.45 0.49 0.46 0.37 0.55 0.36 0.51 0.48 0.42 0.46

H2O 2.00 2.00 2.00 2.00 2.00 2.00 2.00 2.00 2.00 2.00 2.00 2.00 2.00 2.00

Total 98.98 98.90 99.11 99.17 99.51 99.92 100.23 99.33 98.93 98.95 99.53 99.79 99.45 99.58

Si 6.053 5.749 5.998 6.316 6.162 6.124 6.120 6.419 6.384 6.490 5.935 6.092 6.419 6.145

Ti 0.146 0.146 0.164 0.098 0.149 0.061 0.100 0.151 0.159 0.149 0.100 0.108 0.125 0.112

Al 2.425 2.929 2.544 2.074 2.228 2.441 2.335 1.842 1.951 1.800 2.661 2.367 1.944 2.293

Cr 0.002 0.001 0.002 0.001 0.002 0.001 0.002 0.002 0.000 0.000 0.000 0.000 0.000 0.000

Fe3+ 0.685 0.707 0.630 0.709 0.715 0.759 0.775 0.656 0.579 0.567 0.796 0.760 0.592 0.736

Fe2+ 1.592 1.501 1.493 1.552 1.635 1.625 1.757 1.798 1.481 1.426 1.548 1.430 1.537 1.497

Mn 0.006 0.006 0.007 0.004 0.004 0.010 0.010 0.008 0.004 0.001 0.006 0.000 0.005 0.003

Mg 2.092 1.952 2.165 2.243 2.115 1.987 1.902 2.141 2.465 2.563 1.964 2.229 2.377 2.206

Ca 1.885 1.904 1.879 1.889 1.866 1.869 1.883 1.851 1.839 1.893 1.863 1.917 1.887 1.905

Na 0.614 0.654 0.633 0.540 0.597 0.581 0.592 0.555 0.560 0.507 0.627 0.577 0.522 0.577

K 0.106 0.128 0.103 0.073 0.087 0.093 0.088 0.072 0.105 0.069 0.097 0.092 0.080 0.089

Plagioclase Pl-1a Pl-2a Pl-2b Pl-3a Pl-4a Pl-5b Pl-6a Pl-6c Pl-8 Pl-8a Pl-9 Pl-10 Pl-11 Pl-12

SiO2 64.89 54.44 60.06 64.71 58.82 57.81 58.09 64.30 64.70 65.71 62.40 63.95 65.38 60.83

Al2O3 23.30 28.75 25.19 23.60 26.31 26.85 27.44 23.35 23.46 23.49 24.69 23.88 24.52 25.55

CaO 3.03 10.34 5.89 3.23 7.35 7.99 8.50 3.29 2.75 2.70 4.84 3.53 2.98 5.81

Fe2O3 0.21 0.28 0.09 0.13 0.16 0.22 0.18 0.25 0.13 0.15 0.18 0.22 0.20 0.26

Na2O 7.61 5.22 6.75 7.46 6.42 6.41 6.24 8.68 7.46 7.42 7.14 7.40 7.26 6.92

K2O 0.06 0.01 0.04 0.07 0.04 0.04 0.03 0.09 0.09 0.10 0.06 0.07 0.10 0.07

Total 99.10 99.04 98.02 99.19 99.09 99.31 100.47 99.95 98.56 99.56 99.30 99.04 100.46 99.43

Si 2.855 2.473 2.705 2.845 2.638 2.597 2.582 2.825 2.856 2.869 2.7620 2.822 2.834 2.703

Al 1.209 1.540 1.337 1.223 1.391 1.422 1.437 1.209 1.221 1.209 1.288 1.242 1.253 1.338

Ca 0.143 0.503 0.284 0.152 0.353 0.385 0.405 0.155 0.130 0.126 0.230 0.167 0.139 0.277

Fe3+ 0.008 0.011 0.004 0.005 0.006 0.008 0.007 0.009 0.005 0.005 0.007 0.008 0.007 0.010

Na 0.649 0.460 0.590 0.636 0.559 0.558 0.538 0.739 0.639 0.628 0.613 0.633 0.610 0.597

K 0.004 0.001 0.002 0.004 0.002 0.002 0.001 0.005 0.005 0.005 0.003 0.004 0.006 0.004

Xalbite 0.82 0.48 0.67 0.80 0.61 0.59 0.57 0.82 0.83 0.83 0.73 0.79 0.81 0.68

DiopsideWo 50

800 °C

600 °C

1000 °C

1200 °C 1000 °C

Interstitial Plagioclase

Plagioclase Symplectitein Pyroxene

B

A

Jadeite

Enstatite

ReconstructedOmphacite

ExsolvedDiopside

DiHd to EnFs

Fig. 5. Mineral data from eclogite ⁄ granulite sample NEW-2:(a) Jadeite-high Ca Px-Low Ca Px ternary plot, showing analyzedpyroxene (squares) and reconstructedomphacite (X); (b) pyroxenequadrilateral plot showing analyzed pyroxene (squares), alongwith temperature contours of Lindsley & Anderson (1983);(c) albite corner of the feldspar ternary, showing compositionsof plagioclase symplectite in diopside (open) and interstitialplagioclase associated with hornblende (closed).

7 0 J . W . S H E R V A I S E T A L .

Fig. 6. X-ray composition maps of diopside-sodic plagioclase symplectites (¼ former omphacite) surrounded by hornblende, plagioclase, garnet, and calcite. (A) Mg map,New-1; (B) Ca map, New-1; (C) Al map, 3080E (D) Al map, 3080E. (A, B) Field of view ¼ 5 mm, hotter colours equal higher concentrations. Note shapes of the diopside-plagioclase-hornblende aggregates, which seem to pseudomorph the primary omphacite. (C, D) Field of view 2.5 mm. Lighter shades ¼ higher concentrations.

A B C D

Fig. 7. X-ray maps of zoned garnet surrounded by hornblende with minor plagioclase and ilmenite. A ¼ Fe, B ¼ Mn, C ¼ Mg, D ¼ Ca. Garnet has high Mn and Fein core, with higher Mg and Ca in mantle. Note the sharp contact between the inner garnet core and the outer garnet mantle seen clearly in the Fe and Ca X-ray maps.Note also the small garnet cores (high Mn and Fe, low Ca and Mg) that have been subsumed by the garnet mantle. Hotter colours equal higher concentration in Fe, Mn,and Mg; darker blue equals higher Ca. Black line in A is approximate location of line profile (Table 1a). Field of view is 5 mm in all maps.

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outermost rim analysis of the garnet in Table 1a andselected hornblende-plagioclase pairs from Table 1c.Hornblende-plagioclase temperatures (Holland &Blundy, 1994) were also calculated using the data fromTable 1c, which represent adjacent hornblende-plagio-clase pairs from a range of textural associations. Wealso used GRIPS (garnet-rutile-ilmenite-plagioclase-silica, Bohlen & Liotta, 1986) to estimate pressure, sinceilmenite is associated with the hornblende-formingreactions.Calculation of equilibrium T-P conditions was car-

ried out using the program GTB of Spear & Kohn(2001), and the hornblende-plagioclase program ofHolland & Blundy (1994). The pyroxene quadrilateralthermometer of Lindsley & Anderson (1983) is usedfor diopside (but not reconstructed omphacite) becauseits nonquadrilateral components are less than 20%

(Fig. 5). The results from this graphical solvus thermo-meter �700–800 �C, or up to �50 �C higher thanresults from the garnet rim-diopside thermometers(700–750 �C). Garnet-clinopyroxene temperatureswere calculated using stoichiometry to partition totalFe between Fe2+ and Fe3+; calculation of Fe3+ stoi-chiometrically is strongly dependent on analyticalprecision and generally overestimates Fe3+ in pyroxenedue to vacancies in the pyroxene lattice (e.g. Robinson,1980). Calculation of garnet-diopside temperaturesassuming total Fe as Fe2+ results in temperatures50–80 �C higher than those using calculated Fe3+

(Table 2). The c. 50 �C difference between the pyrox-ene solvus temperatures and garnet-diopside tempera-tures calculated here probably results from theoverestimation of Fe3+ using stoichiometry.Variations in hornblende-plagioclase temperatures

correlate with texture and composition, as noted ear-lier. Aluminous pargasite and calcic plagioclase thatreplace diopside-plagioclase symplectites formed athigher temperatures than the magnesian pargasite andsodic plagioclase that replace garnet and form thegroundmass in highly amphibolitized samples. Fig-ure 10 shows hornblende-plagioclase temperatures as afunction of plagioclase composition at 1.2 GPa, whichis the mean pressure calculated for these assemblages.The high temperature hornblende-plagioclase assem-blage clearly replaces pre-existing diopside-plagioclasesymplectites, but formed at similar temperatures andpressures, probably in response to increased PH2Oduring the thermal peak; we speculate that this watermust have come from dehydration reactions in theenclosing felsic gneisses.Using the data and methods described above, the

following equilibration conditions are suggested foreach stage of metamorphism, with each diagnosticassemblage shown in parentheses:(1) Eclogite facies metamorphism of a mafic protolith(garnet mantle + omphacite + rutile) at 650–730 �Cand ‡ 1.4 GPa.(2) HP granulite facies conditions during decompres-sion (garnet rim + diopside + pargasite I + plagio-clase) at 700–800 �C and 1.2–1.5 GPa.(3) Amphibolite facies conditions (pargasite II +plagioclase + ilmenite ± epidote) at 660 �C to 720 �Cand 0.9–1.2 GPa.These data are summarized in Table 2 and Fig. 11,

which depicts the calculated equilibria for variousmineral associations and facies with ellipses thatoverlie the intersection of geothermometer and geo-barometer equilibria for each stage of metamorphism.In the absence of primary plagioclase, the pressureestimated for the eclogite assemblage (P ¼ 1.4 GPa)is a minimum equilibration pressure; this may belowered somewhat based on the high Fe content of thesample, but may also be considerably higher (Carswell& Harley, 1990). The equilibration pressures of theHP granulite assemblage (1.2–1.5 GPa) are well

Fig. 8. Profile of single large garnet grain, from centre to rim.Distance from rim in lm. Note sharp increase in Grs (CaO) anddecrease in Alm (FeO) at around 1150 lm. Pyr (MgO) showsless precipitous increase, Sps (MnO) decays exponentiallytoward rim.

7 2 J . W . S H E R V A I S E T A L .

constrained since plagioclase and quartz are present inboth assemblages.The conditions calculated for these assemblages

imply a clockwise pressure-temperature-time (P-T-t)path (Fig. 11). The clockwise P-T-t configuration isconsistent with models that involve collision of largecontinental or arc blocks, where one block is thrustbeneath another (high pressure at relative low tem-peratures) and then rebounds to an equilibriumgeothermal gradient when the block is exhumed duringuplift (England & Thompson, 1984). Based on thepreservation of primary zoning profiles in the garnet attemperatures up to 800 �C, we suggest that uplift andcooling must have been relatively rapid after peakmetamorphic conditions were reached (O’Brien, 1997;Cooke et al., 2000).

Protolith of mafic boudins and layers

Field relations suggest that protoliths of the maficboudins and layers were originally mafic dykes intru-ded into the more abundant felsic gneisses that com-pose the country rock of the Silverstreet domain.Whole rock analyses presented here (Table 3) andelsewhere (Dennis & Shervais, 1991, 1996) show thatthe felsic gneisses were derived from arc-related felsicto intermediate composition metavolcanic and meta-plutonic rocks of Charlotte belt affinity.Most of the mafic boudins and dykes are basaltic in

composition, with SiO2 � 50%, MgO � 6–8%,FeO* � 10% and TiO2 � 1–3% (Fig. 12). Thesecompositions are typical of oceanic basalts, but are toohigh in TiO2 to represent arc-related high-alumina

0.5

1.5

2.5

3.5

Table 2. Summary of T-P data for high-P mafic lithology from Silverstreet domain. Numbers in brackets refer to references listedbelow.

Assemblage Facies Themometer Temperature Barometer Pressure

1 Eclogite Grt-Cpx 650–730 �C @1.4 GPa [1,2] Grt-Cpx-Pl-Qtz

Jd-Ab-Qtz

> 1.3 GPa @700 �C [6]> 1.5 GPa @700 �C [7,8]> 1.4 Gpa @700 �C [9]

2 High P Granulite Grt-Cpx 700–750 �C @1.2–1.5 GPa [1,2] Grt-Cpx-Pl-Qtz 1.2 GPa @800 �C [6,7]Grt-Cpx 760–780 �C @1.2–1.5 GPa [1,2]* 1.5 GPa @800 �C [7,8]Cpx Solvus �700–800 �C [3]Grt-Hbl 770–820 �C @1.2 GPa [4] Grt-Hbl-Pl-Qtz 1.2–1.5 GPa @800 �C [10]Hbl-Pl 760–830 �C @1.2 GPa [5] GRIPS 1.2–1.5 GPa @800 �C [11]

3 Amphibolite Grt-Hbl 660–775 �C @1.2 GPa [4] Grt-Cpx-Pl-Qtz 1.0–1.2 GPa @700 �C [10]Hbl-Pl 690–740 �C @1.2 GPa [5] GRIPS 1.0–1.2 GPa @675 �C [11]

References [1] Ellis & Green (1979); [2] Powell (1985); [3] Lindsley & Anderson (1983); [4] Graham & Powell (1984); [5] Holland & Blundy (1994); [6] Newton & Perkins (1982); [7] Powell &

Holland (1988); [8] Moecher et al. (1988); [9] Holland (1980); [10] Kohn & Spear (1989); [11] Bohlen & Liotta (1986). All temperatures with Fe3+ correction except *.

Fig. 9. Combined profiles of three garnet grains in sample NEW-1, scaled to percentradius of grain. Note sharp increase in Grs (CaO) and decrease in Alm (FeO) at around60% of total radius. Pyr (MgO) shows less precipitous increase, Sps (MnO) decaysexponentially toward rim.

D E E P I N T H E H E A R T O F D I X I E 7 3

basalts. Two samples are somewhat unusual ferro-basalts, with SiO2 � 41%, MgO � 6%, FeO* �15–18%, and TiO2 � 2.5–3.5% (Fig. 12). They arechemically equivalent to evolved tholeiitic basalts, withvery low Cr and Ni (<50 p.p.m). Similar ferrobasalticcompositions were reported by Dal Piaz & Lombardo(1986), Galan & Marcos (2000), and Will & Schma-dicke (2001). All of the basalts and ferrobasalts studiedhere can be classified as mid-ocean ridge basalts orocean island basalts using geochemical discriminationplots such as Ti-V and Ti-Zr (Fig. 13; Shervais, 1982;Pearce & Cann, 1973). This oceanic affinity contrastswith the characteristic arc-related compositions of thesurrounding felsic to intermediate gneisses and otherrocks of the Charlotte belt (Dennis & Shervais, 1991,1996). Similar relationships are observed in the Pro-terozoic Nagssugtoqidan mobile belt of east Greenland(Messiga et al., 1990).

DISCUSSION

Tectonic setting of high pressure metamorphism

The equilibration conditions calculated here imply aclockwise P-T-t path for mafic rocks of the Silverstreetdomain, consistent with collision of two crustal blocksduring attempted subduction of one of these blocks.These conditions are similar to those inferred for othermedium temperature eclogites and related high-pres-sure granulites (e.g. Carswell & O’Brien, 1993; Galan& Marcos, 2000; Cooke et al., 2000; Will & Schma-dicke, 2001; O’Brien & Rotzler, 2003). In many cases,medium temperature eclogites are associated withcontinent-continent collisions, as seen in the Norwe-gian and Greenland Caledonides (Krogh, 1982; Cuth-bert & Carswell, 1990; Cuthbert et al., 2000; Elvevold& Gilotti, 2000) and the Variscan foldbelts of centralEurope (O’Brien et al., 1990; Galan & Marcos, 2000;Cooke et al., 2000; Will & Schmadicke, 2001; O’Brien& Rotzler, 2003).The Kohistan arc terrane of northern Pakistan may

provide the closest analogue to the rocks studied here,because it involves collision of an island arc with acontinental margin (Jan & Howie, 1981; Coward et al.,1987; Khan et al., 1989). High pressure granulites ofthe Jijal complex formed at the base of the Kohistanarc, possibly during its amalgamation with Asia (e.g.Coward et al., 1987; Khan et al., 1989). It was exposedduring the subsequent collision of India with the com-bined Kohistan-Asia block, during which Kohistan wasin the upper plate of the collision (Coward et al., 1987).The c. 450 Ma eclogites of the Eastern Blue Ridge

province of the southern Appalachians are not relatedto the MT eclogite ⁄HP granulites from the Carolinaterrane described here. The Blue Ridge eclogites areinterpreted as low temperature (LT) eclogites formedduring the subduction of Ordovician oceanic crustbeneath the Inner Piedmont terrane (Willard & Adams,1994; Adams et al., 1995; Adams & Trupe, 1997). These

400 500 600 700 800 9000

0.4

0.8

1.2

1.6

2

T ˚C

P G

Pa

Combined P-T path for Silverstreet domain

2 = Granulite Gt-Cpx-Hb-Pl1 = Eclogite Gt-Omp

3 = Amphibolite Gt-Hb-Pl-Ilm

12

3

Eclogite

High-PGranulite

Amphibolite

Fig. 11. P-T-t plot showing clockwise path, with isobaricheating from granulite to hornblende granulite assemblages.1 ¼ inferred eclogite (reconstructed omphacite-plagio-clase-garnetmantles;minimumpressures only); 2 ¼ high-pressuregranulite (diopside-pargasite-plagioclase-garnet rims-ilmenite);3 ¼ amphibolite (pargasite II-plagioclase-ilmenite-epidote).

680

700

720

740

760

780

800

820

840

0.40 0.50 0.60 0.70 0.80 0.90 1.00

T@1.0 GPa

Hbl

-Pl T

empe

ratu

res

Albite

Fig. 10. Plot of hornblende-plagioclase temperatures at 1.0 GPapressure, using Holland & Blundy (1994), as a function ofplagioclase composition. The strong correlation of calculatedtemperature with composition is consistent with observedchanges in assemblage and texture.

7 4 J . W . S H E R V A I S E T A L .

rocks were preserved in thrust sheets during the Alle-ghanian collision of North America with Gondwana inthe late Palaeozoic (Stewart et al., 1997).

Regional Implications

One conclusion that seems inescapable at this time isthat the Carolina terrane, as it is now understood, is acomposite terrane composed of two previously unre-lated arcs: the Charlotte belt arc and the Carolinaslate belt arc. Amalgamation of these two arcs toform the Carolina terrane must have occurred far

from Laurentia, and prior to accretion of the Caro-lina terrane to the Laurentian margin (Late Palaeo-zoic). Since the Silverstreet domain appears to be partof the Charlotte belt and may represent in part theinfrastructure of the Charlotte belt arc, subductionpolarity during amalgamation of the Charlotte beltarc with the Carolina slate belt arc must have been tothe SE (present day co-ordinates; Fig. 14). That is,the Charlotte belt arc formed part of the lower plateassemblage that was over-ridden by the Carolina slatebelt arc (which formed part of the upper plate of thesubduction zone).

Table 3. Whole rock major and trace element analyses by X-ray fluorescence.

Sample#

Rock

type

3080

Ferro-

basalt

NEW-2

Ferro-

basalt

3070–1

Basalt

3070–2

Basalt

3070–3

Basalt

3070–4

Basalt

3071UP

Amphib-

olite dyke

3071 A

Mafic

boudin

3071B

Mafic

boudin

3071C

Mafic

boudin

3071–4

Amphib-

olite dyke

3071–5

Amphib-

olite dyke

3071 FG

Felsic

Gneiss

3025 A

Felsic

Gneiss

3025B

Felsic

Gneiss

SiO2 41.7 41.5 50.1 49.8 49.1 50.4 51.0 49.3 50.4 49.3 50.3 48.0 54.9 60.6 60.0

TiO2 2.77 3.60 0.54 1.20 1.31 1.32 1.14 2.56 3.15 3.12 2.05 1.24 1.16 0.89 0.88

Al2O3 16.24 13.01 16.86 13.50 13.70 13.32 15.10 16.20 15.36 15.67 12.69 15.01 19.88 16.53 16.79

Fe2O3 16.70 20.36 7.38 12.11 11.71 13.12 10.69 11.66 12.70 12.37 14.23 11.66 9.93 8.37 8.54

MnO 0.13 0.18 0.13 0.20 0.22 0.20 0.17 0.17 0.16 0.20 0.25 0.20 0.08 0.33 0.33

MgO 5.61 6.48 8.65 8.00 7.83 5.83 6.67 5.81 5.84 5.82 5.83 6.75 2.49 1.17 1.24

CaO 13.51 11.30 11.48 12.31 12.87 13.18 10.92 10.43 9.46 10.10 10.36 13.06 2.96 3.69 3.87

Na2O 2.09 2.10 2.72 2.57 2.20 2.03 2.91 1.70 1.78 1.57 2.21 1.99 4.98 4.16 4.29

K2O 0.176 0.209 0.606 0.39 0.398 0.132 1.091 0.956 0.495 0.697 1.228 0.707 2.948 3.006 2.903

P2O5 0.100 0.076 0.045 0.106 0.094 0.163 0.090 0.498 0.450 0.481 0.224 0.112 0.031 0.123 0.145

Total 99.03 98.84 98.47 100.18 99.43 99.71 99.79 99.25 99.82 99.36 99.40 98.76 99.31 98.84 98.94

p.p.m.

Nb 2.4 2.5 1.4 2.8 3.3 3.2 4.7 21.1 25.9 25.2 9.5 3.3 23 12.1 12.3

Zr 66 32 33 60 64 61 65 230 273 244 122 69 177 259 273

Y 17 14 14 23 23 20 22 37 42 37 37 28 13 59 63

Sr 937 100 180 59 116 85 210 548 367 436 133 274 255 422 418

Rb 5 4 19 7 6 5 15 47 13 33 20 15 160 55 53

Sc 50.1 52.6 40.3 38.3 44.2 41.7 36.1 35.1 39.2 37.6 39.2 51.2 10.2 8 9.4

V 666 734 171 309 324 341 293 363 438 397 406 325 172 70 82

Cr 30 43 259 288 283 76 125 160 185 186 65 268 123 10 15

Ni 8 18 158 78 63 69 65 67 49 55 48 112 79 8 10

Cu 46 107 107 96 90 44 62 31 9 30 138 148 121 41 29

Zn 117 124 47 88 87 93 86 90 98 89 112 99 116 81 85

Ba 34 19 13 85 117 12 77 bdl bdll bdl 26 168 365 659 586

Note: Major elements in weight percentage oxide, trace elements in p.p.m.

(a) (b) (c)

(d) (e) (f)

Fig. 12. Harker diagrams for eclogite ⁄ high-P granulites of the Silverstreet domain, along with three felsic gneiss host rocks. Plots showSiO2 vs. (a) TiO2 (b) FeO* (c) MgO and CaO (d) Na2O and K2O (e) Cr and Ni p.p.m., and (e) Zr p.p.m.

D E E P I N T H E H E A R T O F D I X I E 7 5

Alternatively, Hibbard & Samson (1995) have sug-gested that collision between Carolina and the Gren-ville-aged Goochland terrane of eastern Virginia(Farrar, 1984) might be responsible for the meta-morphic fabric of the western Carolina terrane.Mueller et al. (1996) and Heatherington et al. (1996)have presented results based on their work in NorthCarolina that suggest a swing in Nd isotopic compo-sitions of Carolina lavas from strongly positive eNd tonear 0 or even negative at approximately the Cambrianboundary. A complex collision between a c. 1.1 Gacontinental fragment and some portion of the Carolinacomposite terrane could explain this observed swing inisotopic compositions and some of the xenocrysticzircon in Albemarle Group lavas from the NorthCarolina slate belt. Subsequent terrane dispersalduring postcollisional strike-slip faulting could beresponsible for the present disposition of high pressurerocks far from the present outcrop belt of theGoochland terrane. However, since the Charlotte belt-Silverstreet arc must have been in the lower plate of thecollision, the upper plate would have to include an arc

assemblage that was active at the time of collision; thisis not observed in the Goochland terrane.The high pressure metamorphic event documented

here must predate the c. 415 Ma Newberry granite(which is unaffected by the amphibolite facies over-print, and contains xenoliths of the sheared felsicgneisses which host the eclogites), and it must postdateformation of the Carolina arc (c. 620 to 550 Ma;Dennis et al. 1997; Dennis & Wright, 1997; Samsonet al., 1995; Wortman et al., 1996, 2000; Barker et al.,1998). High-P metamorphism may coincide with the c.535 Ma collisional event documented in the westernCharlotte belt by Dennis & Wright (1997), or it mayrepresent an older, as yet unrecognized collisionalevent that occurred within the Carolina terrane priorto its amalgamation with Laurentia.The occurrence of MORB-chemistry dykes in the

roots of the arc implies that prior to its collision andpartial subduction beneath the Slate belt arc, theCharlotte belt-Silverstreet arc may have collided withand over-ridden an active spreading centre. This isconsistent with the collision of two arcs that wereoriginally separated by a spreading centre, whichwould have to be consumed before collision of the twoarcs could occur (Fig. 14). It may also explain the hightemperatures and isobaric heating observed in theSilverstreet domain.

Uplift and Exhumation

High-pressure, MT granulites ⁄ eclogites of the Silver-street domain were exhumed and cooled extremelyrapidly, as shown by the preservation of progradezoning profiles in garnet that formed at 660–820 �C(e.g. O’Brien, 1997). These profiles could not persist ifthe boudins were held for long times at such hightemperatures. Exhumation of high-P metamorphicrocks involves two related problems: (1) a driving forcefor uplift of the crust, and (2) the dominant mechanismfor exhumation – erosion vs. low-angle normal faulting(Jamieson & Beaumont, 1989). In this context, upliftrefers to upward movement with respect to a fixeddatum, whereas exhumation refers to unroofing andmovement to lower lithostatic pressures (Jamieson &Beaumont, 1989; Ring et al., 1999).There are two possible models that may drive the

uplift of deeply buried rocks in subduction zones orcollision zones, both related to the buoyancy of crustalrocks at depth: (1) the buoyancy of tectonically thickencrust when material is removed from the upper crustby erosion or faulting, or (2) break-off of the sub-ducting slab, thus removing slab pull and allowing thesubducting crust to return buoyantly to the surface(von Blanckenburg & Davies, 1995; Ernst et al., 1997).We favour the slab breakoff model as the releasemechanism for uplift, because it is a logical conse-quence of the partial subduction of a buoyant blockattached to oceanic lithosphere, and because the twoarcs involved in this collision (Charlotte belt, Slate

0

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0 50 100 150 200 250 300

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ferro-basalts

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0 5000 10000 15000 20000 25000

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Fig. 13. Ti-V and Ti-Zr plots for eclogite ⁄ granulite blocksfrom Silverstreet domain, showing MORB ⁄OIB affinities ofthe mafic rocks.

7 6 J . W . S H E R V A I S E T A L .

belt) were likely too thin to generate great thicknessesof crust. In addition, it would allow isobaric heatingfollowed by sudden and rapid pressure release andcooling.Exhumation, defined as the return of deeply buried

rocks to the surface, is generally driven either by ero-sion, low-angle normal faulting, or both; ductileextension of the crust or lithosphere is slow and cannotaccount for more than a small fraction of exhumation(Ring et al., 1999). Erosion and low-angle normalfaulting both operate at similar rates (5–13 km Myr) 1

for erosion, 5–10 km Myr)1 for normal faulting) andeither can account for the rapid cooling required topreserve the growth zoning in garnet. In the case of theSilverstreet domain, we suggest that low angle faultingwas the dominant process, because the fault contactbetween the Charlotte belt and Slate belt removes asignificant thickness of metamorphic section (c. 14 km)and juxtaposes terranes with significantly differentmetamorphic facies. Clearly, this process must havebeen aided by rapid erosion to remove material fromthe footwall, but erosion alone cannot account for thejuxtaposition of terranes with distinctly differentmetamorphic grades and palaeodepths (Platt, 1986,1993).

CONCLUSIONS

Mafic meta-igneous rocks found along the boundarybetween the Charlotte belt and the Carolina Slate beltpreserve metamorphic phase assemblages that imply

progressive ⁄ retrogressive metamorphism under eclog-ite, high pressure granulite, and amphibolite faciesconditions. These rocks define a clockwise P-T-t path,consistent with collision and partial subduction. Wesuggest that this collision may have occurred duringamalgamation of the Charlotte belt to the CarolinaSlate belt to form the composite Carolina terrane thatwas later accreted to Laurentia.Our conceptual model for this collision, based on the

data discussed above, is outlined in Fig. 14. In stage 1,the Charlotte belt arc and the Slate belt arc face oneanother across an active spreading centre. The Char-lotte belt arc over-rides this spreading centre in stage 2,leading to the emplacement of MORB compositiondykes in the dominantly felsic arc basement. By stage3, the Charlotte belt arc became extinct and attachedto oceanic crust still subducting beneath the Slate beltarc. Collision occurred during stage 4, with theCharlotte belt arc in the lower plate being partiallyover-ridden by the Slate belt arc, leading to the high-pressure metamorphism at eclogite and high-P granu-lite facies conditions. During stage 5 the subductingoceanic slab broke off, allowing rapid exhumationof the Charlotte belt arc basement, possibly along alow-angle normal fault. Finally (stage 6) subductionwas re-established beneath the combined Charlottebelt-Slate belt arc with renewed volcanism and plut-onism, and possible reactivation of the suture as ahigh-angle transcurrent structure. Further work isneeded to refine and test this model in other parts ofthe Carolina terrane.

Fig. 14. Model for collision and amalgamation of the Charlotte belt ⁄Slate belt arcs. Stage 1: convergence of Charlotte belt and Slatebelt arcs, separated by mid-ocean ridge spreading centre; Stage 2: collision of Charlotte belt with MOR, emplacement of MORBcomposition dykes into infrastructure of the arc; Stage 3: continued convergence of Charlotte belt and Slate belt arcs, with detachmentand sinking of subducted lithosphere; Stage 4: collision of Charlotte belt and Slate belt arcs, with eclogite facies metamorphism ofCharlotte belt arc infrastructure; Stage 5: delamination and sinking of oceanic lithosphere at leading edge of Charlotte belt arc,followed by rapid uplift and exhumation of Charlotte belt infrastructure; granulite and then amphibolite facies overprint duringexhumation; Stage 6: postcollisional �Carolina terrane� compositer arc; later arc volcanism and sedimentation may represent overlapassemblages that postdate suture; later reactivation of suture during Alleghanian sinistral shear?

D E E P I N T H E H E A R T O F D I X I E 7 7

ACKNOWLEDGEMENTS

The authors thank R. Jamieson and J. Gilloti for theirthoughtful and detailed reviews, A. Indares for edi-torial handling, and especially M.J. Kohn for discus-sions of thermobarometry issues. We also thankA. Bell and M. A. Jones (deceased) for assistance in thefield. This work was supported by NSF grantEAR9805159 to Dennis and Shervais.

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Received 26 October 2001; revision accepted 8 July 2002.

APPENDIX: METHODS

All minerals were analyzed on the Cameca SX-50 electron micro-probe at the University of South Carolina using natural and syn-thetic mineral standards from the Smithsonian Institution;operating conditions were typically 20 KV at 25 nA. Data reductionwas carried out using the Cameca implementation of the phi-rho-zalgorithm (Pouchou & Pichoir, 1991). Large area X-ray composi-tion mapping was carried out in stage mode using four fixedwavelength spectrometers in conjunction with the backscatteredelectron (BSE) diodes. Typical maps are 512 · 512 pixels with a stepsize 10 lm and dwell time of 200 milliseconds, for a total area scannedof 5.0 · 5.0 mm and an analysis time of about 14 h per map.

Omphacite was reconstructed from diopside-plagioclase symplec-tite by acquiring a series of BSE images on different diopside grains,which were then segmented in the Cameca image analysis software torecover the proportion of plagioclase in diopside. Results for allgrains imaged were around 20% modal plagioclase. The inferredomphacite composition was reconstructed by converting the averagecomposition of plagioclase in symplectite to a mineral formulaand subtracting one mole of SiO2 to create jadeite. The jadeiteformula was converted back to weight% oxide and mixed with theaverage composition of diopside in 20 : 80 proportions to createomphacite.Calculation of Fe3+/Fe2+ by stoichiometry for thermobarometry

followed method of Spear (1993).

8 0 J . W . S H E R V A I S E T A L .