Pressure–Temperature Evolution of a Late Palaeozoic Paired Metamorphic Belt in North–Central Chile (34 (cid:1) –35 (cid:1) 30 0 S)

In the Chilean Coastal Cordillera, two units, the Western and Eastern Series, constitute coeval parts of a Late Palaeozoic paired metamorphic belt dominated by siliciclastic metasediments. The Western Series also contains rocks from the upper oceanic crust and represents an accretionary prism. Omnipresent high-pressure conditions are reflected by Na–Ca-amphibole and phengite in greenschists. Peak PT conditions of 7 (cid:2) 0–9 (cid:2) 3 kbar, 380–420 (cid:1) C point to a metamorphic gradient of 11–16 (cid:1) C/km. Three unique occurrences of blueschist yield deviating conditions of 9 (cid:2) 5–10 (cid:2) 7 kbar, 350– 385 (cid:1) C and are interpreted as relics from the lowermost part of the basal accretion zone preserving the original gradient of 9–11 (cid:1) C/km along the subducting slab. Pervasive ductile deformation related to basal accretion occurred near peak PT conditions. Deformation and PT evolution of the metapsammopelitic rocks is similar to that of the metabasites. However, a rare garnet mica-schist yields peak PT conditions of 9 (cid:2) 6–14 (cid:2) 7 kbar, 390–440 (cid:1) C reflecting a retrograde stage after cooling from a high-temperature garnet-forming stage. It is considered to be an exhumed relic from the earliest siliciclastic rocks subducted below a still hot mantle wedge. A retrograde overprint of all rock types occurred at (cid:3) 300–380 (cid:1) C. Continuous reactions caused crystal growth and recrystallization with abundant free water mostly under strain-free conditions. They record a pressure release of 3–4 kbar without erasing peak metamorphic mineral compositions. The Eastern Series lacks metabasite intercalations and represents a less deformed retro-wedge area. In the study area it was entirely overprinted at a uniform depth at 3 (cid:4) 0 (cid:2) 5 kbar with temperatures progressively rising from 400 (cid:1) C to 720 (cid:1) C towards the coeval Late Palaeozoic magmatic arc batholith. The interrelated pattern of PT data permits a conceptual reconstruction of the fossil convergent margin suggesting a flat subduction angle of (cid:3) 25 (cid:1) with continuous basal accretion at a depth of 25–40 km and a short main intrusion pulse in the magmatic arc. The latter was accompanied by the formation of a thermal dome in the retro-wedge area, which remained stable relative to the vertically growing accretionary prism characterized by cyclic mass flow.


INTRODUCTION
The basement of the Coastal Cordillera in central Chile between Pichilemu and Constituci o on (34 -35 30 0 S; Fig. 1) represents the first region on the South American active continental margin in which metamorphic zonation was studied (Gonz a alez Bonorino, 1971). This resulted in recognition of this area as a classic Pacific-rim type paired metamorphic belt (Aguirre et al., 1972;Ernst, 1975). Principles and concepts were recognized here that could be applied to most of the metamorphic basement along the Chilean Coastal Cordillera between 26 and 55 S (Hervé, 1988). This unusually long chain of basement exposures represents a series of fossil, deeply subducted accretionary prisms of Permo-Carboniferous age in the north and Mesozoic age in the south that are partly associated with magmatic arcs and hightemperature metamorphic belts of variable age (Hervé, 1988). The metamorphic complexes were not overprinted by later collisional processes, but were destroyed to variable extents by processes after the end of accretion during the continuing long-term activity at the convergent margin.
The type area was revisited because it exposes the most characteristic elements of the Chilean basement. Here we concentrate primarily on metamorphic processes and correlate these with concomitant deformation and magmatic events. Together with an associated geochronological study (Willner et al., 2005) this provides a basis for development of a more detailed conceptual dynamic model for this type of active continental margin. Questions addressed in detail are: What partial PT paths can Fig. 1. Geological map of the paired metamorphic belt within the basement of the Coastal Cordillera in north-central Chile (34 and 35 30 0 S) and its cover rocks. Information is included from Godoy (1970), Gonz a alez Bonorino (1971), Moraga (1981), Gana & Hervé (1983), Bravo Espinosa (2001 and the author's own observations. be deduced from the different lithologies present? What governs the metamorphic reaction history in the accretionary prism? Did peak pressures vary regionally and between rock types? Why is blueschist a very rare rock type in the high-pressure belt? How is metamorphism related to penetrative deformation? What is the nature of the metamorphic overprint during exhumation? What is the character of metamorphism in the concomitant high-temperature belt? Is it possible to reconstruct the fossil thermal structure of the paired metamorphic belt from the restricted information preserved within its rocks?

GEOLOGICAL SETTING AND FIELD RELATIONSHIPS
Traditionally the basement of the Coastal Cordillera has been subdivided into two metamorphic complexes (the Western and Eastern Series; Fig. 1), representing contrasting forearc environments. This association is a fundamental feature of the basement that can be observed consistently throughout the Coastal Cordillera despite variable ages of deposition, metamorphism and deformation. The concept was introduced by Aguirre et al. (1972) and summarized by Hervé (1988). The Western Series comprises low-grade metapsammopelitic rocks with a dominant transposition foliation and metabasite intercalations, whereas the Eastern Series lacks metabasites and is represented by a less deformed, very low grade metagreywacke-pelite sequence. Whereas the Western Series is regarded as an accretionary prism, the Eastern Series is considered to represent the retro-wedge area (Hervé, 1988;Willner et al., 2000). In central Chile the Eastern Series is partly intruded by calc-alkaline plutons of a late Palaeozoic arc with an associated low-pressurehigh-temperature metamorphic overprint.
In the Western Series ( Fig. 1) the predominant rocks are former turbiditic deposits characterized by a penetrative, mainly subhorizontal transposition foliation with pronounced banding. This represents a second, or locally a third, foliation with frequent intrafolial folding of relic bands, which mostly lacks kinematic indicators and represents ductile thinning. Quartz veins of decimetre thickness transposed parallel to the penetrative foliation are prominent, but deformed cross-cutting quartz veins and undeformed subvertical, quartz-filled tension gashes also exist. Younger subparallel shear bands with variable transport directions are rare. Stretching lineations are characteristically subparallel to the mesoscopic fold axes and mainly NW-SE-trending in the southern part of the area, but varying in the north. Frequently black, postkinematic, albite porphyroblasts are present, locally giving rise to spotted schists. Whereas the metapsammopelitic schists lack garnet, an exceptional garnet mica-schist occurs only in the area of Punta Sirena (Fig. 1). This rock is characterized by abundant porphyroblasts of garnet of 2-10 mm size, by a brighter colour caused by predominant white mica and by a coarser grain size. It forms several layers of 10 m thickness at two localities north and south of Punta Sirena.
Metabasite intercalations in the Western Series make up only 15-20% of the rock volume, forming lenses of metre to kilometre size. Whereas these are commonly greenschist, blueschist was observed as rare lenses of 1-5 m thickness at three localities ( Fig. 1: Infiernillo beach, Pichilemu; El Molino gorge, eastern Cahuil; a gorge NE of Iloca). Occasional green rims around these lenses are due to intensive retrograde growth of chlorite. In the greenschist lenses relic depositional features can be observed locally. At Infiernillo beach and at Punta Lobos ( Fig. 1) pillow structures of 20-50 cm diameter are preserved with radial fractures filled with calcite and amygdules towards the centre of the pillows. At Infiernillo beach relic pyroclastic structures also occur: lenticular clasts (1-10 cm) of massive dark greenschist with abundant amygdules float in a more foliated matrix richer in ferromagnesian minerals. The structure strongly resembles former hyaloclastite. Also, the presence of relatively abundant white mica-bearing metabasite may point to the presence of former tuffitic deposits. According to Godoy (1986), the chemical composition of the metabasites (particularly immobile trace elements) throughout the basement of the Coastal Cordillera resembles that of mid-ocean ridge basalts (MORB) or intraplate basalts. Zones of enhanced fluid flow are indicated by: (1) layers or irregular zones of centimetre to metre scale characterized by phase reduction (e.g. monomineralic zones of epidote or chlorite); (2) concentrations of white albite porphyroblasts; (3) veins filled with quartz, albite, locally calcite and amphibole. The structural inventory of the metabasites is similar to that of the metapsammopelitic schists. Mesoscopic folds of centimetre to metre scale are more prominent and amphibole is often oriented parallel to the regional stretching lineation.
Several minor rock types are associated with the metabasites: (1) rare serpentinite lenses of several tens of metres in extent; (2) local layers of marble, black graphite-rich metapelite and pure quartzite of centimetre to metre thickness (metachert; Hervé, 1988); (3) prominent intercalations of ferruginous metasediments of centimetre to metre thickness. These last rocks comprise mainly stilpnomelane-bearing schists and quartzites partly with garnet and/or concentrations of magnetite of economic value (e.g. at Punta Sirena; Fig. 1) as well as layers of massive sulphide of centimetres thickness. In south-central Chile such rocks also grade into Mnrich sediments (spessartine quartzites; 'coticules') which are regarded as pre-metamorphic Mn-and Fe-rich hydrothermal precipitates mixed with aluminous alteration-derived material at the surface of the oceanic crust . A similar origin is also possible for the ferruginous metasediments. The metabasites and their associated rock types appear to represent the upper part of segments of oceanic crust incorporated into the accretionary prism.
In the Eastern Series metabasic intercalations are absent and metagreywacke-pelite alternations prevail with occasional calcsilicate. Particularly in the central part of the exposed Eastern Series in the study area stratigraphic coherence of strata and well-preserved turbiditic sedimentary structures (cross-bedding, load casts, convolute bedding, graded bedding) are observed as well as slightly east-vergent folding of bedding by chevron folds up to 10 m wide. These rocks are overprinted by a flat west-dipping second foliation, which becomes a transposition foliation approaching the Western Series. Early formed quartz veins are frequent, but albite porphyroblasts are absent. In the study area, the Eastern Series is overprinted by a HT metamorphic event. The earlier stages of its tectono-thermal evolution under very low grade conditions can only be inferred by comparison with other areas in Chile, where the HT overprint is lacking (Hervé, 1988;Willner et al., 2000). Gonz a alez Bonorino (1971) mapped several prograde north-southtrending metamorphic zones with the metamorphic grade increasing towards the axis of the batholith, which intrudes the Eastern Series at its eastern flank. Incipient biotite growth coincides with the western boundary of the Eastern Series. In the north of the study area garnet and oligoclase appear shortly before the staurolite isograd, which delimits the following zone characterized by garnet, staurolite and andalusite porphyroblasts. Then sillimanite appears and the highest grade zone is characterized by a migmatitic garnetcordierite-sillimanite-K-feldspar gneiss. In the southern part of the study area staurolite does not appear and temperatures did not overstep the andalusite-sillimanite transition. The porphyroblasts grew postkinematically after the first and second deformation. However, local slight rotation of the porphyroblasts is observed, as well as occasional stretching of andalusite blasts and quartzfilled tension gashes parallel to the regional stretching lineation. This indicates that deformation continued with lesser intensity after the peak of the HT event within a stress field similar to that before this overprint.
At three localities (Pichilemu, eastern Punta Lobos, southern Boyeruca; Fig. 1) a north-south-striking semibrittle mélange-type shear zone occurs related to late-stage destruction of the accretionary prism. The boundary between the Eastern and Western Series in the north of the study area is a brittle reverse fault (Pichilemu-Vichuquén Fault; Fig. 1), which cuts the isograds in the Eastern Series, whereas in the south of the study area the boundary is transitional, as observed by Godoy (1970). The prominent fault is a further late deformation, which caused shortening of the accretionary prism.
Tonalite, granodiorite and granite dominate in the eastern part of the study area, forming part of the Southern Coastal Batholith (SCB) of Permo-Carboniferous age . Granite with magmatic muscovite is frequently observed, but granitoids also occur containing hornblende and titanite. S-type granitoids seem to be abundant in the SCB consistent with their high 87 Sr/ 86 Sr ratios . Lucassen et al. (2004) showed that isotope ratios of Nd and Pb are similar to those of the Palaeozoic metasediments, indicating a magmatic arc with a high crustal component. The Western Series are intruded by three small isolated bodies of biotite granite ( Fig. 1; from north to south the plutons of Pichilemu, Los Ciruelos and Constituci o on). Scattered, local, posttectonic basalt dykes of decimetre to metre thickness and a few rhyolitic dykes occur throughout the area. The Eastern Series and the batholith are unconformably overlain by Late Triassic to Early Cretaceous marine siliciclastic sediments and volcanic rocks.

PETROGRAPHIC CHARACTERISTICS OF THE WESTERN SERIES Rock fabric Metabasites
The mineral assemblage of the greenschists is amphibole-chlorite-epidote-albite-quartz AE titanite AE magnetite AE white mica AE calcite. Amphibole, chlorite and white mica (0Á05-0Á2 mm) are oriented parallel to the penetrative foliation, but cross-cutting grains are frequent. The recrystallized amphibole is always euhedral, forms up to 2 mm long needles and is strongly zoned, displaying bluish cores grading into green rims. Faint internal crenulation with recrystallized hinge zones can be detected within the dominant foliation. Epidote occurs as euhedral, optically zoned crystals of 0Á1 mm size crosscutting the fabric. Epidote and chlorite can continuously replace the existing assemblage until monomineralic layers are formed. Titanite forms small pods or trails of tiny anhedral grains (0Á01-0Á04 mm) parallel to the foliation with some relic crenulation hinges or larger euhedral recrystallized grains (0Á1 mm). Quartz, albite and/or calcite form small polygonal aggregates or cross-cutting veinlets including all minerals of the matrix assemblage. Occasional anhedral albite porphyroblasts (0Á1-0Á5 mm) with internal trails of epidote and amphibole have grown after formation of the predominant foliation and across relic crenulation hinges. They may be rotated in rare sheared rocks. Opaque phases are pyrite or magnetite which grew as large, euhedral, recrystallized grains (0Á5-1 mm). Clinopyroxene (0Á1-0Á5 mm) is a ubiquitous relic of the protolith assemblage. It often has irregular grain boundaries as a result of replacement by surrounding minerals. In some cases, large clinopyroxene crystals still display their original euhedral outline as former phenocrysts. In rare sheared rocks the mineral shows brittle deformation and rotation. Further relic fabric are occasional amygdales (1-5 mm size) filled with albite and/or calcite. The amygdales are slightly flattened in the more strongly deformed areas.
The mineral assemblage of the rare blueschists is blue amphibole-chlorite-epidote-albite-quartz AE white mica AE titanite AE magnetite AE calcite. Banding at millimetre to centimetre scale is represented by dark bands of weakly oriented euhedral amphibole, chlorite, epidote and white mica (0Á05-0Á2 mm), alternating with bright bimineralic bands (amphibole-quartz, amphiboleepidote, amphibole-chlorite) or monomineralic strings (amphibole, chlorite, titanite, white mica or epidote). Crenulation of a relic foliation can also be observed within the bands, with oriented minerals recrystallizing in the crenulation hinges. Epidote and amphibole are optically zoned. Green amphibole overgrows blue amphibole along the rims. One sample (12544) contains relic clinopyroxene (0Á5 mm). Unoriented euhedral albite crystals of similar size occur near the clinopyroxene crystals, suggesting a further magmatic relic. Quartzalbite veinlets with some blue amphibole occur parallel to the bands or cut across.
At four localities serpentinite lenses of 10 m scale are associated with the greenschist. Clinopyroxene occurs as the only relic phase forming a network of mainly 0Á5 mm crystals, which surround other, entirely replaced phases with partly euhedral outline. Replacement minerals are mainly antigorite, minor tremolite and chlorite with exsolved magnetite. The original fabric resembles that of an ultramafic igneous cumulate. Godoy & Kato (1990) also decribed pyroxene relics and abundant layered magnetite concentrations in serpentinite from south-central Chile pointing to a similar origin.

Ferruginous metasediments
The three recognized types of iron-rich metasedimentsstilpnomelane quartzite, stilpnomelane schist and magnetite-stilpnomelane rocks-can grade into each other and into the associated greenschist. The typical mineral assemblage is magnetite-stilpnomelaneamphibole-garnet-quartz-albite AE white mica AE chlorite AE epidote.

Metapsammopelitic schist
The typical mineral assemblage of the monotonous metapsammopeltic schist is quartz-albite-white micachlorite-ilmenite AE magnetite AE epidote. The heavy mineral assemblage is characterized by zircon, apatite and tourmaline. There is prominent banding of alternating quartz-and phyllosilicate-rich bands of millimetre thickness. Quartz and albite (0Á05-0Á30 mm) form a polygonal fabric without relics of former detrital or oriented grains, but with local subgrain formation and sutured grain boundaries indicating late continuous deformation. White mica and chlorite (0Á1-0Á3 mm) are intensively intergrown showing a relic orientation. Crenulation hinges of various generations (F 2 , F 3 ) are prominent, but the phyllosilicates are recrystallized in the hinges with frequent growth of cross-cutting mica. Albite porphyroblasts (0Á5-2 mm) are a late, mostly unoriented phase and an intrinsic feature of the metapsammopelitic schist, overgrowing fold hinges of all generations (F 2 , F 3 ). They are often macroscopically black as a result of internal inclusion trails of graphite, which trace relic crenulation hinges. The porphyroblasts are bound to the phyllosilicate-rich bands, growing at the expense of white mica. In some cases they can completely replace the white mica, forming bands of albite. The porphyroblasts are euhedral or partly anhedral as a result of incomplete development of the crystals or late pressure solution at the rims. Apart from this feature, local slight rotation of the porphyroblasts also indicates continuing weak deformation after the growth of the porphyroblasts.
The assemblage of the unusual garnet mica-schist at Punta Sirena is garnet-quartz-albite-white micachlorite-epidote-titanite AE ilmenite AE rutile. Garnet porphyroblasts range from 1 to 10 mm size with internal sigmoidal trails of titanite, ilmenite or quartz (0Á01-0Á05 mm). Near the rims the garnet overgrows a polygonal fabric of coarser quartz (0Á05-0Á3 mm), similar to that of the surrounding matrix. The grains are euhedral or partly replaced at the rims by white mica and chlorite; in some samples they are also replaced along cracks by chlorite and epidote. Dominant white mica and minor chlorite (0Á2-0Á5 mm) form two foliations within a matrix of polygonal quartz and albite. The phyllosilicates recrystallize in crenulation hinges and cross-cutting grains are abundant. An early white mica occurs as inclusions in garnet and titanite. Subhedral grains of unoriented epidote (0Á05-0Á10 mm) are abundant in the foliation planes. Titanite forms euhedral, unoriented crystals of 0Á1-0Á5 mm size in the matrix, occasionally enclosing round rutile. Albite forms prominent, unoriented porphyroblasts (0Á2-0Á5 mm) enclosing trails of graphite, epidote, white mica, titanite or garnet. Some garnet mica-schist samples show a prominent orientation of the phyllosilicates parallel to the prevailing foliation. In these porphyroblasts of garnet, albite and titanite are strongly rotated, indicating a late, localized, non-coaxial deformation.

Mineral chemistry
Mineral compositions were determined using a Cameca SX 50 electron microprobe at Ruhr-Universit€ a at Bochum, Germany. Operating conditions were an acceleration voltage of 15 kV, a beam current of 15 nA, 20 s counting time per element on the peak and on the background and a defocused beam of 8 mm diameter to avoid loss of alkalis in micas, feldspars and amphiboles. Standards used were synthetic pyrope (Si, Al, Mg), rutile (Ti), glass of andradite composition (Ca, Fe), jadeite (Na), K-bearing glass (K), topaz (F), Ba-silicate glass (Ba, La). The PAP procedure was used for matrix correction. Representative analyses and structural formulae of minerals used for PT calculations, together with the calculation procedure of the structural formulae, are presented in Table 1. Further data are available as supplementary data tables which may be downloaded from http://www.petrology. oupjournals.org or upon request to the author. Element distribution maps were simultaneously produced for three elements by stepwise scanning over rectangular areas. Abbreviations for minerals and mineral components used throughout the text follow Kretz (1983), if not indicated otherwise. Whole-rock analyses were performed at Ruhr-Universit€ a at Bochum by XRF except Fe 2þ and H 2 O (standard wet chemical methods).

Garnet
Garnet in the Western Series is restricted to the unusual garnet mica-schist and the ferruginous metasediments. The garnet mica-schist contains a grossular-rich garnet with the compositional range almandine 0Á47-0Á76 , grossular 0Á14-0Á34 , spessartine 0Á01-0Á21 , pyrope 0Á02-0Á09 (X Mg 0Á02-0Á13, Ti 0Á04; Table 1). Zoning is typically prograde and bell-shaped with an increase in Ca and Mg and a decrease in Mn, Fe 2þ , Fe 3þ and Ti from core to rim. Zonation of Ca is distinctly oscillatory.
In the ferruginous metasediments, the garnet is Mn-and Ca-rich with the compositional range almandine 0Á14-0Á47 , spessartine 0Á27-0Á56 , grossular 0Á18-0Á26 , pyrope 0Á01-0Á03 , uvarovite 0Á06-0Á07 , andradite 0Á01-0Á04 (X Mg 0Á06-0Á12, Ti 0Á04 a.p.f.u.). These compositions are rather similar to that of garnet in the spessartine quartzite (coticule) in other parts of the basement, which have a premetamorphic hydrothermal origin . Zonation is prograde and bell-shaped with an increase in Ca, X Mg , Mg and Fe 2þ and a decrease in Mn and Fe 3þ from core to rim.
In the greenschist and the ferruginous metasediments, amphibole mostly grades from NaCa-amphibole to Caamphibole or is Ca-amphibole with a high Na B content ( Fig. 3c; Table 1). This variation also corresponds to high Na B in the core decreasing towards the rims. The           Cations based on 56 valencies; F and Cl are at the detection limit.
NaCa-amphibole (Na B 0Á50-0Á88 a.p.f.u., Na A 0Á00-0Á31, X Mg 0Á40-0Á82, X Fe 3þ 0Á60-0Á97) includes winchite (Si 7Á50-7Á93 a.p.f.u.) and barroisite (Si 6Á64-7Á48 a.p.f.u.). Barroisite is partly ferribarroisite (Fe 3þ 1Á23-2Á00 a.p.f.u.) in the ferruginous metasediments. The Caamphibole (Na B 0Á02-0Á49 a.p.f.u., Na A 0Á00-0Á39, X Mg 0Á58-0Á86, X Fe 3þ 0Á30-1Á00) ranges gradually from actinolite (Si 7Á58-7Á93 a.p.f.u.) to magnesiohornblende (Si 7Á00-7Á48 a.p.f.u.). It is notable that, at a given Na B content, the total R 3þ content in the amphiboles of the greenschist is considerably higher than in those of the blueschist (Fig. 3b and c; except sample M3404). This may be due to a higher Tschermak substitution in the amphiboles of the greenschists leading in part to barroisite and magnesiohornblende compositions. The overall compositional variation of amphibole during continuous grain growth, as well as between the peak metamorphic compositions of different blueschist and greenschist samples, shows complete transitions between Ca-and Na-amphibole, suggesting that no miscibility gap exists between Na-and Ca-amphiboles at the given conditions and compositions. Amphibole compositions can be plotted in terms of 'actinolite, glaucophane and riebeckite components' (Fig. 5a and b) showing complete solid-solution between Fe-rich Ca-and Na-amphiboles. The remaining possible solid-solution gap between Mg-rich actinolite and glaucophane must be smaller than that calculated by Massonne (1995aMassonne ( , 1995b) at 300 C, indicating amphibole growth at T > 300 C.

White mica
White mica of phengite composition occurs in all rock types (Table 1). Si contents are highest in the blueschist (3Á33-3Á53 a.p.f.u.) with a variation of 0Á10-0Á15 a.p.f.u. in single samples, whereas the range is wider in the greenschist (3Á14-3Á5 a.p.f.u.) with mostly lower maximum contents and a similar range in individual samples (Fig. 6). Si contents are still lower in the metapsammopelites (3Á10-3Á30 a.p.f.u.), but also in the garnet mica-schist (3Á2-3Á36 a.p.f.u.). Ti and Na contents are very low in all rock types (<0Á05 a.p.f.u.). Most compositions plot below the ideal Tschermak-substitution line in Fig. 6 owing to partial substitution of Al by Fe 3þ and some di/trioctahedral substitution. Fe 3þ contents were estimated by normalizing the sum of cations on the octahedral site to 2Á05 a.p.f.u. (see Massonne, 1995aMassonne, , 1995b. This is due to a restriction of the di/trioctahedral substitution experimentally detected by Massonne & Schreyer (1986) for white mica with variable Si contents. Calculated Fe 3þ contents are highest in the magnetite-rich ferruginous metasediments (0Á17-0Á36 a.p.f.u.) and in the metabasites (<0Á32 a.p.f.u.), which also contain Fe 3þ -rich amphibole. Fig. 2. MnO-TiO 2 -Na 2 O variation diagram (wt %) for magmatic clinopyroxene in metabasite and its compositional range in reference rock types (Nisbet & Pearce, 1977).
No Fe 3þ was estimated in the white mica of the metapsammopelites. In each metabasite sample there is a strong negative correlation of Si with Fe 3þ that seems to be enriched in the Si-poor rims of phengite grains.
Titanite is a prominent accessory phase in the metabasites and in the garnet mica-schist with a Ca(Al,Fe 3þ )SiO 4 (F,OH)-component between 4 and 52 mol %. Notable contents of F (0Á02-0Á59 wt %), Al (0Á03-0Á46 a.p.f.u.) and Fe 3þ (0Á01-0Á22 a.p.f.u.) are observed. The Fe 3þ content of epidote varies widely in different samples (0Á44-0Á99 a.p.f.u.), but generally an increase is observed from core to rim.

PETROGRAPHIC CHARACTERISTICS OF THE EASTERN SERIES
Apart from very rare calcsilicate rocks, the Eastern Series are lithologically extremely homogeneous and mineral assemblages, fabric and mineral chemistry change in response to the zonation of the high-temperature metamorphic overprint.
A staurolite-andalusite zone is only observed in the north of the study area. Two main assemblages are: garnet-biotite-muscovite-plagioclase-quartz AE staurolite AE ilmenite and andalusite-biotite-muscoviteplagioclase-quartz AE staurolite AE ilmenite. Although porphyroblasts of garnet, biotite, staurolite and andalusite grew post-kinematically with respect to the penetrative foliation, slight rotation is observed locally, indicating continuing deformation with waning intensity after the peak of HT metamorphism. Staurolite porphyroblasts (1-2 mm) are euhedral with tiny inclusions of quartz and biotite. At the rims slight replacement by muscovite, chlorite and ilmenite is observed. Small euhedral garnet porphyroblasts (0Á1-0Á3 mm) are nearly devoid of inclusions. The size of the prominent andalusite porphyroblasts ranges from 0Á1 cm to several centimetres. Frequently, partial replacement by sericite and chlorite occurs, indicating very low temperature alteration. Also, quartz-rich calcsilicate rocks are locally observed containing the assemblage garnet-clinoproxene-quartzplagioclase-titanite.
In the south of the study area medium-grade conditions are represented by an andalusite-sillimanite zone as the highest grade without appearance of staurolite. However, some poikilitic cordierite in the matrix has been described by Gana & Hervé (1983). Andalusite porphyroblasts are only of 1-2 mm size, but locally abundant. In the eastern part of the zone fibrolite appears replacing andalusite at the rims.

METAMORPHIC EVOLUTION OF THE WESTERN SERIES Phase relationships and reaction history
To visualize the approximate PT stability fields of the high variance blueschist-and greenschist-facies assemblages, pseudosections were calculated in the system K 2 O-Na 2 O-CaO-TiO 2 -Fe 2 O 3 -FeO-MgO-Al 2 O 3 -SiO 2 -H 2 O from the whole-rock composition of four representative white mica-bearing samples of all major rock types ( Fig. 7; Table 2). For calculating the equilibrium assemblages and respective mineral compositions,  Table 3. Abbreviations not following Kretz (1983) are: Kwm, K-white mica; Nam, Na-amphibole; Cam, Ca-amphibole; V, vapour.
the Gibbs free energy minimization procedure was applied using the DEKAP code developed by Gerya et al. (2001). This approach is based on an algorithm suggested by de Capitani & Brown (1987). The calculation of the petrogenetic grid was performed with a resolution of 5 K and 100 bar for T and P, respectively. Calculations involved the entire thermodynamic data set for minerals and aqueous fluids of Holland & Powell (1998a). References to the mixing models used, consistent with this dataset, are listed in Table 3. In the two calculated pseudosections of the blueschist and greenschist samples, which have no marked bulkrock chemical differences, a narrow transitional field, of similar size, with coexisting Ca-and Na-amphiboles, is predicted between the blueschist and greenschist assemblages between 300 C, $5-7 kbar and 400 C, 6-8Á5 kbar ( Fig. 7a and b). The predicted coexistence of two amphiboles contrasts with the observation made above that a complete compositional transition exists between Na-and Ca-amphiboles within the studied samples. The transition between the facies stability fields is actually represented by the NaCa-amphiboles winchite and barroisite, which are common in all metabasites. Hence the predicted coexistence of two amphiboles in the pseudosections must be due to the activity models used for amphibole, which imply a too wide miscibility gap. Nevertheless, the minimum pressure for blueschist assemblages at 7Á8-8Á8 kbar, 300-400 C is equivalent in both pseudosections. This predicts that there is a pressure difference between the recorded peak assemblages of the blueschist and greenschist samples. Lawsonite is not observed in our samples, but appears at pressures above 9-11 kbar at 300-350 C. This can be taken as a lower temperature limit for the studied epidote blueschist-facies assemblages. At the highest temperature limit, a transitional field to the albite amphibolite facies may already appear at 430 C. In the greenschist assemblages biotite would be stable at T > 400 C and P < 4-5 kbar.
A typical pseudosection for the metapsammopelites (Fig. 7c) shows that their common assemblage white mica-chlorite-quartz-albite AE epidote is stable over a very wide PT field including greenschist, epidote blueschist and albite-epidote amphibolite facies. Lawsonite is predicted already at 9-11 kbar and 300-350 C, representing a good lower temperature limit. Garnet in the Western Series is restricted only to very Mn-rich assemblages, such as the ferruginous metasediments, and it is thus stabilized to low temperature by high Mn contents. An exception is the Ca-rich garnet mica-schist of Punta Sirena, where garnet is predicted to be stable above 10-11 kbar. However, in the absence of omphacite, temperatures should have exceeded $450-500 C (Fig. 7d). The calculated composition of the highpressure garnet (e.g. at 11 kbar, 550 C: almandine 0Á661 , grossular 0Á241 , pyrope 0Á098 ) corresponds well to the measured one, as noted above.
Four localities of ferruginous metasediments (associated with blueschist and greenschist) contain the assemblage stilpnomelane-white mica (Fig. 1), proving that temperatures did not exceed stilpnomelane breakdown to biotite coexisting with phengite and quartz (Massonne & Szpurka 1997; here calculated for mean compositions; method I, Table 3) at $350-400 C, >5 kbar (Fig. 8a). On the other hand, thorough recrystallization of quartz within the pentratively deformed rocks, lacking any visible distinction between clastic and recrystallized grains in the metapsammopelites, indicates minimum temperatures above 350 C (Brix et al., 2002). The pumpellyite breakdown reaction marking the boundary between pumpellyite-actinolite and greenschist facies (Evans, 1990; here calculated for mean compositions; method I, Table 3) at 300-350 C, >5 kbar (Fig. 8b), was well overstepped in the entire study area. Also, retrograde pumpellyite did not form, indicating that retrograde metamorphic reactions appear to have ceased before cooling through 300 C. Hence the evolution of most rocks of the study area was apparently restricted to a rather narrow temperature range. Maximum pressure is limited by the presence of pure albite in all rock types to below 10Á5-12Á5 kbar at 300-400 C.

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JOURNAL OF PETROLOGY VOLUME 46 NUMBER 9 SEPTEMBER 2005 fluid influx is necessary for retrograde reaction progress, considering the common assumption that water released during prograde dehydration left the system. Pressuresensitive multivariant reactions such as reaction (E6) (see Table 4) at the blueschist-greenschist-facies transition, that are used for geobarometry below, have water partly as a reactant on the high-pressure side, but also on the low-pressure side [see reaction (5), Table 4]. This means that water can be consumed or released during continuous retrograde decompression reactions. The calculated pseudosections allow quantification of the change in the amount of free water relative to the bulk water content of the system with changing PT conditions (Fig. 9), assuming that reactions are instantaneous and complete, and the water content of the rock was the total water content of the system. Considering PT changes from 400 C, 8-10 kbar to 350 C, 5 kbar (simulating the partial PT path derived above) the changes in X free water /X bulk water are negative for greenschist sample 95CH24 (consumption of free water), but positive for blueschist sample 95CH11 and the metapsammopelitic sample 98CH32 (release of free water). This predicts that with continuous reaction during decompression at low-grade conditions (either isothermally or with slight cooling), the amount of free water might increase in many cases, such that no external water is required for reactions to proceed. A limited amount of steadily available free water will favour localized equilibrium over short distances during continuous mineral growth with activities of elements in the fluid always buffered.

Geothermobarometry
For quantification of the PT conditions for equilibration stages along the PT path, local equilibria with multivariant reactions were calculated using mineral compositions of phases in close contact. Multivariant equilibria calculations were undertaken mainly using the Ge0calc software of Brown et al. (1989) and derivations (TWQ) with the thermodynamic dataset of Berman (1988) supplemented by further compatible data and activity models (Table 3). A list of the calculated reactions is given in Table 4. Results are plotted in Fig. 8.

Metabasite
Because of the high number of reliable components available for calculations, good geothermobarometric results were obtained for the low-variance assemblage amphibole-white mica-chlorite-epidote-quartz-albite. Invariant points were calculated using the waterindependent multivariant reactions (E1)-(E4) ( Table 3).
Including water as a further phase, nine additional reactions were calculated. However, these relatively flat water-dependent reactions are not only sensitive to minor changes in (unknown) water activity, but also are much more dependent on the activity of the clinozoisite component than the water-independent ones. Thus their use as a further check for equilibrium conditions is limited, although closest coincidence of all possible invariant points was always approached. For blueschist samples lacking chlorite, the water-dependent reaction (E5) was used as a barometer; for greenschist lacking white mica, the water-dependent reaction (E6) was calculated.
The two generations of amphibole in the two different metabasite rock types reflect two stages of equilibration along a partial PT path, a peak metamorphic stage I and a retrograde stage II. Calculations of the stage I conditions yield a range of PT results (invariant points) of 9Á5-10Á7 kbar, 350-385 C for the blueschist and 7Á0-9Á3 kbar, 380-420 C for the greenschist (Fig. 8). The temperature range for the latter was independently corroborated by conventional Fe-Mg exchange thermometry with rims of garnet-amphibole pairs (Graham & Powell, 1984) in two magnetite-stilpnomelane rocks (samples 95CH25 and 98CH25). The scatter presumably represents continuous equilibration around peak PT conditions during the late prograde and early retrograde PT path, which could not be resolved in detail in the present case, but also differences in peak pressure between greenschist samples are likely. Calculations of the stage II conditions yielded a range of PT results of 6Á0-7Á7 kbar, 290-345 C for the blueschist and 4Á4-7Á2 kbar, 315-380 C for the greenschist (Fig. 8), thus indicating pressure release with slight cooling. The slight temperature difference between the paths of the blueschist and greenschist presumably concurs with a generally higher Tschermaks substitution in the amphiboles of the greenschist (Fig. 3c).
There is no regional trend in the distribution of peak pressures (Fig. 1), but there is a significant peak pressure difference between the two metabasite types as predicted from the pseudosections. It is often argued that in the Chilean basement the very rare blueschist assemblages are the principal relics of HP-HT conditions generally completely erased by a pervasive retrograde greenschist overprint (e.g. Kato, 1985;Martin et al., 1999). Here peak PT compositions of solid-solution phases are regarded as preserved in most rock types for the following reasons: (1) relic magmatic clinopyroxene phenocrysts are replaced by Na-, CaNa-or Ca-amphibole in different rock types. It seems unlikely that a premetamorphic phase is preserved but not the peak metamorphic amphibole.
(2) A pervasive overprint, erasing all relic compositions, could be driven by influx of abundant external fluid; however, this should lead to phase reduction. Such metasomatic effects are frequently observed, but not predominant in the metabasite lenses, where low-variance assemblages are also common. It was shown above that major external fluid infiltration is unlikely for most of the studied rocks.

Metapsammopelite
For the high-variance assemblage present in most of the metapsammopelitic rocks, thus far only the approach of Vidal & Parra (2000) and Parra et al. (2002aParra et al. ( , 2002b, using coexisting chlorite-phengite equilibria, has been shown to yield consistent results, especially for metapelites in similar HP-LT terranes. This approach (method 2; Table 3) is based on thermodynamic solution models involving the Tschermak and pyrophyllitic substitutions in white mica and the di/trioctahedral substitution in chlorite. Application of this approach to the metapsammopelitic rocks of the study area is, however, restricted only to the water-independent multivariant equilibria (E7)-(E9) and (E3). All analysed iron is assumed to be ferrous in this approach. Other possible end-members with contents in chlorite and mica of less than 5% (e.g. sudoite, pyrophyllite) could not be considered because of the high uncertainty of their activity in these phases. For two metapsammopelitic schist samples calculated ranges of conditions of local equilibria of 4-9Á6 kbar, 355-435 C suggest similar peak PT conditions and decompressional overprint to those in the greenschists. Hence a comparable PT evolution path for both rock types is inferred (Fig. 8b and c).

METAMORPHIC EVOLUTION OF THE EASTERN SERIES
The interpretation of the HT metamorphic sequence and phase relationships in the Eastern Series is straightforward (Fig. 10). The zonation and sequence of mapped assemblages indicate progressive increase in grade from upper greenschist facies to granulite facies, suggesting a classic 'Abakuma-type' sequence at pressures below the aluminosilicate triple point. The sequence starts with the formation of biotite, passes the staurolite-in reaction in the andalusite stability field and the staurolite-quartzmuscovite-out reaction in the sillimanite stability field, and ends with the first anatectic melts. Breakdown of muscovite þ quartz in the sillimanite field before reaching the wet granite solidus indicates a pressure below 3Á6 kbar (intersection of the muscovite þ quartz breakdown and wet granite solidus curves). This is consistent with the position of the univariant reaction Bt þ Sil þ Qtz ¼ Grt þ Cord þ Kfs þ H 2 O of the KFMASH system (Spear & Cheney 1989), which is recorded by the highest grade assemblage. Geothermobarometry is consistent with predictions from the petrogenetic net (Fig. 10). All calculations were carried out using method 1 (Table 3) with multivariant reactions (E10)-(E20) listed in Table 4. In the biotite zone, the temperature can be approximated calculating reaction (E10) (curve 3a in Fig. 10) and the minimum pressure with reaction (E11) (curve 3b in Fig. 10) involving a theoretical K-feldspar. For mica-schist 01CH29 approximate conditions of 2-3 kbar, 400-450 C result. PT conditions in the medium-grade rocks can be estimated in two ways. (1) Overstepping the staurolite-in reaction conditions in the andalusite stability field requires $520-580 C, 2Á5-3 kbar around the isopleth X Fe ¼ 0Á9 for garnet coexisting with staurolite, biotite, muscovite and quartz (Spear & Cheney 1989; curve 4 in Fig. 10).
Evaluation of the highest grade conditions are as follows: (1) Fe-Mg exchange thermometry for cordieritebiotite pairs (Bhattacharya et al., 1988) in sample 01CH48 results in 684-716 C (point 8 in Fig. 10), and the isopleth X Fe ¼ 0Á85 for garnet coexisting with cordierite, biotite, K-feldspar and quartz occurs at 650 C (curve 7 in Fig. 10). The position of the univariant reaction Bt þ Sil þ Qtz ¼ Grt þ Cord þ Kfs þ H 2 O in this temperature range indicates a minimum of 2Á5-3Á2 kbar.
The intrusion depth of the neighbouring granite (98CH43) was approximated using the zoned magmatic muscovite coexisting with biotite and K-feldspar. Intersection of reaction (E11) with the wet granite solidus is at 3Á6 kbar for an Si content of 3Á08 a.p.f.u. in white mica cores (curve 9a in Fig. 10) and at 2Á8 kbar for Si 3Á04 a.p.f.u. in the white mica rims (curve 9b). The quartzmuscovite breakdown curve is considerably lowered for Si 3Á08 a.p.f.u. (curve 2b in Fig. 10). Hence most muscovite presumably crystallized near the granite solidus just on the low-temperature side of the muscovite þ quartz breakdown curve.

DISCUSSION AND GEODYNAMIC CONSTRAINTS
The petrological information derived in this study from the paired metamorphic belt can contribute to a tentative reconstruction of the approximate thermal structure of the former continental margin and its geometric constraints. The resulting conceptual model is presented in Fig. 11.

The evolution of the accretionary prism
The protoliths of the metabasites and metapsammopelites in the Western Series are of very different origin; that is, from the uppermost part of the subducting oceanic plate and predominantly from the overriding continental plate (terrigeneous trench filling), respectively.  Spear & Cheney (1989). Numbered curves are as follows: 1, Johannes (1984); 2a, calculated for pure phases; 2b, calculated for muscovite with Si 3Á06 a.p.f.u.; 3a, 3b, reactions (E10) and (E11), respectively, calculated for compositions in sample 01CH29; 4, X Fe ¼ 0Á9 in garnet coexisting with staurolite, biotite, quartz and muscovite (Spear & Cheney 1989); 5, calculated invariant point [reactions (E12)-(E14) in Table 4] for the assemblage garnet-muscovite-biotite-quartz in sample 01CH43; 6, calculated invariant point [reactions (E12), (E15)-(E20); Table 4] for the assemblage garnet-cordierite-biotite-sillimanite-plagioclase-K-feldspar-quartz in sample 01CH48; 7, X Fe ¼ 0Á85 in garnet in assemblage with cordierite, biotite, quartz and K-feldspar (Spear & Cheney 1989); 8a, 8b, Fe-Mg exchange thermometer for garnet-cordierite in sample 01CH43; 9a, calculated Si 3Á08 a.p.f.u. isopleth, and 9b, Si 3Á04 a.p.f.u. isopleth for muscovite coexisting with biotite, K-feldspar and quartz [reaction (E11) in Table 4]. Measured mineral compositions are plotted in the inset AFM projections. Nevertheless, it can be shown that their metamorphic evolution, their deformational history and their metamorphic ages (Willner et al., 2005) are similar, which indicates a joint evolution from the earliest detectable stage. Their mixture could have occurred during subduction and early basal accretion. Analogue modelling by Gutscher et al. (1998) has demonstrated that effective subduction of long, thick sheets of sediments is possible with high basal friction during low-angle subduction involving steep erosional frontal slopes. As shown above, the oceanic crust incorporated into the Western Series may also have included alkali basalts. Thus a decrease of the subduction angle (or even resistance to subduction) might have been caused by the presence of oceanic islands on the subducting slab.
Peak PT conditions of the greenschists (7Á0-9Á3 kbar, 380-420 C) indicate metamorphism under a metamorphic gradient of 11-16 C/km (on the basis of an average density of 2Á8 g/cm 3 ), which appears relatively high for a subduction environment. However, this gradient seems to be typical for the Western Series as it was also detected in south-central and southern Chile (Willner et al., 2000. The elevated metamorphic gradient may be due to several factors. Numerical modelling by Peacock (1996) predicts that (1) slow subduction and (2) a relatively flat subducting slab may enhance the thermal gradient. (3) The subduction of upper crustal material (greywackes) with high contents of radiogenic elements also contributes to the heat production at depth. A further factor (4) is envisaged here: analogue modelling has recently shown that basal accretion during flat subduction may involve formation of long, flat duplexes forming an antiformal stack (Kukowski et al., 2002). This is tentatively included in the conceptual model (Fig. 11). Such a process predicts that part of the accreted material will initially move horizontally away from the lower plate before vertical exhumation and thus cross isotherms towards higher temperatures at maximum depth. A near-isobaric, late, prograde PT path (particle path 1 in Fig. 11) can be expected, although it could not be deduced for the studied rocks. However, a late prograde heating with little pressure variation is known from albite amphibolite grade rocks of comparable settings (Chonos Archipelago-Chile: Willner et al., 2000;South Shetland Islands: Trouw et al., 1998). A pervasive subhorizontal foliation (s 2 , locally s 3 ) mainly originated during peak PT conditions, reflecting basal accretion and crustal thinning at depth following basal accretion.
The occurrence of glaucophane-bearing blueschist must be considered as extremely rare, because only three localities are known along the $1500 km of basement exposure of the Coastal Cordillera (Willner et al.,Fig. 11. Conceptual model of the convergent margin of central Chile during late Palaeozoic times. Grey lines in the figure and the depthtemperature inset (summary of Figs 8 and 10) indicate tentative particle and depth-temperature paths in the Western Series of: 1, greenschist; 2, blueschist; 3, garnet mica-schist; line 4 represents the level of isobaric heating and cooling in the Eastern Series. Black dashed lines are isotherms.
2004a, 2004b) implying a special preservation mode. This rock was metamorphosed to significantly different peak PT conditions at 9Á5-10Á7 kbar, 350-385 C, corresponding to a lower metamorphic gradient ( $9-11 C/km) than in the predominant greenschist. There is no difference in peak PT ages of both neighbouring metabasite types (Willner et al., 2005). This appears problematic, because a higher peak temperature would be expected for the blueschists compared with the greenschists if they were metamorphosed along a gradient parallel to the subducting slab (Fig. 11). More common metabasites, which were subducted to similar depths as the blueschists in other areas of the Western Series, are metamorphosed to albite-epidote-amphibolite facies (Kato, 1985;Trouw et al., 1998;Willner et al., 2000Willner et al., , 2004a, showing comparable metamorphic gradients to the greenschists. Here it is suggested that the blueschists were derived from the lowermost part of the basal accretion zone of the accretionary wedge, near the uppermost tip of the mantle wedge ( Fig. 11; particle path 2), and that they conserved the original thermal gradient along the subducting slab (see Fig. 11), as was also implied by Trouw et al. (1998) and Willner et al. (2004aWillner et al. ( , 2004b for similar settings containing blueschists. However, the blueschists were not heated during exhumation. It is suggested that they were emplaced by local low-angle thrusting at depth onto the already isobarically heated greenschists. The second 'exotic' rock type is the unusual garnet mica-schist at Punta Sirena that yielded the highest PT conditions in the entire study area (390-440 C, 9Á6-14Á7 kbar), which were shown to reflect a retrograde stage after presumable isobaric cooling from a still higher peak temperature (particle path 3 in Fig. 11). The ages for this stage are the oldest recorded in the study area (Willner et al., 2005). A geodynamic interpretation can be provided by analogy to a better constrained occurrence in south-central Chile (Willner et al., 2004b), to similar findings in comparable settings worldwide (e.g. Wakabayashi, 1990), and to numerical modelling (Gerya et al., 2003). Siliciclastic material was subducted at the earliest stage of accretion to the deepest level under the mantle wedge and heated in contact with a still hot mantle. Later accreted material at this site caused hydration and cooling of the earliest accreted material and the overlying mantle. After this change (also of rheological conditions in the mantle), effective exhumation of the early subducted material followed at the base of the hydrated mantle wedge within a cooler environment than during its burial. The exotic garnet mica-schist thus provides an important relic and time marker for the onset of subduction mass flow in the Coastal Cordillera accretionary prism. It must be noted that its predominant retrograde equilibration occurred under the same metamorphic gradient as the blueschist, presumably in a position near the subducting slab (Fig. 11).
In all rock types of the Western Series a similar type of partial exhumation path, involving slight cooling with decompression, is preserved that is also similar to those of other HP-LT belts worldwide (e.g. Vidal & Parra, 2000, and references therein). It involves decompression with only slight cooling after peak metamorphic conditions recorded by the formation of retrograde local equilibria in the presence of free water and crystallization-recrystallization processes. The retrograde overprint occurred within a narrow temperature range of 300-400 C. Continuous reactions during pressure release of $3-4 kbar caused further crystal growth at the rims, as well as recrystallization, recording a clockwise decompression path. Further reaction to below 300 C is probably hampered for kinetic reasons. The geometry of the retrograde PT path implies a kink after cooling through 350 C at $4 kbar to cooling below 300 C at $2-3 kbar (Fig. 8). Late exhumation thus occurred under a high geothermal gradient, implying a 'doming' of isotherms above the accretionary prism (Fig. 11). Retrograde mineral growth and recrystallization generally occurred under strain-free conditions. Retrograde ductile deformation is restricted to rare local shear bands, indicating that there is little tectonic control of the exhumation process.

The high-temperature belt
The spatial field relationships of isograd surfaces dipping to the west and following the north-south trend of the batholith along strike indicate a close relation to a major heat input during the intrusion of the arc batholith. The HT metamorphic overprint of regional extent in the Eastern Series involves progressively rising temperatures from 400 C to 720 C toward the intruding batholith at a uniform shallow level at $10 km depth (3 AE 0Á5 kbar), which is also consistent with the intrusion depth of the batholith. It can be shown that the HT metamorphism and the main intrusion pulse of the batholith is contemporaneous at $300 Ma (Willner et al., 2005). The observed HT metamorphism involves a nearly isobaric temperature increase, which requires a short-time massive heat input related to voluminous magma emplacement. For the retrograde path, a short-term isobaric cooling occurred, at nearly the same temperature as those prevailing in the neighbouring Western Series. A lack of inverse zonation in high-temperature garnets precludes a long time of cooling. In contrast with the Western Series, the local retrograde overprint is of very low temperature type and unrelated to the early exhumation path. Although no definite metamorphic relics prior to the HT overprint of the Eastern Series were detected in the study area, deformation structures were overprinted that occur at very low grade conditions in the Eastern Series of other areas in the Coastal Cordillera basement (Hervé, 1988).
The garnet mica-schist in the Western Series could have reached its maximum depth during subduction roughly below the magmatic arc. As shown by Willner et al. (2005), its peak of metamorphism is older than the main pulse of intrusion in the magmatic arc. Considering the above inferred genetic model for the garnet micaschist, it seems conceivable that some siliciclastic material was subducted to great depth at an early stage, giving rise to a pulse of hydrous fluids released by dehydration that could be responsible for generating the substantial volume of magmas of the late Palaeozoic arc.

The conceptual model
The above considerations point to a convergent subduction regime above a relatively low-angle subducting slab. The data from the study area can help to construct a conceptual model for the Early Palaeozoic convergent margin at an approximate scale (Fig. 11). According to the recorded maximum PT data and their link to the penetrative deformation, basal accretion occurred in the Western Series at a depth of $25-40 km, and small quantities of subducted material (garnet mica-schist) reached maximum depths of $45-50 km at an early stage. If the relationship between this deeply subducted material and the main pulse of magma formation in the arc is correct, this implies a depth of $45-50 km of the subducting slab just below the magmatic arc. The distance between the axis of the magmatic arc and the boundary of the Western and Eastern Series in the southern study area is $30 km. This boundary marks the transition between two environments of contrasting crustal thickness and exhumation rates (Willner et al., 2005). It is assumed here that the thickness of the accretionary prism is a maximum ( $40 km) at this boundary. The distance of $30 km hence marks the horizontal distance between the slab at $40 km and at $50 km depth. A dip angle of the subducting slab of $25 and a width of the Western Series of $40 km results. Isotherms along the subducting slab were drawn in Fig. 11 according to the metamorphic gradient indicated by the blueschist and garnet mica-schist, but at lower crustal levels according to the retrograde path of all rock types and the metamorphic zonation in the Eastern Series.
The boundary between the two metamorphic units lacks an apparent shear zone juxtaposing different crustal levels and excising intermediate levels as is common in orogens worldwide. This transitional nature has been observed at several sites in the Coastal Cordillera (see Hervé, 1988). Such a special situation can be explained only by the cyclic nature of particle paths in the accretionary prism (Western Series), when continuous basal accretion at depth is mainly outbalanced by erosion of the forearc, as is also inferred by modelling (e.g. Kukowski et al., 2002). This creates a stack of crustal slices from the base to the top of the crust with a similar metamorphic and deformational imprint. The retro-wedge (Eastern Series), including the magmatic arc, remained relatively stationary during accretion. Brittle thrusting of the Eastern Series on top of the Western Series, as observed in the north of the study area, occurred at an upper crustal level a long time after accretion had ceased (Willner et al., 2005). This is related to late shortening of the convergent margin.
The oceanward continuation of the Western Series (i.e. the part of the prism with frontal accretion) is not observed anywhere in the Coastal Cordillera basement. However, within the offshore continuation of continental crust $50-80 km toward the west, relics of this missing frontal accretion zone might still be preserved. Hence, it is concluded that in the study area a nearly intact Late Palaeozoic convergent margin, including an accretionary prism and a magmatic arc, is preserved, in which continuous basal accretion of mainly siliciclastic material and minor uppermost oceanic crust occurred over a limited range of time and above a low-angle subducting slab.