Low-temperature eclogite and eclogite facies metapelite together with serpentinite and marble occur as blocks within foliated blueschist that was originated from greywacke matrix; they formed a highpressure low-temperature (HPLT) subduction complex (me´lange) in the North Qilian oceanic-type suture zone, NW China. Phengite-eclogite (type I) and epidote-eclogite (type II) were recognized on the basis of mineral assemblage. Relic lawsonite and lawsonite pseudomorphs occur as inclusions in garnet from both types of eclogite. Garnet-omphacite-phengite geothermobarometry yields metamorphic conditions of 460-510°C and 2.20-2.60 GPa for weakly deformed eclogite, and 475-500°C and 1.75-1.95 GPa for strongly foliated eclogite. Eclogite facies metasediments include garnet-omphacitephengite-glaucophane schist and various chloritoid-bearing schists. Mg-carpholite was identified in some high-Mg chloritoid schists. P-T estimates yield 2.60-2.15 GPa and 495-540°C for Grt-OmpPhn-Gln schist, and 2.45-2.50 GPa and 525-530°C for the Mg-carpholite schist. Mineral assemblages and P-T estimates, together with isotopic ages, suggest that the oceanic lithosphere as well as pelagic to semi-pelagic sediments have been subducted to the mantle depths ( ‡75 km) before 460 Ma. Blueschist facies retrogression occurred at c. 454-446 Ma and led to eclogite deformation and dehydration of lawsonite during exhumation. The peak P-Tconditions for eclogite and metapelite in the North Qilian suture zone demonstrate the existence of cold subduction-zone gradients (6-7°C km )1 ), and this cold subduction brought a large amount of H 2 O to the deep mantle in the Early Palaeozoic times.

Low-T eclogites in the North Qilian orogen, NW China share a common assemblage of garnet, omphacite, glaucophane, epidote, phengite, quartz and rutile with or without paragonite. Phase relations for the low-T eclogites can be modelled well in the system NCKFMASHO with the updated solid-solution models for amphibole and clinopyroxene. Garnet in the eclogite typically exhibits growth zonations in which pyrope increases while grossular somewhat decreases from core to rim, which is modelled as having formed mainly in the P-T conditions of lawsonite-eclogite facies at the pre-peak stage. Omphacite shows an increase in jadeite component as aegirine and also total FeO decrease in going from the inclusions in garnet to grains in the matrix, and from core to rim of zoned crystals, reflecting an increase in metamorphic P-T conditions. Glaucophane exhibits a compositional variation in X(gl) (= Fe 2+ ⁄ (Fe 2+ + Mg)) and F(gl) (= Fe 3+ ⁄ (Fe 3+ + Al) in M2 site), which decrease from the inclusions in garnet to crystals in the matrix, consistent with an increase in P-T conditions. However, for zoned matrix crystals, the X(gl) and F(gl) increase from core to rim, is interpreted to reflect a late-stage decompression. Using composition isopleths for garnet rim and phengite in P-T pseudosections, peak P-T conditions for three samples Q5-45, Q5-01 and Q7-28 were estimated as 530-540°C at 2.10-2.25 GPa, 580-590°C at 2.30-2.45 GPa and 575-590°C at 2.50-2.65 GPa, respectively, for the same assemblage garnet + omphacite + glaucophane + lawsonite (+ phengite + quartz + rutile) at the peak stage. The eclogites suggest similar P-T ranges to their surrounding felsic-pelitic schists. During post-peak decompression of the eclogites, the most distinctive change involves the transformation of lawsonite to epidote, releasing large amount of water in the rock. The released fluid promoted further growth of glaucophane at the expense of omphacite and, in appropriate bulk-rock compositions, paragonite formed. The decompression of eclogite did not lead to pronounced changes in garnet and phengite compositions. Peak P-T conditions of the North Qilian eclogite are well constrained using both the average P-T and pseudosection approaches in Thermocalc. Generally, the conventional garnetclinopyroxene geothermometer is too sensitive to be used for constraining the temperature of low-T eclogite because of the uncertainty in Fe 3+ determination in omphacite and slight variations in mineral compositions because of incomplete equilibration.

In the Chinese southwestern Tianshan (U)HP belt, former lawsonite presence has been predicted for many (U)HP metamorphic eclogites, but only a very few lawsonite grains have been found so far. We discovered armoured lawsonite relicts included in quartz, which, on its part, is enclosed in porphyroblastic garnet in an epidote eclogite H711-14 and a paragonite eclogite H711-29. H711-14 is mainly composed of garnet, omphacite, epidote and titanite, with minor quartz, paragonite and secondary barroisite and glaucophane. Coarse-grained titanite occasionally occurs in millimetre-wide veins in equilibrium with epidote and omphacite, and relict rutile is only preserved as inclusions in matrix titanite and garnet. H711-29 shows the mineral assemblage of garnet, omphacite, glaucophane, paragonite, quartz, dolomite, rutile and minor epidote. Dolomite and rutile are commonly rimed by secondary calcite and titanite respectively. Porphyroblastic garnet in both eclogites is compositionally zoned and exhibits an inclusion-rich core overgrown by an inclusion-poor rim. Phase equilibria modelling predicts that garnet cores formed at the P-peak (490-505°C and 23-25.5 kbar) and coexisted with the lawsonite eclogite facies assemblage of omphacite + glaucophane + lawsonite + quartz. Garnet rims (550-570°C and~20 kbar) grew subsequently during a post-peak epidote eclogite facies metamorphism and coexisted with omphacite + quartz AE glaucophane AE epidote AE paragonite. The results confirm the former presence of a cold subduction zone environment in the Chinese southwestern Tianshan. The P-T evolution of the eclogites is characterized by a clockwise P-T path with a heating stage during early exhumation (thermal relaxation). The preservation of lawsonite in these eclogites is attributed to isolation from the matrix by quartz and rigid garnet, which should be considered as a new type of lawsonite preservation in eclogites. The complete rutile-titanite transition in H711-14 took place in the epidote eclogite facies stage in the presence of an extremely CO 2 -poor fluid with X(CO 2 ) [CO 2 /(CO 2 + H 2 O) in the fluid] <<0.008. In contrast, the incomplete rutile-titanite transition in H711-29 may have occurred after the epidote eclogite facies stage and the presence of dolomite reflects a higher X(CO 2 ) (>0.01) in the coexisting fluid at the epidote eclogite facies stage.

Although eclogites in the Belomorian Province have been regarded as Archean in age and among the oldest in the world, there are also multiple studies that have proposed a Paleoproterozoic age. Here, we present new data for the Gridino‐type eclogites, which occur as boudins and metamorphosed dykes within tonalite–trondhjemite–granodiorite gneisses. Zircon from these eclogites has core and rim structures. The cores display high Th/U ratios (0.18–0.45), negative Eu anomalies and strong enrichment in HREE, and have Neoarchean U–Pb ages of c. 2.70 Ga; they are interpreted to be magmatic in origin. Zircon cores have δ18O of 5.64–6.07‰ suggesting the possibility of crystallization from evolved mantle‐derived magmas. In contrast, the rims, which include the eclogite facies minerals omphacite and garnet, are characterized by low Th/U ratios (<0.035) and flat HREE patterns, and yield U–Pb ages of c. 1.90 Ga; they are interpreted to be metamorphic in origin. Zircon rims have elevated δ18O of 6.23–6.80‰, which was acquired during eclogite facies metamorphism. Based on petrography and phase equilibria modelling, we recognize a prograde epidote amphibolite facies mineral assemblage, the peak eclogite facies mineral assemblage and a retrograde high‐P amphibolite facies mineral assemblage. The peak metamorphic conditions of 695–755°C at >18 kbar for the Gridino‐type eclogites suggest an apparent thermal gradient of <39–42°C/kbar for the Lapland–Kola collisional orogeny.

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