Contrasting Textural and Chemical Signatures of Chromitites in the Mesoarchaean Ulamertoq Peridotite Body, Southern West Greenland

Peridotites occur as lensoid bodies within the Mesoarchaean orthogneiss in the Akia terrane of Southern West Greenland. The Ulamertoq peridotite body is the largest of these peridotites hosted within the regional orthogneiss. It consists mainly of olivine, orthopyroxene, and amphibole-rich ultramafic rocks exhibiting metamorphic textural and chemical features. Chromitite layers from different localities in Ulamertoq show contrasting characteristics. In one locality, zoned chromites are hosted in orthopyroxene-amphibole peridotites. Compositional zonation in chromites is evident with decreasing Cr and Fe content from core to rim, while Al and Mg increase. Homogeneous chromites from another locality are fairly uniform and Fe-rich. The mineral chemistry of the major and accessory phases shows metamorphic signatures. Inferred temperature conditions suggest that the zoned chromites, homogeneous chromites, and their hosts are equilibrated at different metamorphic conditions. In this paper, various mechanisms during the cumulus to subsolidus stages are explored in order to understand the origin of the two contrasting types of chromites.


Introduction
Several peridotite bodies enclosed in tonalitic orthogneiss are found in the Mesoarchaean Akia terrane in Southern West Greenland, which is part of the North Atlantic Craton [1]. However, the origin of these peridotite bodies is still enigmatic. The Ulamertoq body forms part of a series of lens-shaped peridotite bodies that occur in the Akia terrane, and also contains chromitite layers. Chromitites from two localities within the Ulamertoq peridotite body exhibit contrasting petrological and geochemical characteristics.  [22]); (C) Geologic map of Ulamertoq peridotite body showing the sampling locations of chromitites with zoned chromites (filled circle) and homogeneous chromites (filled square) (adapted from Garde [21]).
The Ulamertoq peridotite body measures about 1 km × 1.5 km. The immediately surrounding orthogneiss host also includes smaller pods of amphibolite, as well as peridotite ( Figure 1C). The Ulamertoq peridotite body is dominated by olivine-rich plutonic rocks containing orthopyroxene  [22]); (C) Geologic map of Ulamertoq peridotite body showing the sampling locations of chromitites with zoned chromites (filled circle) and homogeneous chromites (filled square) (adapted from Garde [21]).
The Ulamertoq peridotite body measures about 1 km × 1.5 km. The immediately surrounding orthogneiss host also includes smaller pods of amphibolite, as well as peridotite ( Figure 1C). The Ulamertoq peridotite body is dominated by olivine-rich plutonic rocks containing orthopyroxene and amphibole, which is similar to the other ultramafic bodies in the Akia terrane. The lithological contacts are gradational to uncertain. It is interesting to note that some Ulamertoq samples contain clinopyroxenes, which are not common in other peridotite bodies in the Akia terrane. Anthophyllite, tremolite, chlorite, and phlogopite veins are common. Chromitites occur as irregular and discontinuous layers or thin seams. Harzburgites with poikilitic orthopyroxenes are exposed in the northeastern part. The harzburgites are bounded to the northeast by medium to coarse-grained norite comprised of plagioclase, orthopyroxene, and accessory hornblende and phlogopite. These lithologies have gradational contacts. The peridotite body also has irregular sheets and pods of pink granite, which also cuts the surrounding gneiss [21,22]. The lithologies in Ulamertoq are comparable to those found in the Seqi ultramafic complex (pyroxene-amphibole peridotites or amphibole harzburgites), and tend to occur randomly [22]. The classification used by Szilas et al. [22] to refer to olivine-rich rocks with varying amounts of orthopyroxene and amphibole is also adopted. The ultramafic host and envelope will be simply referred to as peridotites hereafter.

Petrography
The chromitites sampled from the two localities in Ulamertoq (blue symbols in Figure 1C) are differentiated based on the textural and chemical characteristics of its constituent grains, as zoned and homogeneous chromites. The zoned chromites are characterized by concentric zonation with gradually decreasing Cr and Fe concomitant with increasing Mg and Al from core to rim. The homogeneous chromites have fairly uniform composition from core to rim. The peridotite envelope and host of the two types of chromitites also have contrasting features, which will be discussed below.

Zoned Chromite
Chromitites that contain zoned chromites have massive texture. The chromites occur as subhedral to euhedral grains (up to 500 µm). Zonations are observed in backscattered electron (BSE) images, which show concentric variation from bright cores to dark rims. The contrast from core to rim observed in BSE images can be correlated with compositional variation (Section 4.2) (Figure 2C,D and Figure 3). The cores of the zoned chromites are Cr-and Fe-rich, which decrease steadily toward the rim. In contrast, the concentrations of Al and Mg progressively increase away from the core. Thin overgrowths having intermediate composition relative to the core and rim appear as irregular light gray "outer rims" in the BSE images ( Figure 2C,D). The outer rims have sharp contacts with the dark rims of the zoned chromites. Zonation is clearer in coarser chromite grains than in finer grains. Chromite core chemistry was analyzed from the brightest portion of a grain (BSE images), and shows a wide range of compositions within a single thin section. Inclusions in the chromites are mainly amphibole, orthopyroxene, and chlorite, which also commonly occur as interstitial minerals between chromites (Figure 2A-D). The portions within chromite enclosing the silicate inclusions are dark in the BSE images, suggesting that the composition of chromite is affected by the included and surrounding silicate phases. Elemental diffusion in the presence of Al-rich phases has been demonstrated by previous studies on zoned chromites from other localities (e.g., Red Mountain in New Zealand [23]; Rhum layered intrusion in Scotland [7], and the Yanmenguan mafic-ultramafic complex in China [24]). The peridotite envelope and host consist mainly of olivine, orthopyroxene, magnesiohornblende, phlogopite, and accessory chromite ( Figure 2E-G). The accessory chromites in the peridotite envelope are also zoned similar to those in the chromite-rich zone. However, accessory chromites in the host have different textures that are more irregular to subhedral with Cr-rich thin rims (Cr# = 0.37-0.58). The chromite rims have porous textures and contain fine chlorite inclusions ( Figure 2C). envelope, and host peridotites. Exsolution lamellae of clinopyroxene were not observed in any of the orthopyroxenes from the studied samples. In some portions, orthopyroxenes occur adjacent to chromites, forming sutured contacts with chromites ( Figure 2E). Amphiboles are commonly anhedral to subhedral, and are closely associated with intergranular orthopyroxenes and chlorite in the chromitites. In the peridotite host, amphiboles are commonly found as discrete grains between olivine and orthopyroxenes ( Figure 2F).

Homogeneous Chromites
Chromitites with homogeneous chromites are closely packed, and have a low proportion of interstitial phases. These chromites are also finer (up to 200 μm) and exhibit equilibrium textures. Inclusions are also fewer and finer compared to the zoned chromites. Chromites within the chromitite have fairly uniform composition from core to rim. Intergranular phases include olivine, amphibole, and chlorite ( Figure 2G,I). Clinopyroxenes are only observed in chromitite with homogeneous chromites. The clinopyroxenes are also free of exsolution lamellae. The envelope adjacent to the chromite-rich zone contains clinopyroxenes that are closely associated with tremolite ( Figure 2G). Clinopyroxenes and amphiboles are more abundant around the chromite-rich zones. The amount of olivine also increases toward the host as you go away from the chromite-rich zone. Tremolite commonly encloses clinopyroxene, and also occurs as prismatic grains.

Analytical Methods
Major-element compositions of minerals were obtained using a JEOL JXA-8800 (Jeol Ltd., Akishima, Tokyo, Japon) electron probe microanalyzer (EPMA) at the Kanazawa University with    Olivine in the peridotite envelope and host occurs as large crystals (approximately 1.5-6.5 mm), which sometimes contain orthopyroxene and amphibole inclusions. Most of the coarse olivine grains contain minute opaque inclusions, which are probably magnetites ( Figure 2E,F). Finer euhedral olivine grains with well-formed polygonal crystal boundaries are also present. These finer olivine grains are clear and appear to be forming a vein-like fabric. Orthopyroxenes are mainly enstatite (En 89-91 ), and are the only pyroxene phase observed in the chromitites with zoned chromites, envelope, and host peridotites. Exsolution lamellae of clinopyroxene were not observed in any of the orthopyroxenes from the studied samples. In some portions, orthopyroxenes occur adjacent to chromites, forming sutured contacts with chromites ( Figure 2E). Amphiboles are commonly anhedral to subhedral, and are closely associated with intergranular orthopyroxenes and chlorite in the chromitites. In the peridotite host, amphiboles are commonly found as discrete grains between olivine and orthopyroxenes ( Figure 2F).

Homogeneous Chromites
Chromitites with homogeneous chromites are closely packed, and have a low proportion of interstitial phases. These chromites are also finer (up to 200 µm) and exhibit equilibrium textures. Inclusions are also fewer and finer compared to the zoned chromites. Chromites within the chromitite have fairly uniform composition from core to rim. Intergranular phases include olivine, amphibole, and chlorite ( Figure 2G,I). Clinopyroxenes are only observed in chromitite with homogeneous chromites. The clinopyroxenes are also free of exsolution lamellae. The envelope adjacent to the chromite-rich zone contains clinopyroxenes that are closely associated with tremolite ( Figure 2G). Clinopyroxenes and amphiboles are more abundant around the chromite-rich zones. The amount of olivine also increases toward the host as you go away from the chromite-rich zone. Tremolite commonly encloses clinopyroxene, and also occurs as prismatic grains.

Analytical Methods
Major-element compositions of minerals were obtained using a JEOL JXA-8800 (Jeol Ltd., Akishima, Tokyo, Japon) electron probe microanalyzer (EPMA) at the Kanazawa University with operating conditions of 20-kV accelerating voltage, 20-nA beam current, and a 3-µm beam diameter. Natural and synthetic standards were used throughout the analysis. ZAF (Z = atomic number, A = absorption, F = characteristic fluorescence) correction using JEOL JXA-880 software was also used in data processing. Representative major element compositions are presented in Supplementary  Tables S1-S8. Rare earth element (REE) and trace element compositions of amphiboles and clinopyroxenes were determined using a Laser Ablation Inductively Coupled Plasma Mass Spectrometry (LA-ICP-MS) (Agilent 7500S equipped with MicroLas Geolas Q-plus laser system; Agilent Technologies, Santa Clara, CA, US) at Kanazawa University. Each analysis was performed by an ablating spot of 50 µm in diameter at a repetition rate of 6 Hz. NIST SRM 612 was used as an external reference material [25], and data reduction was facilitated using 29 Si as the internal standard, based on the SiO 2 content obtained by EPMA [26]. The complete details of the analytical methods and conditions are described by Morishita et al. [27,28]. Representative REE and trace element compositions are listed in Supplementary Table S9.

Chromite
The chromites in the zoned chromitites have a varying core to rim composition. lower TiO 2 (0.07-0.14 wt %), and lower FeO* (21.4-25.8 wt %). Proportions of Fe 2+ and Fe 3+ were calculated based on stoichiometry. The Fe 2+ and Fe 3+ contents decrease from core to rim and increase in the outer rims ( Figure 3). The thin and irregular-shaped outer rims occur as overgrowths, and are compositionally different (Cr# = 0.37-0.58) from the dark rims with Al 2 O 3 contents from 21.2 wt % to 35.2 wt %, TiO 2 varying from 0.04 wt % to 0.14 wt % and FeO* from 20.4 wt % to 26.3 wt % ( Figure 4A). The accessory chromites in the peridotite immediately adjacent to the chromitites (envelope) also show similar Cr and Fe depletion with Al and Mg enrichment from core to rim. The same zonation is not observed with the accessory chromite in the peridotite host, which is characterized by Cr enrichment from core to rim.  Fields of the olivine-spinel mantle array (OSMA) [4] and Seqi ultramafic complex [1] are shown for reference; (C) The homogeneous chromites are characterized by higher TiO2 contents compared to the zoned chromites. Fields for Rhum layered complex [29], Ujaragssuit [30], and Fiskenaesset [31] are included for comparison.  [4] and Seqi ultramafic complex [1] are shown for reference; (C) The homogeneous chromites are characterized by higher TiO 2 contents compared to the zoned chromites. Fields for Rhum layered complex [29], Ujaragssuit [30], and Fiskenaesset [31] are included for comparison.
The olivine grains interstitial to the homogeneous chromites and those within its host have a narrow range of forsterite contents (Fo = 93.5-94.1 wt % and 93.4-93.7 wt %, respectively) which is higher than those associated with zoned chromites. It is also shown in the OSMA (olivine-spinel mantle array) diagram [4] that the olivine forsterite content in the sample with homogenous chromites is slightly higher relative to those with zoned chromites, as also shown in Figure 4B. The olivine NiO content values related with the homogeneous chromites (0.31-0.44 wt %) are comparable to those with the zoned chromites ( Figure 5A). The olivine MnO contents in both types of chromites are almost similar.
The olivine grains interstitial to the homogeneous chromites and those within its host have a narrow range of forsterite contents (Fo = 93.5-94.1 wt % and 93.4-93.7 wt %, respectively) which is higher than those associated with zoned chromites. It is also shown in the OSMA (olivine-spinel mantle array) diagram [4] that the olivine forsterite content in the sample with homogenous chromites is slightly higher relative to those with zoned chromites, as also shown in Figure 4B. The olivine NiO content values related with the homogeneous chromites (0.31-0.44 wt %) are comparable to those with the zoned chromites ( Figure 5A). The olivine MnO contents in both types of chromites are almost similar.  [29][30][31][32] are also plotted. The mantle olivine array is from Takahashi et al. [33]; (B) The olivine forsterite content and MnO wt % of the Ulamertoq samples are compared with other metamorphic olivine from various studies and olivine from typical residual abyssal peridotite from Warren [34]. Compositions of metamorphic olivine from the Happo-O'ne peridotite complex [35], Tari-Misaka [36], Ohsa-Yama [37] in Japan, and abyssal peridotites [34] are also included for comparison.

Trace Element Geochemistry of Amphiboles and Clinopyroxenes
Amphiboles in both studied chromitites are slightly enriched in light REEs relative to heavy REEs ([Ce/Yb]N = 1.46-3.33). As shown in Figure 8A, in the trace element patterns of hornblende in the zoned chromitite, Sr and high field strength elements (HFSE: Ti, Zr, Nb, and Ta) exhibit various degrees of negative anomalies relative to neighboring REEs. In the homogeneous chromitite ( Figure  8B), trace element abundances are clearly lower in tremolite (e.g., YbN = 4.29) than in hornblende (e.g, YbN = 6.60-13.18). The REE patterns of the hornblende and tremolite are characterized by obvious negative Eu anomalies in contrast to those of hornblende in the chromitite hosting zoned chromites. In the trace element patterns, Sr and HFSE exhibit strong negative anomalies ( Figure 8B). The REE compositions of clinopyroxene are almost equivalent to that of tremolite related to the homogeneous chromites. The clinopyroxenes associated with the homogeneous chromites are depleted in Sr, Eu, and HFSE (Ti, Zr, and Ta).
Amphiboles show similar patterns in the chondrite-normalized spider diagram, with a more pronounced Sr anomaly compared to the clinopyroxenes (Figure 8).

Trace Element Geochemistry of Amphiboles and Clinopyroxenes
Amphiboles in both studied chromitites are slightly enriched in light REEs relative to heavy REEs ([Ce/Yb] N = 1.46-3.33). As shown in Figure 8A, in the trace element patterns of hornblende in the zoned chromitite, Sr and high field strength elements (HFSE: Ti, Zr, Nb, and Ta) exhibit various degrees of negative anomalies relative to neighboring REEs. In the homogeneous chromitite ( Figure 8B), trace element abundances are clearly lower in tremolite (e.g., Yb N = 4.29) than in hornblende (e.g, Yb N = 6.60-13.18). The REE patterns of the hornblende and tremolite are characterized by obvious negative Eu anomalies in contrast to those of hornblende in the chromitite hosting zoned chromites. In the trace element patterns, Sr and HFSE exhibit strong negative anomalies ( Figure 8B). The REE compositions of clinopyroxene are almost equivalent to that of tremolite related to the homogeneous chromites. The clinopyroxenes associated with the homogeneous chromites are depleted in Sr, Eu, and HFSE (Ti, Zr, and Ta).
Amphiboles show similar patterns in the chondrite-normalized spider diagram, with a more pronounced Sr anomaly compared to the clinopyroxenes (Figure 8).

Original Composition of Zoned Chromites
The cores of the zoned chromites show a wide variety of chemical compositions. The core compositions from different grains have a broad range of Cr# aside from the individual variation within each grain. Therefore, the original composition of the chromites may not be preserved by most of the chromite cores. The most Cr-rich cores of the zoned chromites are comparable to the homogeneous chromites. Chromite cores with the highest Cr content could have possibly retained the original composition of the zoned chromites. Some of these chromite grains, with relatively higher Cr#, are partly or entirely enclosed within olivine. Chromites that are closely associated with olivine show lesser variation in composition from core to rim (Figure 9). The surrounding olivine may have buffered the trivalent cation diffusion with chromite, because it contains lesser Al, Cr, and Fe 3+ . This observation is also similar to the accessory spinels in the ultramafic rocks from the Yanmenguan mafic-ultramafic complex [42]. In comparison to the chromites enveloped by Al-rich phases, the core compositions of some of the chromites surrounded by olivine may be the least modified. Core compositions of such zoned chromites are characterized by higher Cr content (Cr# = 0.52-0.62) relative to other zoned chromite grains (as low as Cr# = 0.35) that are surrounded by Al-rich phases. Those chromites enveloped by olivine, which are also the most Cr-rich, could possibly represent the original composition of the chromites. Although, the possibility that the original chromite composition may have completely overprinted is also not ruled out.
It is obvious that zoned chromites were chemically modified from the original igneous compositions. Core analyses exhibit a wide variety of Al contents from core to rim, and among chromite grains in a single thin section ( Figure 10). Moreover, coarser chromite grains tend to retain a more pronounced compositional zonation, whereas finer grains are more readily equilibrated with surrounding silicate phases. These observations further complicate the possible original composition of chromites.
The TiO2 and Al2O3 of the melt from which the chromites crystallized are highly associated with the TiO2 and Al2O3 of the chromites [6,24]. The composition of the Ulamertoq chromites suggests that the zoned chromites, if retaining igneous compositions, formed from a melt with higher Al2O3 and lower TiO2 melt, in contrast to the homogeneous chromite ( Figure 4C).

Original Composition of Zoned Chromites
The cores of the zoned chromites show a wide variety of chemical compositions. The core compositions from different grains have a broad range of Cr# aside from the individual variation within each grain. Therefore, the original composition of the chromites may not be preserved by most of the chromite cores. The most Cr-rich cores of the zoned chromites are comparable to the homogeneous chromites. Chromite cores with the highest Cr content could have possibly retained the original composition of the zoned chromites. Some of these chromite grains, with relatively higher Cr#, are partly or entirely enclosed within olivine. Chromites that are closely associated with olivine show lesser variation in composition from core to rim (Figure 9). The surrounding olivine may have buffered the trivalent cation diffusion with chromite, because it contains lesser Al, Cr, and Fe 3+ . This observation is also similar to the accessory spinels in the ultramafic rocks from the Yanmenguan mafic-ultramafic complex [42]. In comparison to the chromites enveloped by Al-rich phases, the core compositions of some of the chromites surrounded by olivine may be the least modified. Core compositions of such zoned chromites are characterized by higher Cr content (Cr# = 0.52-0.62) relative to other zoned chromite grains (as low as Cr# = 0.35) that are surrounded by Al-rich phases. Those chromites enveloped by olivine, which are also the most Cr-rich, could possibly represent the original composition of the chromites. Although, the possibility that the original chromite composition may have completely overprinted is also not ruled out.  It is obvious that zoned chromites were chemically modified from the original igneous compositions. Core analyses exhibit a wide variety of Al contents from core to rim, and among chromite grains in a single thin section ( Figure 10). Moreover, coarser chromite grains tend to retain a more pronounced compositional zonation, whereas finer grains are more readily equilibrated with surrounding silicate phases. These observations further complicate the possible original composition of chromites.  [43], Evans and Frost, [9], and Suita and Streider [44]).

Chromite Composition Variation
Compositional variations within chromite grains may be associated with the changes in the parental melt [45]. The depletion of Cr in the residual melt as a result of extensive chromite crystallization could produce a more Cr-poor and Al-rich melt [45,46]. The change in melt composition during crystallization could also affect the chromite composition. This mechanism of progressive change from a Cr-rich core to Al-rich rim was observed in layered mafic-ultramafic complexes (e.g., the Rhum layered mafic-ultramafic complex) [46,47]. The spinel chemistry of the peridotites from the Rhum layered complex (Scotland) [46] and Red Mountain (New Zealand) [23] also show an increase in Mg and Al, and a decrease in Cr and Fe, from core to rim. The compositional changes within chromite grains were attributed to the postcumulus reaction of chromite with intercumulus liquid and Al-rich cumulus phases. Similar chromite zonation was also observed in cumulates from the Bushveld complex (South Africa), but it was linked to reactions during the cumulus stage at the onset and early stages of chromite crystallization [48].
Subsolidus elemental exchange between chromite and coexisting Al-rich phases could also account for the zonation observed in the chromites [49]. The compositional zonation observed in the chromites that are closely associated with pyroxenes, amphiboles and plagioclase from the Red Mountain mafic-ultramafic complex and Rhum layered complex are also attributed to subsolidus reactions. Continuous elemental exchange from postcumulus to subsolidus stages may have caused the Al enrichment along the chromite rims. In the Yanmenguan mafic-ultramafic complex in China, similar zonations characterize the chromite inclusions in enstatite, tschermakite, and phlogopite [42]. Olivine-hosted chromites also exhibit zonation, but to a lesser extent due to its low Cr and Al contents relative to pyroxenes and amphiboles.
Another mechanism that may explain the enrichment of Al toward the rim in chromite is its reaction with surrounding chlorite, as observed in the Calzadilla de los Barros ultramafic body (Spain). In a retrograde P-T path, chromite and olivine with high silica activity and a high fluid-to-rock ratio result in the formation of chlorite and Al-poor chromite [13]. Subsequent heating, which may have been caused by the gabbro intrusions in the area, initiated a reaction in the opposite Figure 10. Cr-Fe 3+ -Al triangular plot of the Ulamertoq chromites with fields of metamorphic spinels from different metamorphic grades (fields taken from the data of Purvis et al. [43], Evans and Frost, [9], and Suita and Streider [44]).
The TiO 2 and Al 2 O 3 of the melt from which the chromites crystallized are highly associated with the TiO 2 and Al 2 O 3 of the chromites [6,24]. The composition of the Ulamertoq chromites suggests that the zoned chromites, if retaining igneous compositions, formed from a melt with higher Al 2 O 3 and lower TiO 2 melt, in contrast to the homogeneous chromite ( Figure 4C).

Chromite Composition Variation
Compositional variations within chromite grains may be associated with the changes in the parental melt [45]. The depletion of Cr in the residual melt as a result of extensive chromite crystallization could produce a more Cr-poor and Al-rich melt [45,46]. The change in melt composition during crystallization could also affect the chromite composition. This mechanism of progressive change from a Cr-rich core to Al-rich rim was observed in layered mafic-ultramafic complexes (e.g., the Rhum layered mafic-ultramafic complex) [46,47]. The spinel chemistry of the peridotites from the Rhum layered complex (Scotland) [46] and Red Mountain (New Zealand) [23] also show an increase in Mg and Al, and a decrease in Cr and Fe, from core to rim. The compositional changes within chromite grains were attributed to the postcumulus reaction of chromite with intercumulus liquid and Al-rich cumulus phases. Similar chromite zonation was also observed in cumulates from the Bushveld complex (South Africa), but it was linked to reactions during the cumulus stage at the onset and early stages of chromite crystallization [48].
Subsolidus elemental exchange between chromite and coexisting Al-rich phases could also account for the zonation observed in the chromites [49]. The compositional zonation observed in the chromites that are closely associated with pyroxenes, amphiboles and plagioclase from the Red Mountain mafic-ultramafic complex and Rhum layered complex are also attributed to subsolidus reactions. Continuous elemental exchange from postcumulus to subsolidus stages may have caused the Al enrichment along the chromite rims. In the Yanmenguan mafic-ultramafic complex in China, similar zonations characterize the chromite inclusions in enstatite, tschermakite, and phlogopite [42]. Olivine-hosted chromites also exhibit zonation, but to a lesser extent due to its low Cr and Al contents relative to pyroxenes and amphiboles.
Another mechanism that may explain the enrichment of Al toward the rim in chromite is its reaction with surrounding chlorite, as observed in the Calzadilla de los Barros ultramafic body (Spain). In a retrograde P-T path, chromite and olivine with high silica activity and a high fluid-to-rock ratio result in the formation of chlorite and Al-poor chromite [13]. Subsequent heating, which may have been caused by the gabbro intrusions in the area, initiated a reaction in the opposite direction. The reaction of chlorite and chromite at a higher temperature resulted in an increase of Mg and Al in the chromites at Calzadilla de los Barros [50].

Metamorphism vs. Metasomatism
Diopsides have compositions that are different from typical primary residual clinopyroxenes. Tremolite surrounding the diopside displays a replacive texture ( Figure 2G). Trace element data show that the tremolites and magnesiohornblendes have trace element patterns similar to the clinopyroxenes, but are relatively more enriched, suggesting the possible effects of metasomatism. The presence of phlogopite in the samples with zoned chromitites hints at the introduction of K from metasomatizing fluids, or melts that could probably be associated with the tonalitic gneiss enclosing and intruding the peridotite bodies.

Metamorphism and Pressure-Temperature Path
Several textural and chemical features of the peridotite envelope and host represent metamorphic imprints on the Ulamertoq peridotite body. The variable compositions of the chromite cores, with a significant increase in Al and Mg coupled with Cr and Fe 2+ decrease from core to rim, suggest that the Ulamertoq chromitites were modified under prograde metamorphism. Chromites that were metamorphosed at low temperatures typically have low Al contents [51]. Metamorphic reactions above 550 • C with surrounding silicates and infiltrating fluids will modify the trivalent cation chemistry of the chromites [52,53]. Comparison with other metamorphic spinels from various metamorphic grades places the zoned chromites from Ulamertoq between the fields of lower amphibolite and upper amphibolite-granulite facies ( Figure 10).
Silicate phases in the peridotite envelope and host show textural and compositional characteristics affected by metamorphism. Most of the olivine grains contain minute opaque inclusions that can be attributed to the deserpentinization process [36]. The dehydration of serpentine during prograde metamorphism produces Mg-rich metamorphic olivine and Fe-rich opaque phases [36,54]. The dehydration of serpentine and recrystallization of secondary olivine could explain the abundance of such inclusions. This process could also be linked to the MnO enrichment in olivine, in which it is preferentially partitioned. Also, the depletion of Al 2 O 3 in the pyroxenes has been ascribed to a metamorphic or secondary origin ( Figure 6A-D) [36,55]. Low CaO, Al 2 O 3 , and Cr 2 O 3 in the orthopyroxenes are commonly observed in metasomatic orthopyroxenes in deserpentinized peridotites [56]. Secondary orthopyroxenes can be formed by the reaction between Si-rich melt/fluid with olivine [57]. The composition of the tremolites and other amphiboles are also similar to prograde tremolites that are interpreted as products of the breakdown of serpentine [35,40].
The silicates that are interstitial to the zoned chromites and within the peridotite envelope include olivine+orthopyroxene+amphibole. In the CaO-MgO-SiO 2 -H 2 O phase equilibria, this assemblage is stable above 650 • C. However, the absence of clinopyroxene from this sample limits the temperature to below 800 • C [58]. Orthopyroxenes in prograde metamorphism may be produced by the reaction: 2Tlc + 2Fo = 5En + 2H 2 O (Tlc = talc; Fo = forsterite; En = enstatite) ( Figure 11).
The Al increase toward the rim can be explained by the reaction of chromite with Al-rich silicates driven by high-grade metamorphism [9]. The outer rims of the zoned chromites preserve porous textures with chlorite inclusions. The Cr# increases and Al content decreases in the outermost rims. The outer rims could be products of equilibration during a retrograde stage in the presence of fluids. The outer rims that are commonly in contact with chlorite could be products of a younger event.
The chromitite with homogeneous chromites and its peridotite envelope contain clinopyroxenes, but are devoid of orthopyroxene. The assemblage olivine+clinopyroxene+tremolite suggests a lower temperature stability at around 530 • C [58]. Clinopyroxene may also be stable at higher temperatures, but the absence of orthopyroxene points more likely to a lower temperature stability.
The similarity of REE patterns between clinopyroxenes and amphiboles possibly indicates strong modification by a hydrous melt [59,60] during metamorphism, which is also suggested by their textural relationship.
The absence of plagioclase and garnet restricts the pressure of the Ulamertoq ultramafic rocks within the spinel stability field. The transition from plagioclase to spinel in lherzolites occurs within 0.6-0.8 GPa [61][62][63], and spinel-to-garnet lherzolite transitions at 3.0 GPa, depending on the Cr# of the system [64,65]. Hence, the equilibration temperature condition of the Ulamertoq peridotite may be between these transition pressures. Pressure constraints may only be based on the presence of chromite in the spinel stability field, although the possibility of coexistence of the assemblages in both types of chromitites and associated peridotites above 14 kbar (CaO-MgO-SiO 2 -H 2 O phase equilibria) is not disregarded (Figure 11). the system [64,65]. Hence, the equilibration temperature condition of the Ulamertoq peridotite may be between these transition pressures. Pressure constraints may only be based on the presence of chromite in the spinel stability field, although the possibility of coexistence of the assemblages in both types of chromitites and associated peridotites above 14 kbar (CaO-MgO-SiO2-H2O phase equilibria) is not disregarded (Figure 11). It is possible that the Fiskefjord peridotite bodies may represent residues after extensive melt extraction; however, a cumulate origin is currently favored [22]. Bulk-rock geochemistry shows that the MgO contents of the Seqi peridotites are compositionally variable, extending up to 50%, and FeOt is too high for typical mantle rocks [68]. The mantle-derived ultramafic rocks erupted by kimberlites in southern West Greenland typically are relatively orthopyroxene-poor, and have orthopyroxene compositions that are consistent with equilibration pressures ranging from the spinel to garnet stability fields [38,69]. Furthermore, the close spatial association of the Fiskefjord It is possible that the Fiskefjord peridotite bodies may represent residues after extensive melt extraction; however, a cumulate origin is currently favored [22]. Bulk-rock geochemistry shows that the MgO contents of the Seqi peridotites are compositionally variable, extending up to 50%, and FeO t is too high for typical mantle rocks [68]. The mantle-derived ultramafic rocks erupted by kimberlites in southern West Greenland typically are relatively orthopyroxene-poor, and have orthopyroxene compositions that are consistent with equilibration pressures ranging from the spinel to garnet stability fields [38,69]. Furthermore, the close spatial association of the Fiskefjord peridotites with norites is consistent with their origin as fragments of layered complexes that predate the regional tonalitic orthogneiss [1]. Several lines of petrological, field, and geochemical evidence also favor a cumulate origin. The presence of poikilitic pyroxenes and reports of chromitites occurring as subparallel layers, orthopyroxene cross-bedding, and layering in the field are more associated with igneous crustal processes [22]. The bulk-rock chemistry of Seqi peridotites is also akin to komatiite cumulates. The spinel Mg# of the Ulamertoq is also incomparable to typical mantle rocks [68], but it is similar to those observed in Seqi peridotites ( Figure 4B) that also intrude the regional orthogneiss, and are currently interpreted as an ultramafic cumulate. The Cr# also exhibits variable Al enrichment, even among core analyses, and thus not all cores are representative of its pristine composition. Norites are closely associated with the Fiskefjord peridotites [1]. In Seqi peridotites, negative Eu anomalies observed in the bulk rock, and amphibole chemistry also suggest a possible link to plagioclase fractionation with the surrounding norites. Such an anomaly was also observed in the orthopyroxenes. The Ulamertoq peridotite body is also closely associated with norites ( Figure 1C).

Conclusions
The chromitites recovered from different localities in Ulamertoq show contrasting textural, mineralogical, and compositional characteristics. The zoned chromites are hosted in olivine-orthopyroxene-amphibole peridotite, and could be possibly metamorphosed up to upper amphibolite facies. The compositional zonation in chromites may be attributed to subsolidus equilibration with surrounding Al-rich phases. The homogeneous chromites, on the other hand, are hosted in olivine-clinopyroxene-tremolite peridotite, and could be metamorphosed at a lower metamorphic grade (greenschist to lower amphibolite facies), or have retrogressed more extensively. The presence of outer rims of Al-poor chromites may represent a younger metasomatic event involving retrograde chlorite. The composition of silicate phases also suggests metamorphic recrystallization. It is possible that several metamorphic imprints are already observed, and the detailed P-T path may be more complex. The combined petrological and mineral chemical data available for the Ulamertoq peridotite body suggest that the ultramafic rocks within it are likely derived via cumulate processes rather than the body representing a fragment of residual upper mantle.