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Article

New Occurrence of Pyroxenites in the Veria-Naousa Ophiolite (North Greece): Implications on Their Origin and Petrogenetic Evolution

by
Aikaterini Rogkala
1,*,
Petros Petrounias
1,
Basilios Tsikouras
2 and
Konstantin Hatzipanagiotou
1
1
Section of Earth Materials, Department of Geology, University of Patras, 265 00 Patras, Greece
2
Faculty of Science, Physical and Geological Sciences, Universiti Brunei Darussalam, Jalan Tungku Link, Bandar Seri Begawan, Gadong BE1410, Brunei Darussalam
*
Author to whom correspondence should be addressed.
Geosciences 2017, 7(4), 92; https://doi.org/10.3390/geosciences7040092
Submission received: 6 June 2017 / Revised: 10 September 2017 / Accepted: 13 September 2017 / Published: 21 September 2017
(This article belongs to the Special Issue Petrogenesis of Ophiolites)
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Abstract

:
The Veria-Naousa ophiolite represents a dismembered unit in north Greece, which includes variably serpentinised lherzolite and harzburgite, locally intruded by a sparse network of dykes or thin layers of websterite and olivine-orthopyroxenite composition. The websterite and the olivine-orthopyroxenite show abundant petrographic and geochemical evidence (relic olivines with mantle affinities, Cr-rich spinels, low Al2O3, depletions in incompatible elements, and concave upwards rare earth element patterns) that they comprise replacive bodies from refractory subarc mantle precursors. The occurrence of these pyroxenites in dykes implies that channelled percolation of melts account for their replacive character. High CaO/Al2O3, low Zr and crystallisation of diopside suggest that a melt of ankaramitic/carbonatitic composition percolated in lherzolite replacing porphyroclastic olivine and forming the pyroxenes in the websterite. At a shallower level, harburgites were impregnated by boninitic melts (inferred by U-shape rare earth element patterns and very rich in Cr spinels) triggering the replacement of porphyroclastic olivine by orthopyroxene for the formation of olivine-orthopyroxenite. These peritectic replacements of olivine commonly occur in a mantle wedge regime. The peculiar characteristics of the Veria-Naousa pyroxenites with LREE and compatible elements enrichments resemble the subarc pyroxenites of Cabo Ortegal implying a similar environment of formation. Whole-rock and mineralogical (spinel and clinopyroxene) compositions are also in favour of a backarc to arc environment. It is recommended that the evolution of the Veria-Naousa pyroxenites record the evolution of the subarc region and the opening of a backarc basin in a broad SSZ setting in the Axios Zone of eastern Greece.

1. Introduction

Subduction-related and subduction-unrelated ophiolites [1] form in a variety of tectonic settings including oceanic spreading centres, backarc and forearc basins, arcs and other extensional magmatic settings including those in association with plumes [2,3,4,5,6]. The chemical composition of ophiolitic rocks is commonly used for recognising a variety of different tectonic settings, as well as the nature of mantle sources. The ophiolites that form as a result of subduction initiation processes host of a sequence of igneous rocks formed by a magma source that changed progressively in composition by the combined effects of melt depletion and subduction-related metasomatism [7,8].
Pyroxenites with variable modal contents of olivine, garnet and spinel, ranging in composition from orthopyroxenite through websterite to clinopyroxenite are important constituents of the upper mantle, usually forming veins, layers, or dykes in peridotites [9,10,11,12]. Mantle-derived pyroxenites also occur as xenoliths in alkali basaltic or kimberlitic lavas, commonly associated with peridotites [13,14]. They are genetically diverse and may have formed initially in the mantle, the oceanic or even in the continental crust. Usually, mantle pyroxenites are interpreted as precipitates from asthenosphere-derived melts that passed through the lithospheric mantle [15]. A small number of these formed as high-pressure, pyroxenitic cumulates [10,15]. This rock type is of great importance for the genesis of mid-ocean ridge basalt [16], ocean-island basalt [17,18,19], and arc magmas [20]. Moreover, pyroxenite may be the missing link to explain the imbalance between the compositions of continental crust and primary arc magmas [21,22], therefore it may play a key role in global dynamic processes.
Numerous studies are associated with diverse pyroxenites, which are commonly distributed in the upper mantle. These rocks do not only influence mantle heterogeneity but also act as inferred source materials of ocean island arc and mid-ocean ridge basalts [23,24,25,26]. Pyroxenites are considered to be a significant component in the Earth’s mantle, yet their genesis remains controversial [27,28]. They can be “secondary” products of reaction between mantle peridotite and infiltrating melts, which may be derived from recycled crustal components or from the melting of ambient peridotite [18,29,30]. The genesis of mantle pyroxenites is divided into three categories: high pressure cumulates from basaltic magmas passing through the mantle, solid-state remnants of subducted oceanic crust and metasomatic products resulting from the interaction of pervasive melts with mantle peridotites [18,21,31]. Modal mineralogy and primary mineral compositions of the upper mantle pyroxenites are considered as a key to constrain the extent of partial melting, fluid phase enrichment and mantle-melt interaction processes subsequent to melt extraction [32].
In this study, we present for the first time textural, petrographic, mineralogical and geochemical features of mantle pyroxenites from the Veria-Naousa ophiolite aiming at constraining their genesis and the geodynamic processes during their formation.

2. Geological Setting

Extensive fieldwork in the Veria-Naousa ophiolitic complex focused mainly on the distribution and mode of development of the ophiolitic rocks, as well as their relation to the adjacent formations. These rocks extend throughout the area between Veria and Naousa towns and belong to the Almopias subzone of the Axios geotectonic zone, in northern Greece (Figure 1). They represent remnants of oceanic lithosphere which were thrust from one or more ocean basins and have been obducted onto Late Triassic-Jurassic platform carbonates of the Pelagonian Zone during Upper Jurassic to Lower Cretaceous [33,34,35,36,37]. The ophiolite is a dismembered suite and includes, from base to top, serpentinised lherzolite and harzburgite, intruded by a sparse network of pyroxenitic dykes, as well as gabbro, diabase and pillow basalt. The serpentinised peridotites are intensely tectonised, showing a dense network of joints. Rare rodingite dykes occur in the serpentinised ultramafic rocks. Neogene to Quaternary sedimentary formations (conglomeratic limestone, breccia limestone, flysch) lie uncomfortably on the ophiolite. A granite to granodiorite body, of unknown age, penetrates serpentinised peridotites near the village of Trilofos (Figure 1). A cataclastic zone of diabasic fragments and albitite veins is observed along the eastern contact of the ophiolite with the Pelagonian carbonate rocks (Figure 1).
Pyroxenites are the least abundant rock units among the Veria-Naousa ultramafic section. Websterite and Olivine-orthopyroxenite (Ol-orthopyroxenite) form tectonically disrupted dykes or thin layers up to 1 m thick and a few tens of meters long, within serpentinised harzburgite. The small sizes of the pyroxenite outcrops render their mapping difficult; hence, their occurrences are indicated on the geological map with stars (Figure 1).

3. Petrographic Features

Pyroxenites show variable degrees of alteration and include two lithotypes: websterite and Ol-orthopyroxenite.

3.1. Websterite

The websterite presents generally porphyroclastic texture in places obliterated by secondary minerals. It consists of porphyroclasts of orthopyroxene and clinopyroxene, which are surrounded by neoblasts of orthopyroxene and clinopyroxene (Figure 2a,b). Overall, orthopyroxene (50–70 vol. %), clinopyroxene (20–40 vol. %), as well as minor olivine (<5 to 10 vol. %) percentages allow its classification as websterite. Blebs and exsolution lamellae of clinopyroxene are observed in orthopyroxene porphyroclasts. The clinopyroxene occurs either as subhedral tabular grains exhibiting sub-grain boundaries with orthopyroxene or as neoblasts at the rims of the subhedral clinopyroxene (Figure 2a,b). Olivine generally occurs in the form of subhedral crystals. Variable amounts of secondary serpentine, Cr-bearing chlorite, talc and Cr-magnetite were formed after orthopyroxene, olivine and presumably spinel, during subsequent hydrothermal alteration (Figure 2b). Numerous serpentine veins are observed within cracks and along grain boundaries of olivine, orthopyroxene and clinopyroxene. In places, metasomatic garnet (Ti-andradite), clinopyroxene and rare magnetite developed in veins crosscutting the rock.

3.2. Ol-Orthopyroxenite

The Ol-orthopyroxenite samples generally display a porphyroclastic texture and their primary modal mineralogical composition includes orthopyroxene (70–80 vol. %), clinopyroxene (up to 5 vol. %), olivine (~10 vol. %) and Cr-spinel (5–10 vol. %) (Figure 2c,d). Rare Fe-Ni-Co sulphides coexist with Cr-spinel. Orthopyroxene porphyroclasts (up to 2 cm long, Figure 2d) exhibit local kink bands, undulatory extinction and frequent exsolution lamellae of clinopyroxene. Unstrained smaller orthopyroxene and lesser clinopyroxene comprise a younger generation and are dispersed along rims or enclosed in orthopyroxene porphyroclasts (Figure 2e). Two generations of Cr-spinel grains occur: The first includes subhedral to anhedral magnesiochromites to chromites commonly with lobate boundaries (Figure 2d,f). Infrequently, they form kelyphitic textures surrounded by orthopyroxene or, more often, they occur along orthopyroxene grain boundaries. The second includes smaller subhedral (rarely euhedral) magnesiochromite to chromite crystals (Figure 2c,d). Serpentine is the dominant alteration product forming mesh and bastite textures; lesser amounts of chlorite, talc and magnetite occur, as well.

4. Analytical Methods

The mineralogical and textural characteristics of the samples were studied in polished-thin sections in polarising optical and scanning electron microscopes (SEM). Mineral microanalyses were performed using a JEOL JSM-6300 SEM equipped with energy dispersive and wavelength spectrometers (EDS and WDS) and INCA software at the Laboratory of Electron Microscopy and Microanalysis, University of Patras, Greece. Operating conditions were accelerating voltage 25 kV and beam current 3.3 nA, with a 4-μm beam diameter. The total counting time was 60 s and dead-time 40%. Synthetic oxides and natural minerals were utilised as standards for our analyses. Detection limits are ~0.01% and accuracy better than 5% was obtained. Whole-rock chemical analyses for major and trace elements were performed at Bureau Veritas Mineral Laboratories, Vancouver, Canada. Major element analyses were carried out using an XRF spectrometer and a sequential spectrometer (ICP-ES). Trace elements and rare earth elements were determined on totally digested samples by inductively coupled plasma-mass spectrometry (ICP-MS) in the same laboratory. Detection limits for major and trace elements range from 0.01 wt % to 0.04 wt % and from 0.01 ppm to 10 ppm, respectively. The analytical precision calculated from replicate analyses is better than 3% for most major elements and better than 5% for trace elements.

5. Mineral Chemistry

5.1. Orthopyroxene

Orthopyroxene crystals in the analysed Ol-orthopyroxenite and websterite are enstatites with relatively homogenous compositions (Table 1). The Mg# (= 100 × Mg/(Mg + Fe2+) in atoms per formula unit) of the orthopyroxenes in the Ol-orthopyroxenite is lower (87.1–91.4) than the Mg# of the orthopyroxenes in the websterite (90.5–92.5) (Figure 3a,b). The porphyroclastic enstatites in the Ol-orthopyroxenite and websterite are generally richer in Al (with large overlap) and poorer in Ca and Cr than the secondary enstatites (Figure 3a,b). Overall, the enstatites of the websterite have higher amounts of Al2O3 (1.90–3.15 wt %) and lower FeO contents (4.84–6.17 wt %) than those in the Ol-orthopyroxenite (0.28–2.03 wt % and 5.47–8.20 wt %, respectively) (Figure 3b). All orthopyroxenes have low CaO (<3 wt %) and Cr2O3 (<0.95 wt %).

5.2. Clinopyroxene

Representative clinopyroxene analyses from the investigated websterite and Ol-orthopyroxenite are listed in Table 2. They comprise diopsides with low Al2O3, Cr2O3 and particularly TiO2 contents (Figure 3c,d). The neoblastic and the porphyroclastic diopsides in these pyroxenites form two geochemically distinct groups. The porphyroclastic diopsides display lower contents in Ca and Fe, and higher contents in Al, and Cr, Mg and Mg# (Mg# is particularly true for the websterite only) having mantle affinities (Figure 3c,d). Some clinopyroxene neoblasts show slight enrichments in Mn.

5.3. Olivine

Representative olivine analyses from the Ol-orthopyroxenite are listed in Table 3. Fo contents range from 88.9 to 89.6, which are similar to Fo values of olivines from typical supra-subduction zone (SSZ) peridotites (Fo = 87–94 [38]). We were unable to obtain reliable microanalyses from the websterite due to extensive serpentinisation. The analysed olivines show a rather uniform composition, having in particular, very similar FeO (9.75–10.46 wt %) and MgO (46.22–49.10 wt %) contents. NiO contents are rather high ranging from 0.22 to 0.46 wt %, in the range of average NiO concentrations for mantle olivines (0.25–0.51 wt % [39]).

5.4. Spinel-group Minerals

Representative analyses of spinel-group minerals are reported in Table 4 and plotted in Figure 4. Anhedral and subhedral to euhedral crystals comprise two texturally different generations of spinels in the Ol-orthopyroxenite. Both are magnesiochromites to chromites and show similar ranges of Mg# (28.1–54.4) and Cr# (= 100 × Cr/(Cr + Al), atomic ratios, 52.5–86.9). A number of analyses from both generations cluster in the field of spinels occurring in boninitic basalts, whereas some others are plotted mostly in the field of spinels from marginal basins basalts (Figure 4).

6. Whole-Rock Geochemistry

Major, trace and rare earth elements data from the pyroxenites from the Veria-Naousa ophiolite are listed in Table 5 and their compositional variations are illustrated in Figure 5, Figure 6 and Figure 7. One websterite and three Ol-orthopyroxenite samples were analysed. Care was taken in screening the samples for whole-rock analyses, as well as for the interpretations, as variable degrees of serpentinisation are observed in the pyroxenites, therefore only the freshest samples have been considered. The websterite has higher loss on ignition (LOI) (8.8 wt %) than the other orthopyroxenites (1.1–2.9 wt %) as a result of its higher degree of alteration.
On a volatile-free basis, the Ol-orthopyroxenite samples are richer in SiO2 (Figure 5a) than the websterite and are silica-hypersthene normative, as an indication for their chemical modification by silica rich fluids. They show moderate Mg# ranging from 80.1 to 81.7 (Table 5). On a volatile-free basis, the websterite is poor in Fe2O3 but it contains higher Al2O3 and expectedly higher CaO than the Ol-orthopyroxenite (Figure 5b,c). It also shows the highest CaO/Al2O3 ratio (Figure 5d) and Mg# (87.9) and has an olivine-hypersthene normative composition.
All samples are poor in incompatible high field strength elements (HFSE) but, generally, the websterite is the most depleted of all (Table 5). Ni contents vary strongly with the Ol-orthopyroxenites having the lowest Ni values (81.3−655.0, Figure 6b, Table 5). The analysed pyroxenites from Veria-Naousa show considerable geochemical similarities in terms of major and some compatible and incompatible trace elements to pyroxenites from Cabo Ortegal (Figure 5 and Figure 6). The websterite and the Ol-orthopyroxenite are strongly depleted in REE, with many REE values below detection limits. LREE in the websterite lie below their detection limits hence a general positive fractionated REE normalised pattern can be inferred for this sample (Figure 7). The Ol-orthopyroxenites are strongly depleted in middle REE showing enrichments in both LREE and HREE, resembling rocks with concave upwards REE normalised patterns (Figure 7). These LREE enriched patterns are similar to most of the well-known pyroxenite assemblages which show depletions in LREE relative to HREE [27,45], and show considerable similarities to pyroxenites from Cabo Ortegal.

7. Geothermometry

The equilibration temperatures for websterite and Ol-orthopyroxenite were determined using two-pyroxenes (clinopyroxene-orthopyroxene) thermometry proposed by Wood and Banno [47]. Rim composition of the coexisting mineral pairs has been used for geothermometry calculation. We selected co-existing mineral phases for estimation of temperature. These co-magmatic mineral phases have a well-defined common boundary with no evidence of alteration and similar Mg#, which indicate that they have attained the equilibrium condition.
Two-pyroxene thermometry indicates equilibration temperature of 1136 °C for the websterite and 972–974 °C for Ol-orthopyroxenites (Table 6).

8. Petrogenetic and Geodynamic Considerations

8.1. Origin of Ol-Orthopyroxenite and Websterite

Several lines of evidence suggest that the Ol-orthopyroxenite and the websterite are results of melt-rock reaction. The occurrence of porphyroclasts of orthopyroxene and olivine with mantle affinities in the pyroxenites suggests mantle peridotite precursors. Their highly depleted nature in HFSE and the high Cr (and Ni in the websterite) contents strongly suggest a residual character for their precursors, which must have been affected by plastic asthenospheric deformation. Spinel with lobate boundaries is compatible with a dominant partial melting process, which is normally observed in such residual peridotites. A harzburgite precursor appears most probable for the Ol-orthopyroxenite whereas a residual lherzolite is more likely the precursor of the websterite, as inferred from the presence of abundant diopsidic porphyroclast relics. This evidence is compatible with the host rocks of the collected lithotypes. Microtextures, like interstitial orthopyroxene and clinopyroxene, as well as subhedral to euhedral Cr-spinels are commonly related to melt-rock reactions and refertilisation [48,49]. Such a formation of orthopyroxene and clinopyroxene neoblasts involves two possible reactions, which can describe the formation of the Ol-orthopyroxenite and the websterite, respectively:
forsterite + Si-rich melt → enstatite + Si-poorer melt
forsterite + melt 1 → enstatite + diopside + melt 2
The above reactions commonly involve the formation of an Al-rich phase, which, in the case of the Veria-Naousa pyroxenites, is spinel and have been described in Archean cratons [29,50] or subcontinental mantle regions such as the Lherz Mountains [51], Ronda [11,52,53] and Cabo Ortegal [45,54]. However, quite recently, it was documented that such reactions producing two pyroxenes after dissolution of olivine can also occur in abyssal pyroxenites [55]. Quantification of the melt/rock ratio is a complicated task that involves a number of parameters, such as changes in modal abundances and the trace element compositions of minerals and can be obtained with confidence if an adequate number of samples is available. In the limited samples available in the Veria-Naousa region, we can only provide qualitative estimations and we interpret that the rather rich in olivine Ol-orthopyroxenites indicate a moderate melt/rock ratio whereas the websterite with limited olivine suggest a higher melt/rock ratio, which is compatible with the much higher CaO/Al2O3 ratio in the websterite.
Reaction (1), which causes Si metasomatism, frequently occurs in the mantle wedge. Natural and experimental data reveal that Si-rich melts [56,57], or aqueous [58] or supercritical fluids [59] are released from the underlying subducted oceanic slab into the sub-arc region driving the dissolution of mantle olivine and the neoformation of pyroxenes and Al-phases in a range of pressures between 0.8 and 3.4 GPa [60,61,62,63,64,65,66,67,68]. Experimental results of Grant et al. [69] at 800 MPa suggest that neoblasts of orthopyroxene and clinopyroxene form at a relatively narrow temperature range of around 800 to 900 °C (with few exceptions up to 1100 °C). Topological conditions like the existence of veins and the SSZ geotectonic environment proposed below (see Section 8.2) render the conditions of the studied Veria-Naousa ophiolite comparable to those of Grant et al. [69] and hence, our geothermometric calculations for the Ol-orthopyroxenites are consistent with the calculated temperatures of these authors.
The metasomatic orthopyroxene and clinopyroxene are generally poorer in Al, but richer in Ca relative to porphyroclasts whereas the metasomatic orthopyroxenes are richer in Cr relative to the porphyroclasts in both rock-types. This behaviour of Ca and Cr is not in agreement with other natural examples [61,70,71] and may imply percolation of a melt that was richer in Ca and Cr than the pyroxenite’s precursors. Relic crystals with lobate boundaries and newly-formed, euhedral spinel crystals in Ol-orthopyroxenite show a range of Cr# resembling spinels from both marginal basins and boninitic basalts (Figure 4b–d). This evidence implies that apart from the crystallisation of spinels with boninitic affinities, residual mantle spinels have also been modified by impregnation from a boninitic melt. The mechanisms for formation and transformation of spinels in the upper mantle through a necessary peridotite-melt reaction process were recently reviewed by Arai and Miura [72]. The elevated Mg# of these rocks, as well as their high Cr and low Ti and Al abundances are compatible with an imprint of a boninitic geochemical signature. This hypothesis is in agreement with the enrichments in LREE and HREE in the REE patterns of the Ol-orthopyroxenites, as boninitic melts, which are typically known to fractionate MREE, may have imprinted their REE signature on the investigated rocks (Figure 7). Similar U-shaped REE patterns have been reported and modelled describing the nature of melt/rock interactions in Greek and other ophiolites [73,74,75,76,77]. Several authors have attributed LREE enrichments in ultramafic rocks to secondary events and particularly to serpentinisation (for a review see [78]), however such a hypothesis is less likely, as the Ol-orthopyroxenites are the least altered and no striking LREE enrichments are observed in any of the pyroxenites. The very low Al contents in the neoblastic pyroxenes also support this hypothesis, as experimental data have shown that such crystals form from hydrous melts with a low Al/Si ratio similar to boninites [79].
The websterite is the most LREE depleted pyroxenite showing however HREE contents similar to the Ol-orthopyroxenite. This resemblance points towards a precursor with similar levels of depletion for both rock-types, however the occurrence of clinopyroxene porphyroclasts along with the lower Cr contents in the websterite indicate a more fertile character for its precursor, compatible with its host refractory lherzolite. Both the websterite and Ol-orthopyroxenite show rather elevated CaO/Al2O3 ratios (5.24 and 1.85–2.59, respectively) with nevertheless a much higher ratio in the websterite. This is a strong indication for the involvement of higher amounts of percolating magma in their origin. Furthermore, CaO/Al2O3 ratios higher than 5 have been assigned to the interaction of peridotites with carbonatite magmas [80], which commonly share their origin with ankaramitic magmas. It is known that boninites and ankaramites have similar origins (both with highly magnesian olivine and Cr-rich spinels) but they differ in that boninites include enstatite or bronzite whereas ankaramites involve the crystallization of diopside [81,82]. Thus, the diopside neoblasts further advocate to the incorporation of ankaramitic melts in the evolution of the websterite. It has been documented that such a process may result in depletions of Zr and reduction of Zr/Y ratios [83,84,85] similar to the studied websterite, which shows lower Zr and Zr/Y ratio than the Ol-orthopyroxenite (see Table 5). However, no primary carbonates have been observed that would further support this hypothesis. The high Mg# of the neoblastic pyroxenes suggests crystallisation from a nearly primitive magma, which may also account for the whole-rock high Mg# and Ni of the websterite. High pressure (>1.5 GPa) melting of refractory lherzolites or clinopyroxene-bearing harzburgites is required and can be triggered from variations in the CO2 and H2O contents in the mantle wedge, which may have been fluxed from the subducted Pelagonian sediments [86,87], to produce carbonatitic or picritic-ankaramitic melts [88,89,90]. Ankaramitic melts are highly magnesian as boninites and are produced at around 1300–1350 °C, at 40–70 km depth [90]. The calculated temperature of 1136 °C for the websterite does not contradict such an ascending, percolating melt, which had slightly cooled prior to the interaction with the wall-rock peridotite. Ankaramitic melts are generally enriched in incompatible elements. The low amounts of incompatible elements in the websterite can be explained by the late quantitative imprint by H2O-rich fluids, which are poor in these elements. This is a common process in subarc mantle, as demonstrated by Green et al. [90]. We recommend that these melts may have subsequently differentiated to the boninitic melts, which impregnated harzburgite, perhaps at a higher level, to form the Ol-orthopyroxenite. This is a process similar to what has been proposed for the pyroxenites of Cabo Ortegal [54].
Koloskov and Zharinov [91] have proposed a multivariate statistical diagram of clinopyroxene compositions in ultramafic and mafic rocks discriminating tectonic zones of clinopyroxenes in equilibrium with garnet (zones I and II), spinel (zones III and IV) and plagioclase (zones V, VI and VII). Despite that the statistical treatment has been questioned by Buccianti and Vaselli [92] other authors have tested the validity and argue for the significance of this diagram, even though a precise setting of different clinopyroxene origins may not be well enough established [45]. The analysed clinopyroxenes from both the Ol-orthopyroxenite and the websterite plot in the field of island arc peridotites (Figure 8) with the first being moreover very similar to clinopyroxenes from the Izu Bonin Marianna forearc peridotites. This is compatible with the replacive character of the Veria-Naousa pyroxenites and their genesis in a mantle wedge or sub-arc setting.

8.2. Tectonic Setting

Unzoned pyroxenes occur in the pyroxenites from the Veria-Naousa ophiolite, which may indicate slow cooling during crystallisation. It is believed that the slowly cooling, unzoned minerals are indicative of crystallisation in a high-pressure environment [96]. The existence of highly magnesian olivine, pyroxene neoblasts and the absence of plagioclase are in line with high pressure crystallisation of basaltic melts [97]. Al contents of the clinopyroxenes and orthopyroxenes in both lithologies are compatible with formation in a SSZ regime. The compositions of the magnesiochromites-chromites in the Veria-Naousa pyroxenites vary widely in Cr# and Mg#, and have low TiO2 contents showing affinities similar to boninitic or backarc forming spinels. This evidence is in agreement with the composition of the clinopyroxenes in these pyroxenites that have affinities analogous to crystals from arc peridotites.
The REE patterns of the Ol-orthopyroxenite provide further evidence for their impregnation from boninitic melts (Figure 7). The enriched in Al2O3 and relatively poor Mg# nature of the analysed pyroxenes in the Ol-orthopyroxenites can be explained from the influence of metasomatic impregnation from fluids generated in a supra-subduction zone setting (Figure 4a,c) [98]. The low TiO2 content in the clinopyroxene from websterite and Ol-orthopyroxenite is interpreted as the result of crystallisation from a Ti-poor magma, similar to that typically generated in SSZ settings [6].

9. Conclusions

New occurrences of websterite and Ol-orthopyroxenite have been discovered in the Veria-Naousa ophiolite. The precursor of the websterite is a more fertile clinopyroxene-bearing lherzolite. Geochemical signatures imply that it was formed from the replacement of olivine from two pyroxenes, induced by the channeled flow of a nearly primitive ankaramitic/carbonatitic melt. The Ol-orthopyroxenites are replacive formations after a harzburgitic precursor with the progressive replacement of olivine by orthopyroxene, induced by channelled flow of boninitic melts, perhaps at a higher level than the websterite. The evolution of both the Ol-orthopyroxenite and the websterite is attributed to the mantle wedge of a sub-arc region. We recommend that the occurrence of the pyroxenites record the evolution of the mantle wedge and the opening of a backarc basin in the region of the Axios (Vardar) Ocean in the region of the Veria and Naousa.

Acknowledgments

This work forms part of the PhD study of Aikaterini Rogkala. We thank Cassian Pirard and three anonymous reviewers for their constructive comments, which greatly improved the manuscript. We kindly thank A.K. Seferlis of the Laboratory of Electron Microscopy and Microanalysis, University of Patras for his assistance with the microanalyses and SEM micrographs.

Author Contributions

Aikaterini Rogkala participated in the fieldwork, in the interpretation of the results and wrote the paper; Petros Petrounias participated in the fieldwork, the interpretation of results and performed SEM work; Basilios Tsikouras participated in the fieldwork, the interpretation of the results, coordinated the research and wrote the paper; and Konstantin Hatzipanagiotou participated in the interpretation of results.

Conflicts of Interest

The authors declare no conflict of interest.

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Figure 1. Geological map of the Veria-Naousa region. Inset shows the geotectonic zones of Greece highlighting the Almopias, Paikon and Peonias (from west to east) subzones of the Axios zone; black rectangle shows the study area.
Figure 1. Geological map of the Veria-Naousa region. Inset shows the geotectonic zones of Greece highlighting the Almopias, Paikon and Peonias (from west to east) subzones of the Axios zone; black rectangle shows the study area.
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Figure 2. Textural characteristics of the pyroxenites from the Veria-Naousa ophiolite: (a) photomicrograph of porphyroclastic orthopyroxene (opx) with lesser clinopyroxene neoblasts (cpx2) with irregular shapes in a websterite (sample BE.6; Nicols +); (b) backscattered electron image of subhedral clinopyroxene (cpx) surrounded by neoblastic clinopyroxene (cpx2), as well as secondary serpentine (srp) and magnetite (mgt) in a websterite (sample BE.6; Nicols +); (c) photomicrograph of porphyroclastic orthopyroxene (opx) and subhedral grains of chromite (chr) in an Ol-orthopyroxenite (sample BE.28); (d) photomicrograph of porphyroclastic orthopyroxene (opx) with neoblasts of clinopyroxene (cpx2) and chromite both subhedral and embayed (chr) in an Ol-orthopyroxenite (sample BE.67B, Nicols +); (e) backscattered electron image of clinopyroxene neoblasts (cpx2) in orthopyroxene (opx) in an Ol-orthopyroxenite (sample BE.67); and (f) backscattered electron image of a chromite (chr) with lobate boundaries surrounded by orthopyroxene in an Ol-orthopyroxenite (sample BE.67B).
Figure 2. Textural characteristics of the pyroxenites from the Veria-Naousa ophiolite: (a) photomicrograph of porphyroclastic orthopyroxene (opx) with lesser clinopyroxene neoblasts (cpx2) with irregular shapes in a websterite (sample BE.6; Nicols +); (b) backscattered electron image of subhedral clinopyroxene (cpx) surrounded by neoblastic clinopyroxene (cpx2), as well as secondary serpentine (srp) and magnetite (mgt) in a websterite (sample BE.6; Nicols +); (c) photomicrograph of porphyroclastic orthopyroxene (opx) and subhedral grains of chromite (chr) in an Ol-orthopyroxenite (sample BE.28); (d) photomicrograph of porphyroclastic orthopyroxene (opx) with neoblasts of clinopyroxene (cpx2) and chromite both subhedral and embayed (chr) in an Ol-orthopyroxenite (sample BE.67B, Nicols +); (e) backscattered electron image of clinopyroxene neoblasts (cpx2) in orthopyroxene (opx) in an Ol-orthopyroxenite (sample BE.67); and (f) backscattered electron image of a chromite (chr) with lobate boundaries surrounded by orthopyroxene in an Ol-orthopyroxenite (sample BE.67B).
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Figure 3. Orthopyroxene and clinopyroxene compositions of the Veria-Naousa pyroxenites: (a) CaO vs. Mg# in orthopyroxene; (b) Al2O3 vs. Mg# in orthopyroxene; (c) Al2O3 vs. Mg# in clinopyroxene and (d) Cr2O3 vs. Mg# in clinopyroxene.
Figure 3. Orthopyroxene and clinopyroxene compositions of the Veria-Naousa pyroxenites: (a) CaO vs. Mg# in orthopyroxene; (b) Al2O3 vs. Mg# in orthopyroxene; (c) Al2O3 vs. Mg# in clinopyroxene and (d) Cr2O3 vs. Mg# in clinopyroxene.
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Figure 4. Compositional variations of the spinel-group minerals from the Ol-orthopyroxenites of the Veria-Naousa ophiolite: (a) Cr# vs. Mg# chemical classification diagram; (b) TiO2 vs. Cr# diagram [40,41,42]; (c) Al2O3 vs. TiO2 diagram [43]; and (d) Mg# vs. Cr# diagram (boninite field after [32], MORB, forearc basin and backarc basin fields after [40]).
Figure 4. Compositional variations of the spinel-group minerals from the Ol-orthopyroxenites of the Veria-Naousa ophiolite: (a) Cr# vs. Mg# chemical classification diagram; (b) TiO2 vs. Cr# diagram [40,41,42]; (c) Al2O3 vs. TiO2 diagram [43]; and (d) Mg# vs. Cr# diagram (boninite field after [32], MORB, forearc basin and backarc basin fields after [40]).
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Figure 5. Variations of MgO versus: SiO2 (a); Al2O3 (b); CaO (c); and CaO/Al2O3 (d), for the pyroxenites from the Veria-Naousa ophiolite (recalculated values to 100% on an anhydrous basis). Fields include data from Gravestock [44] and Santos et al. [45] for the Cabo Ortegal pyroxenites and peridotites.
Figure 5. Variations of MgO versus: SiO2 (a); Al2O3 (b); CaO (c); and CaO/Al2O3 (d), for the pyroxenites from the Veria-Naousa ophiolite (recalculated values to 100% on an anhydrous basis). Fields include data from Gravestock [44] and Santos et al. [45] for the Cabo Ortegal pyroxenites and peridotites.
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Figure 6. Variations of MgO versus: Cr (a); Ni (b); Co (c); and Sc (d), for the pyroxenites from the Veria-Naousa ophiolite (recalculated values to 100% on an anhydrous basis). Fields include data from Gravestock [44] and Santos et al. [45] for the Cabo Ortegal pyroxenites and peridotites, Bodinier et al. [11] for the Ronda spinel websterite and lherzolite.
Figure 6. Variations of MgO versus: Cr (a); Ni (b); Co (c); and Sc (d), for the pyroxenites from the Veria-Naousa ophiolite (recalculated values to 100% on an anhydrous basis). Fields include data from Gravestock [44] and Santos et al. [45] for the Cabo Ortegal pyroxenites and peridotites, Bodinier et al. [11] for the Ronda spinel websterite and lherzolite.
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Figure 7. Chondrite-normalized REE patterns of the analysed pyroxenites. Normalising values are after [46].
Figure 7. Chondrite-normalized REE patterns of the analysed pyroxenites. Normalising values are after [46].
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Figure 8. Tectonic discrimination diagram for pyroxenitic clinopyroxenes from the Veria-Naousa ophiolite. Fields I–VII and parameters P1 and P2 are as defined Koloskov and Zharinov [91]: P1 = − 0.02SiO2 + 0.09TiO2 + 0.64Al2O3 + 0.59Cr2O3 + 1.35FeO + 9.65MnO − 0.50MgO + 0.29CaO − 2.26Na2O + 8.0; and P2 = 0.93TiO2 + 0.07Al2O3 + 1.23Cr2O3 − 0.46FeO + 1.74MnO + 0.36MgO + 0.10CaO − 1.66Na2O + 8.0. Fields: I, peridotite xenoliths in kimberlites; II, eclogites and pyrope-bearing pyroxenites in kimberlites; III, spinel peridotites; IV, spinel pyroxenites; V, island arc peridotites; VI, island arc pyroxenites; and VII, plagioclase-bearing xenoliths in volcanic rocks from island arcs. Data sources: island arc and mid-ocean ridges [91]; Izu-Bonin-Mariana forearc [93]; Ronda pyroxenites [94]; Mid-Atlantic Ridge Kane Fracture Zone (MARK area [95]).
Figure 8. Tectonic discrimination diagram for pyroxenitic clinopyroxenes from the Veria-Naousa ophiolite. Fields I–VII and parameters P1 and P2 are as defined Koloskov and Zharinov [91]: P1 = − 0.02SiO2 + 0.09TiO2 + 0.64Al2O3 + 0.59Cr2O3 + 1.35FeO + 9.65MnO − 0.50MgO + 0.29CaO − 2.26Na2O + 8.0; and P2 = 0.93TiO2 + 0.07Al2O3 + 1.23Cr2O3 − 0.46FeO + 1.74MnO + 0.36MgO + 0.10CaO − 1.66Na2O + 8.0. Fields: I, peridotite xenoliths in kimberlites; II, eclogites and pyrope-bearing pyroxenites in kimberlites; III, spinel peridotites; IV, spinel pyroxenites; V, island arc peridotites; VI, island arc pyroxenites; and VII, plagioclase-bearing xenoliths in volcanic rocks from island arcs. Data sources: island arc and mid-ocean ridges [91]; Izu-Bonin-Mariana forearc [93]; Ronda pyroxenites [94]; Mid-Atlantic Ridge Kane Fracture Zone (MARK area [95]).
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Table
Table 1. Representative electron microanalyses of orthopyroxenes from the Veria-Naousa pyroxenites (Porph.: porphyroclast, Neobl.: neoblast, -: below detection limit).
Table 1. Representative electron microanalyses of orthopyroxenes from the Veria-Naousa pyroxenites (Porph.: porphyroclast, Neobl.: neoblast, -: below detection limit).
SampleBE.6-2BE.6-7BE.28-2BE.28-4BE.67-3BE.67-17BE.67-32BE.67B-5BE.67B-6BE.67B-8BE.67B-14
Rock-TypeWebst.Webst.Ol-Orthop.Ol-Orthop.Ol-Orthop.Ol-Orthop.Ol-Orthop.Ol-Orthop.Ol-Orthop.Ol-Orthop.Ol-Orthop.
(wt %)Porph.Porph.Porph.Porph.Porph.Porph.Neobl.Neobl.Neobl.Porph.Porph.
SiO257.3857.2357.8658.5258.1457.1854.6956.8658.1556.6956.99
TiO2-----------
Al2O32.182.610.510.410.870.790.760.820.810.811.40
FeO5.875.456.106.637.187.739.075.545.957.377.38
MnO---0.23-----0.380.34
MgO32.7133.2633.2133.7133.2532.5132.6631.8532.1631.7232.94
CaO1.630.971.270.500.911.272.051.971.621.090.48
Cr2O3---0.29---0.450.450.290.40
Sum99.7799.5298.95100.29100.4099.4898.3297.4999.1498.3599.93
Structural formula units based on 6 oxygens
Si1.9781.9711.9991.9992.0001.9941.9312.0002.0002.0001.976
Aliv0.0220.0290.0010.0010.0000.0060.0000.0000.0000.0000.024
Alvi0.0670.0760.0320.0270.0360.0270.0320.0420.0510.0330.034
Fe3+0.0000.0000.0000.0000.0000.0000.1070.0000.0000.0000.000
Ti0.0000.0000.0000.0000.0000.0000.0000.0000.0000.0000.000
Cr0.0000.0000.0000.0080.0000.0000.0000.0130.0120.0080.011
Mg1.6811.7071.7211.7271.7061.6901.7191.6771.6641.6681.703
Fe2+0.1690.1570.1770.1900.2070.2250.1340.1640.1730.2170.214
Mn0.0000.0000.0000.0070.0000.0000.0000.0000.0000.0110.010
Ca0.0600.0360.0470.0180.0340.0470.0780.0750.0600.0410.018
En88.089.988.588.987.786.184.487.687.786.187.6
Fs8.98.39.110.210.611.511.88.59.111.811.5
Wo3.21.92.40.91.72.43.83.93.22.10.9
Mg#90.991.690.790.189.288.287.791.190.688.588.8
Table
Table 2. Representative electron microanalyses of clinopyroxenes from the Veria-Naousa pyroxenites (Porph.: porphyroclast, Neobl.: neoblast, -: below detection limit).
Table 2. Representative electron microanalyses of clinopyroxenes from the Veria-Naousa pyroxenites (Porph.: porphyroclast, Neobl.: neoblast, -: below detection limit).
SampleBE.6-12BE6-13BE.6-27BE.6-58BE.28-12BE.28-13BE.67-28BE.67-21BE.67B-1BE.67B-4BE.67B-9
Rock-TypeWebst.Webst.Webst.Webst.Ol-Orthop.Ol-Orthop.Ol-Orthop.Ol-Orthop.Ol-Orthop.Ol-Orthop.Ol-Orthop.
(wt %)Neobl.Neobl.Porph.Porph.Porph.Porph.Porph.Neobl.Neobl.Neobl.Neobl.
SiO253.4154.5153.8955.0754.6655.2455.2355.4753.9154.5353.84
TiO2----------0.21
Al2O31.040.871.271.690.950.750.940.971.020.790.68
FeO3.253.251.982.112.142.472.102.312.412.602.35
MnO--------0.030.250.08
MgO18.1417.7522.7624.1317.3517.4417.6817.3117.4818.3717.82
CaO21.9820.9518.0716.8522.3322.8221.9622.4922.6121.3621.75
Cr2O30.690.77-0.610.600.74-0.570.490.510.32
Sum98.5198.1097.97100.5098.0399.4697.9199.1297.9598.4197.05
Structural formula units based on 6 oxygens
Si1.9692.0001.9541.9442.0001.9992.0002.0001.9901.9982.000
Aliv0.0310.0000.0460.0560.0000.0010.0000.0000.0100.0020.000
Alvi0.0140.0380.0080.0140.0500.0380.0640.0570.0350.0330.030
Fe3+0.0000.0000.0380.0250.0000.0000.0000.0000.0000.0000.000
Ti0.0000.0000.0000.0000.0000.0000.0000.0000.0000.0000.006
Cr0.0200.0220.0000.0170.0170.0210.0000.0160.0140.0150.009
Mg0.9970.9731.2301.2700.9500.9440.9660.9370.9621.0040.987
Fe2+0.1000.1000.0220.0370.0660.0750.0640.0700.0740.0800.073
Mn0.0000.0000.0000.0000.0000.0000.0000.0000.0010.0080.003
Ca0.8680.8260.7020.6370.8790.8880.8620.8750.8940.8390.866
En50.751.361.864.550.149.551.049.849.852.051.2
Fs5.15.33.03.23.53.93.43.73.94.53.9
Wo44.243.535.232.446.446.645.646.546.343.544.9
Mg#90.990.795.395.393.592.693.893.092.792.092.9
Table
Table 3. Representative electron microanalyses of olivines from Veria-Naousa Ol-orthopyroxenite (-: below detection limit).
Table 3. Representative electron microanalyses of olivines from Veria-Naousa Ol-orthopyroxenite (-: below detection limit).
SampleBE.28-2BE.28-5BE.28-6BE.28-7BE.28-8BE.28-9
Rock-Type
(wt %)		Ol-Orthop.Ol-Orthop.Ol-Orthop.Ol-Orthop.Ol-Orthop.Ol-Orthop.
SiO241.5542.7342.5541.3442.6241.40
TiO2------
Al2O3------
FeO9.7510.4610.1910.1910.4510.31
MnO------
MgO46.9349.1048.3146.5347.6246.22
CaO------
Cr2O3------
NiO0.460.420.430.250.220.49
Sum98.69102.71101.4898.31100.9198.42
Structural formula units based on 4 oxygens
Si1.0291.0191.0251.0291.0321.030
Al0.0000.0000.0000.0000.0000.000
Ti0.0000.0000.0000.0000.0000.000
Mg1.7321.7451.7361.7261.7191.715
Fe2+0.2020.2090.2050.2120.2120.215
Mn0.0000.0000.0000.0000.0000.000
Ca0.0000.0000.0000.0000.0000.000
Ni0.0090.0080.0080.0050.0040.010
Total2.9702.9802.9702.9702.9702.970
Fo89.689.389.489.189.088.9
Fa10.410.710.610.911.011.1
Table
Table 4. Representative electron microanalyses of spinel-group minerals from the Veria-Naousa Ol-orthopyroxenite (-: below detection limit).
Table 4. Representative electron microanalyses of spinel-group minerals from the Veria-Naousa Ol-orthopyroxenite (-: below detection limit).
SampleBE.28-2BE.28-3BE.28-4BE.28-5BE.28-6BE.67B-9BE.67B-14
Rock-TypeOl-Orthop.Ol-Orthop.Ol-Orthop.Ol-Orthop.Ol-Orthop.Ol-Orthop.Ol-Orthop.
(wt %)ChrChrChrChrChrChrCr-sp
TiO2-----0.05-
Al2O38.989.2811.6411.3811.5910.7020.00
FeO19.7720.0619.6119.4719.5221.6320.59
MnO0.44----0.46-
MgO9.579.4110.1110.8410.778.7211.49
K2O-----0.12-
Cr2O361.6760.0957.8957.4658.9759.4748.72
NiO------0.18
ZnO------0.19
Sum100.4398.8499.2599.15100.85101.15101.17
Structural formula units based on 3 cations
Al0.3510.3680.4520.4410.4420.4100.731
Cr1.6161.5971.5101.4931.5091.5451.195
Fe3+0.0330.0350.0380.0660.0480.0430.074
Ti0.0000.0000.0000.0000.0000.0010.000
2.0002.0002.0002.0002.0002.0002.000
Mg0.4730.4720.4970.5310.5200.4270.531
Ni0.0000.0000.0000.0000.0000.0000.004
Fe2+0.5150.5280.5030.4690.4800.5550.460
Mn0.0120.0000.0000.0000.0000.0130.000
Zn0.0000.0000.0000.0000.0000.0000.004
K0.0000.0000.0000.0000.0000.0050.000
1.0001.0001.0001.0001.0001.0001.000
Cr#82.281.376.977.277.378.962.0
Mg#47.947.249.753.152.043.753.6
Table
Table 5. Representative geochemical analyses of pyroxenites from Veria-Naousa ophiolite (-: below detection limit).
Table 5. Representative geochemical analyses of pyroxenites from Veria-Naousa ophiolite (-: below detection limit).
SampleBE.6BE.28BE.67BE.67B
Rock-TypeWebsteriteOl-orthopyroxenites
Major Elements (wt %)
SiO245.7654.7957.6554.79
TiO20.01-0.020.02
Al2O31.840.661.031.30
Fe2O3t4.347.697.788.57
MnO0.140.160.170.18
MgO28.3930.9629.0130.97
CaO9.641.712.142.40
Na2O--0.02-
K2O----
P2O5----
LOI8.82.91.21.1
Total98.9298.8799.0299.33
Trace Elements (ppm)
Cr2812318829013147
Co66.775.466.469.8
Ni1563.4268.481.3655.0
Cu23.93.23.95.4
Zn221065
Rb0.52.51.71.4
Sr7.719.64.22.6
Y0.40.30.30.2
Zr0.10.30.50.4
Nb0.1--2.1
Pb8.96.11.50.2
Ba4532
V1084592132
Sc20132129
Ga3.23.21.30.6
Hf----
As-0.6--
Hg-0.010.02-
Ta----
Th----
U----
Be-2--
Au (ppb)2.33.32.2-
Rare Earth Elements (ppm)
La-0.50.70.4
Ce-0.30.30.2
Pr-0.020.03-
Nd----
Sm----
Eu----
Gd0.05---
Tb----
Dy---0.09
Ho----
Er0.060.030.030.06
Tm0.01---
Yb0.090.070.060.06
Lu0.02-0.020.01
Mg#87.981.780.680.1
CaO/Al2O35.242.592.081.85
Zr/Y0.251.001.672.00
La/Lu-7.1411.676.67
Table
Table 6. Temperature (T °C) estimates on pyroxenites from the Veria-Naousa ophiolite.
Table 6. Temperature (T °C) estimates on pyroxenites from the Veria-Naousa ophiolite.
SampleBE.6BE.28BE.67BE.67B
Rock-TypeWebsteriteOl-orthopyroxenite
Opx-Cpx thermometry (°C) Wood and Bano [47]1136972974974

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Rogkala, A.; Petrounias, P.; Tsikouras, B.; Hatzipanagiotou, K. New Occurrence of Pyroxenites in the Veria-Naousa Ophiolite (North Greece): Implications on Their Origin and Petrogenetic Evolution. Geosciences 2017, 7, 92. https://doi.org/10.3390/geosciences7040092

AMA Style

Rogkala A, Petrounias P, Tsikouras B, Hatzipanagiotou K. New Occurrence of Pyroxenites in the Veria-Naousa Ophiolite (North Greece): Implications on Their Origin and Petrogenetic Evolution. Geosciences. 2017; 7(4):92. https://doi.org/10.3390/geosciences7040092

Chicago/Turabian Style

Rogkala, Aikaterini, Petros Petrounias, Basilios Tsikouras, and Konstantin Hatzipanagiotou. 2017. "New Occurrence of Pyroxenites in the Veria-Naousa Ophiolite (North Greece): Implications on Their Origin and Petrogenetic Evolution" Geosciences 7, no. 4: 92. https://doi.org/10.3390/geosciences7040092

APA Style

Rogkala, A., Petrounias, P., Tsikouras, B., & Hatzipanagiotou, K. (2017). New Occurrence of Pyroxenites in the Veria-Naousa Ophiolite (North Greece): Implications on Their Origin and Petrogenetic Evolution. Geosciences, 7(4), 92. https://doi.org/10.3390/geosciences7040092

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