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Home All issues Volume 191 (2020) BSGF - Earth Sci. Bull., 191 (2020) 28 Full HTML
2 Geological setting
3 Samples description ...
4 Pressure-temperature estimations ...
5 Zircon U-Pb geochronology
Pressure-temperature conditions and significance of Upper Devonian eclogite and amphibolite facies metamorphisms in southern French Massif central
Évolution pression-température et implications des métamorphismes amphibolitique et éclogitique du Dévonien supérieur dans le sud du Massif central français
Anissa Benmammar1,2, Julien Berger1,a,*, Antoine Triantafyllou3,4, Stéphanie Duchene1, Abderrahmane Bendaoud2, Jean-Marc Baele5, Olivier Bruguier6 and Hervé Diot7,8
1 Géosciences Environnement Toulouse, Université de Toulouse, CNRS, IRD, UPS, Toulouse, France
2 Department of Geology, Université des Sciences et de la Technologie Houari Boumediene, Algiers, Algeria
3 Department of Geology, University of Liège, Sart Tilman, Liège, Belgium
4 Department of Geosciences, University of Arizona, Tucson, USA
5 Department of Geology and Applied Geology, Université de Mons, Mons, Belgium
6 University Montpellier, Géosciences Montpellier, UMR-CNRS-UM2 5243, Place Eugene Bataillon, 34095 Montpellier, France
7 LPGN, UMR-CNRS 6112, Université de Nantes, Nantes, France
8 Université de La Rochelle, La Rochelle, France
* Corresponding author: julien.berger@get.omp.eu
The southwestern French Massif central in western Rouergue displays an inverted metamorphic sequence with eclogite and amphibolite facies units forming the top of the nappe stack. They are often grouped into the leptyno-amphibolite complex included, in this area, at the base of the Upper Gneiss Unit. We sampled garnet micaschists and amphibolites to investigate their metamorphic history with isochemical phase diagrams, thermobarometry and U-Pb zircon dating. Our results demonstrate that two different tectono-metamorphic units can be distinguished. The Najac unit consists of biotite-poor phengite-garnet micaschists, a basic-ultrabasic intrusion containing retrogressed eclogites and phengite orthogneisses. Pressure and temperature estimates on micaschists with syn-kinematic garnets yield a prograde with garnet growth starting at 380 °C/6–7 kbar, peak pressure at 16 kbar for 570 °C, followed by retrogression in the greenschist facies. The age of high pressure metamorphism has been constrained in a recent publication between ca. 383 and 369 Ma. The Laguépie unit comprises garnet-free and garnet-bearing amphibolites with isolated lenses, veins or dykes of leucotonalitic gneiss. Thermobarometry and phase diagram calculation on a garnet amphibolite yield suprasolidus peak P-T conditions at 710 °C, 10 kbar followed by retrogression and deformation under greenschist and amphibolite facies conditions. New U-Pb analyses obtained on igneous zircon rims from a leucotonalitic gneiss yield an age of 363 ± 3 Ma, interpreted as the timing of zircon crystallization after incipient partial melting of the host amphibolite. The eclogitic Najac unit records the subduction of a continental margin during Upper Devonian. It is tentatively correlated to a Middle Allochthon, sandwiched between the Lower Gneiss Unit and the Upper Gneiss Unit. Such an intermediate unit is still poorly defined in the French Massif central but it can be a lateral equivalent of the Groix blueschists in the south Armorican massif. The Uppermost Devonian, amphibolite facies Laguépie unit correlates in terms of P-T-t evolution to the Upper Gneiss Unit in the Western French Massif central. This Late Devonian metamorphism is contemporaneous with active margin magmatism and confirms that the French Massif central belonged to the continental upper plate of an ocean-continent subduction system just before the stacking of Mississippian nappes.
Les unités tectono-métamorphiques du sud-ouest du Massif central français, dans l'ouest du Rouergue, sont structurées selon une séquence métamorphique inverse où les unités du faciès éclogite et amphibolite se situent au sommet de l'empilement des nappes. Ces unités régionales sont généralement incorporées dans le complexe leptyno-amphibolique, formant la base de l'Unité des Gneiss Supérieurs. Suite à une étude comparative de l'histoire métamorphique des unités de Najac et de Laguépie, deux unités tectono-metamorphiques peuvent etre distinguées. L'unité de Najac est composée de métapélites à phengite-grenat pauvres en biotite, d'une intrusion basique-ultrabasique renfermant des éclogites rétromorphosées et des orthogneiss à phengite. Le grenat commence sa croissance vers 380 °C/6–7 kbar, suivi d'un pic de pression à 16 kbar et 570 °C et enfin d'une rétromorphose dans les conditions du faciès des schistes verts. L'âge du métamorphisme de haute-pression a été contraint récemment entre 383 et 369 Ma. L'unité de Laguépie est formée par des amphibolites avec ou sans grenat renfermant des lentilles isolées, des veines ou dykes de gneiss leucotonalitique. Les conditions P-T ont été estimées sur une amphibolite à grenat à 710 °C et 10 kbar pour la fusion partielle suivie d'une rétromorphose et une déformation dans les conditions du faciès des amphibolites et des schistes verts. Les datations U-Pb sur des bordures de zircons d'une veine de gneiss leucotonalitique donnent un âge de 363 ± 3 Ma, interprété comme marquant la cristallisation magmatique des zircons après l'initiation de la fusion partielle de l'encaissant amphibolitique. L'unité de Najac a enregistré la subduction d'une marge continentale au Dévonien supérieur. Elle peut être corrélée à un Allochthone Intermédiaire, compris entre l'Unité des Gneiss Inférieurs et l'Unité des Gneiss Supérieurs. Une telle unité intermédiaire est encore mal définie dans le Massif central français mais elle peut être un équivalent latéral des schistes bleus de Groix dans le Massif Armoricain. L'unité amphibolitique du Dévonien Supérieur de Laguépie est reliée en termes d'évolution P-T-t à l'Unité des Gneiss Supérieurs dans le Massif Central français occidental. Ce métamorphisme du Dévonien tardif est contemporain d'un magmatisme de marge active et confirme que le sud du Massif Central français appartenait à la plaque continentale supérieure d'un système de subduction océan-continent juste avant l'empilement des nappes durant le Mississippien.
Key words: Variscan / Rouergue / HP metamorphism / partial melting
Mots clés : Varisque / Rouergue / métamorphisme HP / fusion partielle
Present address: Géosciences Environnement Toulouse, 14 avenue Edouard Belin, 31400 Toulouse, France.
© A. Benmammar et al., Published by EDP Sciences 2020
This is an Open Access article distributed under the terms of the Creative Commons Attribution License (https://creativecommons.org/licenses/by/4.0), which permits unrestricted use, distribution, and reproduction in any medium, provided the original work is properly cited.
The evaluation of pressure-temperature-time paths in orogenic belts is fundamental to reconstruct the geotectonic evolution before, during and after the orogenesis. Specifically, pre-collisional eclogite and blueschist high-pressure (HP) units formed in the subducting slab (Ernst, 2001) and amphibolite to granulite high-temperature (HT) units belonging to the upper plate (Hydmann et al., 2005) may contain crucial information on the dynamics of pre-orogenic subductions (Brown, 2006). The stacking of these subduction-related HP and HT metamorphic rocks onto greenschist facies units during exhumation and/or collision can lead to the formation of inverted metamorphic sequences (Peacock, 1987) where metamorphic conditions increase upward in the tectonic stack and where the boundary between units is marked by localized deformation and sharp contrasts in metamorphic conditions.
Pioneer studies on the Variscan French Massif central (FMC) showed that pre-Visean metamorphic units have a complex tectonic distribution (see Burg et al., 1984, 1989; Ledru et al., 1989, 1994; Santallier et al., 1994; Faure et al., 2005, 2009; Lardeaux, 2014; Lardeaux et al., 2014), with greenschist facies units forming the lowermost and uppermost parts of the tectonic pile (the para-autochthon and the so-called epizonal units, respectively). Amphibolite facies units locally preserving relic of eclogites and HP granulites rocks are classically grouped into the Lower Gneiss Unit (LGU) and the Upper Gneiss Unit (UGU) in the French Massif central (see Bellot and Roig, 2007) but investigations on the neighboring Armorican massif (Bosse et al., 2000, 2005; Ballèvre et al., 2009; Pitra et al., 2010; Ballèvre et al., 2014) pointed out the existence of a Late Devonian ophiolitic and eclogite/blueschist-bearing Middle Allochthon sandwiched between the upper and lower units. Berger et al. (2010a, 2010b) proposed to introduce a Middle Allochthon in the FMC located between LGU and UGU and composed of HP to UHP eclogites with host orthogneiss and micaschists but also of ophiolites marked by a post-oceanic equilibration in the granulite facies (Santallier et al., 1994; Berger et al., 2010b). This subdivision, still immature for the French Massif central, group together rocks with contrasted metamorphic evolutions. More detailed metamorphic petrology studies are thus needed to propose a better scheme of subdivision and coherent geodynamic interpretations. Furthermore, this metamorphic organization is not integrated in the most recent compilations on the metamorphic evolution of the French Massif central (Faure et al., 2009; Lardeaux, 2014) in which most HP metamorphic rocks are included within the Upper Gneiss Unit encompassing the enigmatic leptyno-amphibolite complex (Santallier et al., 1988). The latter is defined as a bimodal association of felsic and mafic gneisses frequently containing relics of eclogite and granulite facies rocks and often located at the base of UGU, sometimes in LGU. These apparent conflicting views are, on the one hand due to the poor quality of exposures in the French Massif central, and on the other hand to the lack of detailed quantitative metamorphic studies coupled to petrochronological investigations that are to propose robust pressure-temperature-time (P-T-t) paths.
Recent dating performed on eclogites from Southern Massif central yielded Upper Devonian to Lowermost Carboniferous ages (Lotout et al., 2018, 2020) while the HP metamorphism and the closure of oceanic domains in the French Massif central are classically considered to be around 410–390 Ma (Eo-varican cycle or D0 event of Faure et al., 2009; see also Lardeaux, 2014). Ages of HP metamorphism published between 1980 and 2000 have to be re-evaluated (Paquette et al., 2017) and, more generally, petrochronological data on metamorphic units are required to better constrain the Devonian evolution of the French Massif central. These data are crucial to determine if the West European Variscan belt is polycylic and marked by two phases of convergence and ocean closure (Faure et al., 2005, 2008, 2009; Lardeaux, 2014) or monocyclic with a single event of continental collision (Ballèvre et al., 2009) or somewhere between the two endmembers models.
This paper addresses the question of the subdivision of amphibolite and eclogite facies metamorphic units and their geological meaning in southern French Massif central near Najac in Western Rouergue (Burg et al., 1984, 1989). According to most authors, the metamorphic units in this area are thought to belong to the leptyno-amphibolite complex and are often integrated into the UGU (Lardeaux, 2014; Lotout et al., 2018). Our study shows that their constitutive rocks display contrasted P-T-t-d histories. Therefore, we provide new P-T estimations on phengite-garnet micaschists from Najac and on migmatitic amphibolites from Laguépie. These results are coupled to U-Pb zircon dating in the latter unit and interpreted considering the new and robust multi-method ages provided by Lotout et al. (2018) on an eclogite from Najac.
The Variscan French Massif central consists of several tectono-metamorphic units that were stacked before the Visean (see Faure et al., 2009; Lardeaux, 2014). Despite the poor quality of their exposures, the metamorphic units are well defined on geological maps and in the literature in Limousin, Haut-Allier and Rouergue domains (Dubuisson et al., 1988; Ledru et al., 1989; Ledru et al., 1994; Burg et al., 1989a). This stack is characterized by an apparent inverse metamorphic gradient, with amphibolite facies and eclogite facies units (Lower Gneiss and Upper Gneiss Units; LGU and UGU, respectively) commonly lying above greenschist units (Para-Autochthon; see Burg et al., 1984; Lardeaux, 2014). At the scale of the French Massif central, the pre-Carboniferous tectono-metamorphic evolution is subdivided into three phases following (Faure et al., 2005, 2008, 2009, 2017): D0 represent the Late Silurian/Early Devonian (420–400 Ma) HP metamorphic phase; D1 relates to amphibolite facies migmatitization in LGU and UGU associated with a top-to-the-southeast kinematics, it occurred during Middle and Upper Devonian (385–375 Ma); D2 (360–350 Ma) is marked by top-to-the-northwest kinematics under amphibolite facies conditions. However, recent petrochronological investigations performed by Lotout et al. (2018, 2020) yielded Upper Devonian to Early Carboniferous ages for HP metamorphism in southern French Massif central (Najac and Lévézou). These new findings suggest that the D1 and D2 phases as defined by Faure et al. (2009) are also contemporaneous with formation and exhumation of eclogites in southern French Massif central.
Outcrops of the Viaur and Aveyron valleys near Najac and Laguépie were described in details by Collomb (1970), Bodinier and Burg (1981) and Burg et al. (1984). The para-autochthon consists of greenschist facies metapelites (chlorite-muscovite ± biotite bearing) with rare intercalation of felsic, often meta-volcanic, orthogneiss (Fig. 1). The Lower Gneiss Unit is separated from the para-autochthon by a low angle mylonitic shear zone. It is made of orthogneiss representing former felsic plutons with rare lenses of amphibolite facies biotite-muscovite ± garnet metapelites. The contact with the Najac-Carmaux unit is not well exposed but it is interpreted as a thrust contact considering that the latter contains eclogite facies rocks that were not found in the Lower Gneiss Unit (see Burg et al., 1984). The Najac-Carmaux klippe as defined by Burg et al. (1984) consists of an association of phengite-rich micaschists (often garnet-bearing, with minor amounts of biotite and locally accompanied by chloritoid and staurolite; Delor et al., 1987), phengite-bearing porphyroclastic orthogneisses and basic-ultrabasic complexes known as the Najac and Laguépie massifs (Delor et al., 1986; Bodinier et al., 1986; Lotout et al., 2018). Bodinier and Burg (1981) and Bodinier et al. (1986) interpret the eclogitic layered intrusion south of Najac as a former laccolith that intruded the precursor of micaschists and orthogneiss prior to high-pressure metamorphism. We observed small (max 10 cm width) xenolithic fragments of phengite orthogneiss included into eclogite facies metagabbros south of Najac, close to Mergieux. This supports the conclusion considering the Najac basic-ultrabasic massif as a former intrusion within the orthogneiss. Bodinier and Burg (1981) and Bodinier et al. (1986) also noted that the Najac eclogitic basic-ultrabasic massif and the Laguépie amphibolite recorded distinct metamorphic histories but so far, no metamorphic studies have been performed on the amphibolites.
Hereafter, the phengite micaschists, the phengite orthogneiss and the eclogitized basic-ultrabasic intrusion cropping out south of Najac will be grouped into the Najac unit because they display a similar metamorphic evolution (Fig. 1; Burg et al., 1984; this study). The amphibolite massif west of Laguépie, devoid of HP mineral assemblage and showing evidence for incipient partial melting will compose the Laguépie unit. Both are either included within (1) the Najac-Carmaux klippe/unit by Burg et al. (1984) and tentatively correlated to the Groix and Bois de Céné units in the Armorican massif (Delor et al., 1986), or (2) following Lardeaux (2014) and Lotout et al. (2018) they are part of the Leptyno-Amphibolite Complex (LAC) at the base of the Upper Gneiss Unit (Santallier et al., 1994; Lardeaux, 2014). The Laguépie unit is bounded by normal and strike-slip faults, its position within or relative to the Najac unit remains unclear but the normal faults suggest it was structurally located above the Najac unit.
Metamorphic foliations in the Viaur and Aveyron valleys are dipping to the east (20–70° dip) except in the eastern part of the map (Fig. 1). They are affected by small scale overturned N-S folds with an axial plane facing west. Stretching lineations are generally trending N350 with low plunges (<10°). Asymmetric criterion for sense of shear are well expressed along the mylonitic band separating the para-autochthon and the Lower Gneiss Unit is top-to-the-north (D2 phase of Faure et al., 2009). The eclogitic orthogneisses and micaschists of the Najac unit also carry a N280–300-trending stretching lineation with top-to-the-southeast kinematics (deduced from C/S structures and asymmetric feldspar porphyroclasts in orthogneisses).
Northeast of Najac, the whole metamorphic massif is intruded by the Carboniferous Villefranche de Rouergue granodioritic pluton (Burg et al., 1989b). It is bounded by the Villefranche fault to the west, which separates the metamorphic units from the large Permian to Mesozoic Quercy basin and it is unconformably overlain by Permian and Cenozoic deposits to the south.
Geological setting of the Najac and Laguépie units: (a) geological map modified after Burg et al. (1989a). The red arrows indicate the kinematics deduced from C'/C/S structures; (b) interpretative W-E cross section with indication of lithology and metamorphic facies for each unit.
3 Samples description and mineral chemistry
In order to compare the metamorphic evolution of Najac and Laguépie units, we focus our study on several samples of phengite-garnet micaschists surrounding the basic-ultrabasic complex and on amphibolites and associated leucotonalitic gneisses at Laguépie. The orthogneisses around Najac are deformed but their mineral assemblage did not fully reequilibrate during metamorphism (except for some late kinematic Si-rich white micas); these samples were consequently disregarded in this study.
3.1 The Laguépie unit
Samples were collected in an abandoned quarry along the Aveyron valley, west of Saint Martin de Laguépie. The amphibolites are homogeneous amphibole-plagioclase rocks alternating with discontinuous leucotonalitic orthogneisses forming isolated lenses (several millimetres to 20 cm in width) (Fig. 2a). In the eastern side of the quarry, one outcrop exposes discontinuous and rounded levels of melanocratic garnet amphibolite wrapped into large veins of leucogneiss. Contacts between both lithologies can be either sharp or lobed, occasionally resembling cauliflower structures in migmatites (Burg and Vanderhaeghe, 1993) (Fig. 2b–d). The leucogneiss locally cuts across the melanocratic levels and it can also forms deformed lenses within the amphibolites (Fig. 2c). These observations suggest that the unconnected felsic lenses were formed in situ in the amphibolites while large felsic veins or dykes containing lobed fragments of garnet amphibolites are the results of melt drainage and segregation. Accordingly, these field observations suggest that the precursor leucotonalitic magma formed after incipient partial melting of the amphibolite.
The most common lithology of the Laguépie unit is an amphibolite made of amphibole, plagioclase and quartz. Plagioclase is commonly cloudy due to advanced sericitization and frequently contains epidote neoblasts (Fig. 3a, b). Amphibole porphyroclasts are pleiochroic from blue-green to brownish and small needles of light colored green amphibole are found at the contact with plagioclase (Fig. 3a, b). Quartz is common, but never exceed 10 vol.%. The texture is porphyroclastic with oblique localized cataclastic shear bands consisting of crushed chlorite, actinolite and albite grains (Fig. 3a). Secondary calcite and pyrite-chlorite veins cut across plagioclase and amphibole with aligned euhedral pyrite crystals is also commonly observed.
Garnet amphibolite levels consist of a mineral assemblage of plagioclase-amphibole-garnet ± titanite ± quartz ± k-feldspar with large (up to 3 cm width), subrounded, pre-kinematic porphyroclastic garnet rich in quartz inclusions (Fig. 3c). Elongated porphyroclasts of amphibole and plagioclase alternating with rare quartz ribbons define a foliation wrapping the garnet (Fig. 3c). Titanite, apatite, zircon and pyrite are the most common accessory phases. Retrogression is evidenced by the cloudy aspect of plagioclase, the development of light-colored amphibole needles rimming large brownish porphyroclastic grains, growth of chlorite within fractures cutting across garnet and thin cataclastic shear bands made of chlorite, albite and epidote.
Leucotonalitic gneisses consist of an assemblage of quartz-albite-chloritized biotite ± K-feldspar ± garnet and display an augen texture (Fig. 3d) with large porphyroclastic feldspars. Garnet are rounded and small (<1 cm) compared to those observed the amphibolite layer. Their modal abundance usually decreases from the contact with the amphibolite to the core of the leucocratic orthogneiss vein. Chlorite, probably replacing a former biotite, forms elongated domains aligned along the foliation or C−C' shear bands indicating a top-to-the-north sense of shear.
One amphibolite sample (LAG3b) and one garnet-amphibolite sample (AJAH08), collected close to a leucotonalitic vein, were analysed for their mineral composition. The garnet-free amphibolite LAG3b is made of oligoclase (XAn: 0.13–0.17) with albitic rims (XAn: down to 0.07). Amphibole appears as large brown-green crystals characterized by low-Ti (0.94–1.25 wt% TiO2) magnesiohornblende (Mg#: 54–55, Si: 6.72–6.78 a.p.f.u., Fig. 4a) core surrounding Si-rich and Ti-poor thin rim (6.84–7.09 Si a.p.f.u.; 0.33–0.69 wt% TiO2 Fig. 4a). Unaltered plagioclase grains in the garnet amphibolite AJAH08 are more calcic (XAn: 0.30–0.32) while altered grains are albitic (XAn: 0.07–0.10). The amphibole is also a low Ti (0.73–1.05 wt% TiO2) tschermakite (Si 6.24–6.41 a.p.f.u., Mg#: 51–54, Fig. 4a), with thin magnesiohornblende rims (Si up to 6.78 a.p.f.u., Fig. 5a). A discrete chemical zoning was evidenced in a large garnet porphyroclast varying from Alm55-Spss4Prp12Grs29 to Alm58Spss2Prp14Grs25 (Fig. 4b). Amphibole inclusions into garnet show the same tschermakitic composition as the ones forming the matrix.
Main macroscopic features of the Laguépie unit: (a) field photographs of leucotonalitic lenses into garnet-free amphibolite (AJAH9; 1,9558°E, 44,1485°N); (b) polished section of a garnet amphibolite within a quartz-feldspar-chlorite leucogneiss (AJAH8; 1,9602°E; 44,1468°N); (c) outcrop image of the complex relationship between garnet amphibolite lenses and leucotonalitic veins (1,9602°E; 44,1468°N). Note the crosscutting relationships and the cauliflower-like structure at the leucogneiss/amphibolite contact; (d) sketch of the outcrop image shown in (c).
Photomicrographs of representative samples from the Najac and Laguépie units. Laguépie samples: (a) amphibole-plagioclase-ilmenite amphibolite LAG3b representing the dominant lithology of the Laguépie amphibolite (1,9558°E, 44,1485°N); (b) chlorite-epidote-albite shear band oblique to the main foliation and indicating a top to the north sense of shear (sample LAG3b); (c) garnet amphibolite AJAH08 with foliation molded around the garnet porphyroclast; (d) leucogneiss from sample AJAH08 showing a porphyroclastic augen texture. Note the C/S structure marked by chlorite formed after soldification and cooling of the leucotonalitic orthogneiss; (e) Representative texture of the Najac unit garnet-phengite micaschists (sample NJC12a; 1.9754°E, 44,2159°N). Note the pressure shadows filled with biotite and phengite around garnet indicating that the high pressure assemblage is syn-kinematic. Greenish chlorite partly replaces garnet and biotite in all samples; (f) large porphyroclastic snowball and skeletal garnet from sample NJC11 (1,9693°E; 44,2196°N), again showing that the high-pressure mineral assemblage developed during deformation.
Minerals compositions in the amphibolites from the Laguépie unit: (a) amphibole composition in the classification diagram by Leake et al. (1997); (b) garnet compositions in AJAH08.
Minerals composition in the micaschists from the Najac unit: (a) Si versus Fe+Mg diagram for white micas showing the phengitic substitution; (b) garnet zoning profile in NJC11; (c) garnet composition for three representative samples (NJC8, NJC11 and NJC12a).
3.2 Micaschists of the Najac unit
Micaschists of the Najac units are homogeneous light gray-blue rocks displaying a penetrative planar fabric with poorly defined mineral lineation. Granoblastic and elongated quartz and plagioclase form millimeter-scale layers alternating with phengite-rich bands (Fig. 3a). Biotite is present in low volumetric proportions but is preferentially concentrated at the contact between garnet and white mica (Fig. 3e). In most samples, garnet forms minute (< 300 μm in diameter) subhedral grains within the phengitic layers and show pressure shadows filled with biotite and phengite (Fig. 3e). Garnet is rich in quartz and rutile inclusions sometimes delineating a foliation that can be parallel or oblique to the main planar fabric. NJC08 contains centimetric syn-kinematic fibrous snowball garnet porphyroblasts with quartz inclusions and enclosed into phengite stacks (Fig. 3f), substantiating that garnet growth occurred during deformation. Accessory minerals consist of rutile (partly transformed into ilmenite), apatite and zircon.
Garnet chemical zoning is obvious in sample NJC11 where compositions range from Alm41Spss27Prp2Grs30 in the core to Alm66Spss4Prp5Grs25 in the rim (Fig. 5b), while its Fe# decreases from core to rim (96 to 92). Garnet in NJC12a shows a more homogenous composition with core at Alm68Spss4Prp6Grs22 and a rim at Alm72.5Spss1.5Prp7Grs19 at nearly constant Fe# (91–93). White micas are phengitic with Si (per formula unit, on the basis of 11 oxygens) ranging from 3.30 to 3.40 in NJC08, 3.18 to 3.36 in NJC12a and 3.17–3.35 in NJC11; and Fe+Mg (a.p.f.u.) between 0.20 and 0.45. Phengite crystals with the lowest Si content are found close to biotite and in the rim of large grains. Biotite has generally low Ti (0.09–0.11 a.p.f.u) with Mg# varying from 0.45 and 0.50 and low Si (2.70–2.80 a.p.f.u.) in the three analyzed samples. Plagioclase is an oligoclase with XAn comprised between 0.14–0.16 in NJC11 and NJC12a.
4 Pressure-temperature estimations
4.1 Amphibolites from the Laguépie unit
Garnet amphibolite AJAH08 collected in the outcrop shown in Figure 2c, d was selected for detailed thermobarometric investigations because it contains garnet, a good tracer to recover P-T conditions. The sample's bulk composition has been calculated using modal proportions (estimated by pixel counting on thin section images) and core composition of unaltered rock forming minerals (garnet, amphibole, plagioclase, titanite and quartz). Two different estimations were made and the results were differing by less than 5% (relative) on the different oxides proportions. Phase diagrams were calculated with Perple_X (Connolly, 2009) in the system Na2O-CaO-FeO-MnO-MgO-TiO2-Al2O3-SiO2-H2O. Water content has been estimated on the basis of the modal proportion of amphiboles, considering they contain approximately 2 wt% H2O. The calculation uses the thermodynamic database of Holland and Powell (2011, update ds62) and solid solution models adapted for amphibolite to granulite facies mafic rocks (see Green et al., 2016). Ferric iron was not considered because its content in minerals (estimated by stoichiometry) is very low and no oxides containing ferric iron were observed. The mineral assemblage observed in the garnet amphibolite AJAH08 (plagioclase-amphibole-garnet ± titanite ± quartz) cannot be reproduced in the isochemical phase diagram because the calculation systematically predicts the presence of small amounts (<4 vol.%) of clinopyroxene in fields where amphibole, garnet and plagioclase are stable. This can be a consequence of retrograde metamorphism that has transformed clinopyroxene into amphibole or inaccuracies of the calculated model. Garnet, plagioclase, amphibole, quartz and titanite without orthopyroxene, epidote, ilmenite or rutile coexist between 8 and 14 kbar and 600 and 740 °C (Fig. 6). XAn and Mg# isopleths for plagioclase and amphibole, respectively, cross between 8 and 10 kbar at 600–700 °C in fields where low amounts of clinopyroxene are predicted (<4 vol.%) (Fig. 6). The overlapping zone of various garnet isopleths (Fe#, grossular, spessartine contents) yields P-T conditions of 710 ± 15 °C and 10 ± 1 kbar (Fig. 6). As the garnet cores display higher Fe# (up to 84) and grossular content (up to 29 mol%) compared to the rim (Fe# down to 80 and 26 grossular mol%), the slight zoning observed in garnet could trace a small increase in temperature from 690 to 730 °C at nearly constant pressure (Fig. 6). This P-T domain locates close to the ilmenite-titanite and ilmenite-rutile phase transitions but also clinopyroxene (<4 vol.%) and melt present (<2 vol.%) fields (Fig. 6); consequently, it lies above the vapor-present solidus calculated for the amphibole-plagioclase-ilmenite amphibolite LAG3b. It is worth to note that the calculated phase diagram closely reproduces the observed modal proportion of garnet (7 vol.%) around 700 °C and 10 kbar.
Application of garnet-amphibole-plagioclase-quartz barometry (Kohn and Spear, 1990) with hornblende-plagioclase thermometry (Holland and Blundy, 1994) yields 640–700 °C, 8–9 kbar. LAG3b plagioclase amphibole pairs yield similar albeit slightly lower temperature conditions of 640–680 °C at a fixed pressure of 9 kbar. The magnesiohornblende and albitic rims in AJAH08 equilibrated at lower temperature (480–560 °C).
Isochemical phase diagram built for the bulk composition of the garnet amphibolite in sample AJAH08 of the Laguépie unit: (a) phase diagram also showing the isopleth for XAn in plagioclase and Mg# of amphibole (corresponding to composition determined with the electron microprobe). The small triangles represent the results of garnet-amphibole plagioclase-quartz thermobarometry; (b) Fe#, grossular and spessartine isopleths in garnet corresponding to composition measured by electron microprobe. Also shown is the vapor-saturated solidus for the amphibolite LAG3b.
4.2 Micaschists from the Najac unit
Sample NJC11 and NJC12a were selected for isochemical phase diagram calculations. They were calculated in the system Na2O-K2O-FeO-MnO-MgO-TiO2-Al2O3-SiO2-H2O using the Holland and Powell (1998) thermodynamic database revised in 2002, with solid solution models from Tajcmanova et al. (2009) for biotite, Newton et al. (1980) for plagioclase, Holland and Powell (1998) for garnet, Coggon and Holland (2002) for white mica, Holland and Powell (1998) for chlorite. We ignored ferric iron because calculated Fe3+ in silicates (by charge balance or stoichiometry) is systematically very low and Fe3+ bearing oxides are absent. Before drawing the isochemical section using the bulk rock composition measured by XRF spectrometry (CAF service, Stellenbosch University, South Africa), we tested different bulk water content using T-X sections because calculated pyrope content in garnet is extremely sensitive to bulk rock H2O content. The best results, i.e. convergence of garnet isopleths and reproduction of the observed mineral assemblages, were obtained with the H2O content calculated using the micas modal proportion and considering a H2O content of ∼5 wt% in white mica.
Garnet in NJC11 preserved a well-developed bell shaped Mn profile. Core composition (spss: 27mol% and Fe#: 96) are in equilibrium in greenschist facies conditions (360–400 °C, 6–7 kbar) slightly above the garnet-in phase boundary in a field where muscovite, biotite, plagioclase, garnet, titanite and rutile are in equilibrium (Fig. 7a). Intermediate compositions between core and rim draw a linear prograd path passing at 420 °C/8 kbar and 460 °C/12 kbar. Garnet rims equilibrated at 510 ± 20 °C and 14 ± 1 kbar in a field where phengitic mica, biotite, plagioclase, garnet, quartz and rutile are stable with minor amounts of sodic amphibole and clinopyroxene (Fig. 7a). Computed modal proportion for garnet and biotite are low (<6 vol.% and <10 vol.%, respectively). Isopleths of Si content in phengite (3.20–3.35 p.f.u.) and of Fe# in garnet (93–94) cross at 510 ± 30 °C and 15 ± 2 kbar.
The field corresponding to the high-pressure assemblage observed in NJC12a (phengite-quartz-biotite-garnet-plagioclase-rutile) lies within 500–570 °C and 13–16 kbar under vapor under-saturated conditions (Fig. 7b). Free H2O coexist with the observed assemblage at higher temperatures. At higher pressure conditions, the formation of sodic amphibole and pyroxene appears as a result of plagioclase and biotite breakdown while titanite is stable below 13–14 kbar and 520–560 °C (Fig. 7b). Calculated Fe# in garnet is temperature sensitive. Measured values (90–92) correspond to temperatures ranging between 520 and 585 °C for 10 and 20 kbar of pressure (Fig. 7b). These isopleths cross those representing measured Si content in white mica (3.18–3.36 a.p.f.u.) in a narrow P-T domain centered at 570 ± 15 °C and 16 ± 1 kbar (Fig. 7b). Our calculation predicts minor amounts of sodic pyroxene and amphibole (<10 vol.%), despite these ones were not observed in any micaschist samples. It can be due to retrogression of these phase or to inaccuracies of the thermodynamic calculations. Calculated grossular content in this P-T domain (0.20–0.28, increasing with decreasing pressure) is slightly above those determined with electron-microprobe (0.18–0.22). The pressure conditions at which measured and calculated grossular content are overlapping (0.20–0.22) are around 17 kbar. Low-Si (2.72–2.78 a.p.f.u.) biotite with Mg# of 45–48 and Ti between 0.10 and 0.11 p.f.u. is in equilibrium between 460–520 °C and 2–7 kbar (Fig. 7b); this is consistent with the presence of chlorite in the retrograde assemblage and the higher modal amounts of biotite calculated in greenschist facies conditions (around 16 vol.%) compared to eclogitic conditions (<10 vol.%). Biotite stable in the eclogite facies has much higher calculated Si content (>2.90 a.p.f.u.), compositions that were not observed in our samples.
Isochemical phase diagrams computed for compositions corresponding to garnet micaschists from the Najac unit: (a) sample NJC11 used to determine the prograde P-T path; (b) sample NJC12a used to determine the peak P-T conditions and the retrograde path. Garnet in/out and chlorite in/out curves are indicated in bold to better localize the retrogression in greenschist facies conditions.
The age of high-pressure, low temperature metamorphism in the Najac eclogite has been recently determined by multi-method geochronology (prograde path at 385–383 Ma, HP peak at 377 ± 3 Ma, exhumation around 369 ± 13 Ma; Sm-Nd and Lu-Hf isochron plus U-Pb zircon and apatite dating by Lotout et al., 2018) but the age of amphibolite facies metamorphism in the Laguépie amphibolite has not been constrained. A large leucotonalitic lens (AJAH09, 20 × 30 cm) included into the amphibolite was sampled, from which about 40 zircon grains were extracted using heavy liquids and magnetic separation techniques at the Geosciences Environnement Toulouse laboratory.
Zircon images were acquired using a cold-cathode optical cathodoluminescence (CL) at the University of Mons using a Cambridge Image Technology model 8200 Mk5 system. They are generally small (length <200 μm), with minute quartz and apatite inclusions. These zircons show two different textures (Fig. 8a):
cores of subhedral elongated grains or crystal fragments with dark shade (CL or transmitted light) displaying chaotic or no zoning and being often cracked with fractures extending into the rims. These features are typical of metamict zircons (Corfu et al., 2003);
luminescent part, often light brown and translucent, riming the dark cores and showing oscillatory growth zoning. These rims are usually 15 to 50 μm large and are relatively rare compared to dark zircon cores. These luminescent rims were also found as isolated fragments.
U-Pb analyses were performed at Géosciences Montpellier (University of Montpellier, France) using a Teledyne G2 excimer laser probe coupled to a ThermoFinnigan Element XR high-resolution ICP-MS (AETE-ISO regional facility of the OSU OREME). The probe was set at 25 μm diameter, with an ablation frequency of 4 Hz and a fluency of 6 J/cm2. More details on analytical setup can be found in Bosch et al. (2011). Unknowns were calibrated against zircon 91500 standard reference material and GJ-1 was used as secondary standard (both reference materials were analyzed before and after each 5 unknowns). U-Pb ages and common Pb corrections were calculated using the IsoplotR code by Vermeesch (2018). Twelve analyses of GJ-1 zircon yield an upper intercept of 605 ± 14 Ma with 606 ± 7 Ma and 598 ± 5 Ma for the average 207Pb/235U and 206Pb/238U ages, respectively. This is in good agreement with the recommended values, i.e. an upper intercept of 608.5 ± 1.5 Ma calculated from slightly discordant ID-TIMS analyses (Jackson et al., 2004).
Dark metamict cores are U-rich (often >1000 ppm and up to 4650 ppm) and yield strongly discordant U-Pb ellipses (Fig. 8b; Tab. 1). The ablation spectra were moreover irregular and consequently, none of the analyzed zircon cores were used to calculate an age. About 15 spots were shot in the luminescent zoned rims but only 9 were not contaminated by the U-rich metamict cores or by apatite inclusions in depth (evidenced by irregular ablation spectra and/or a continuous increase in U or Pb count rates). These analyses show regular ablation spectra for the 206Pb/238U ratios (i.e. comparable to those of reference zircons 91500 and GJ-1) but more irregular ones for those involving 207Pb. U contents range between 420 and 1044 ppm and Th/U ratios (Tab. 1) are on average slightly higher (0.02–0.04) compared to cores (Th/U: 0.01–0.02 with one analysis at 0.04). The data are discordant (1 to 14% of discordance, 4 ellipses are overlapping Concordia) with 206Pb/238U ages ranging between 356 ± 9 Ma and 374 ± 9 Ma and 207Pb/235U ages between 370 ± 12 Ma and 419 ± 14 Ma. Age calculation using a discordia regression line for rim analyzes yields a lower intercept at 363 ± 3 Ma (MSWD = 2) (Fig. 8c). The weighted average of 206Pb/238U common Pb corrected age is slightly older at 365 ± 3 Ma (Fig. 8d; Tab. 1).
Results of U-Pb zircon dating for leucogneiss AJAH09 of the Laguépie unit: (a) CL images showing the texture of zircon with dark resorbed metamict cores and luminescent oscillatory zoned rims. Some representative spots made on rims are indicated with their 206Pb/238U age; (b) Concordia diagram showing all the U-Pb analyses. Color range corresponds to Th/U ratio values. The rim data are the sub-concordant ellipses just below 400 Ma; (c) regression of rim U-Pb data in a Tera-Wasserburg plot; (d) weighted average of 206Pb/238U common lead corrected ages obtained in zircon rims.
Results of U-Pb zircon dating on leucogneiss sample AJAH09.
6.1 Two distinct tectono-metamorphic units with contrasted P-T paths
The Najac and Laguépie units are grouped into a single tectono-metamorphic unit by different authors (Burg et al., 1984, 1989; Lardeaux, 2014; Faure et al., 2017; Lotout et al., 2018) but we show hereafter that they display different metamorphic histories and ages.
The Najac unit encompasses the eclogitic basic-ultrabasic massif, the phengite-bearing orthogneiss and the phengite-garnet micaschists (Fig. 1). Micaschists record early garnet nucleation around 360–400 °C, 6–7 kbar (Fig. 7a) followed by syn-kinematic growth (Fig. 7a) and equilibration of garnet rims and phengite around 510–570 °C and 14–17 kbar (∼340 °C/GPa) in the eclogite facies (Fig. 7a, b). Late- to post-kinematic biotite and chlorite developed preferentially around garnet (Fig. 7b) and are indicative of retrogression in the greenschist facies at 460–520 °C and 2–7 kbar (Fig. 7b). Lotout et al. (2018) obtained slightly higher peak conditions for an eclogite from the basic-ultrabasic Najac massif (600 °C, 18 kbar; Fig. 9) but similar thermal gradient at peak pressure (330 °C/GPa) (Fig. 9). Multi-methods dating performed by Lotout et al. (2018) on an eclogite from Najac constrained the age of prograde evolution around 383–385 ± 3 Ma and the pressure peak at 377 ± 3 Ma (Fig. 9). The P-T path determined for the Najac unit (Fig. 9) is different than those determined for the paragneisses and micaschists of the Lower Gneiss and Upper Gneiss units in Limousin and French Massif central (Bellot and Roig, 2007; Faure et al., 2009; Lardeaux, 2014; Do Couto et al., 2016), both showing pervasive recrystallization in the amphibolite facies (600–700 °C, 5–10 kbar) during Devonian D1 and D2 events (Faure et al., 2009).
The Laguépie unit comprises garnet-bearing amphibolite, garnet-free amphibolite and a leucotonalitic orthogneiss forming isolated lenses and, sporadically, veins and dykes within amphibolites (Fig. 2). The isolated, unconnected leucotonalitic lenses, the lobed contact between the garnet amphibolite and the leucotonalite magma as well as the sodic nature of the felsic material support that it formed after partial melting of the amphibolite. Garnet in the amphibolite sample AJAH08 preserves core to rim zoning attesting for isobaric (∼10 kbar) heating from 690 to 730 °C (Fig. 6). The main plagioclase-garnet-amphibole-quartz-ilmenite-melt assemblage equilibrated around 700–730 °C at 10 ± 1 kbar. (∼720 °C/GPa; ∼20 °C/km) on a garnet-amphibolite residue. These conditions are just above the vapor-present solidus calculated for the bulk composition of garnet-bearing and garnet-free amphibolites from Laguépie. Retrogression is evidenced by the development of low-Al magnesiohornblende rims around tschermakite in equilibrium with oligoclase and epidote (THbl-Pl around 510–580 °C) in the epidote-amphibolite and/or greenschist facies. The porphyroclastic texture of garnet, amphibole and plagioclase and the crystallization of albite, chlorite and actinolite whithin cataclasic shear zones were acquired in the amphibolite and greenschist facies, respectively. Solid state deformation characterized by a top-to-the-north sense of shear (the D2 event of Faure et al., 2009) affected the Laguépie unit during retrogression in P-T conditions corresponding to the amphibolite and greenschist facies after the partial melting event. U-Pb ages of luminescent and zoned zircon rims in a leucotonalitic lens from Laguépie unit (sample AJAH09) yield an age of 363 ± 3 Ma (Fig. 8; Tab. 1) which is interpreted as the timing of felsic magma crystallization following partial melting of the amphibolite.
Our petrological and chronological study demonstrates that these two units have contrasted pressure-temperature-time-deformation histories (Fig. 9) and cannot be assigned to a single tectono-metamorphic unit. The implications of this result are discussed below.
Proposed P-T path (orange arrows) for the Najac and the Laguépie units. Grey P-T paths are from the literature: Groix blueschists from Ballèvre et al. (2003), Cellier éclogites from Ballèvre et al. (2014); Najac éclogite from Lotout et al. (2018); UGU eclogite from Bellot and Roig (2007); UGU paragneiss from Bellot and Roig (2007) and Schulz et al. (2009), Champtoceaux migmatites after Pitra et al. (2010). Age of the HP metamorphism in the Groix Island from Bosse et al. (2005), age of pressure peak in the Najac eclogite from Lotout et al. (2018).
6.2 Correlations with tectono-metamorphic units of the Western European variscan belt
The metamorphic units of the FMC are characterized by contrasted P-T evolutions. The metapelites of the para-autochthon have a metamorphic evolution within the greenschist facies locally reaching amphibolite facies near large Carboniferous plutons (Bellot and Roig, 2007). Both the Lower Gneiss (Lower Allochthon by Santallier et al., 1994) and Upper Gneiss Units (Bellot and Roig, 2007; Lardeaux, 2014; called Middle Allochthon by Santallier et al., 1994) display evidences for pervasive recrystallization in the amphibolite facies, around 600–750 °C, 5–10 kbar (see Faure et al., 2009; Do Couto et al., 2016) after a phase of high pressure metamorphism, mostly recorded in the UGU. The uppermost epizonal units (called Upper Allochthon by Santallier et al., 1994) are poorly characterized, they are mostly considered as greenschist facies meta-sedimentary and meta-igneous rocks (Roig et al., 1996; Lardeaux, 2014). The nappe stack in the southern Armorican massif is either described similarly to the FMC by Faure et al. (2005, 2008) or subdivided into various allochthons by Ballèvre et al. (2009, 2014). In both the FMC and AM, a Middle Allochthon has been defined on the basis of its structural position within the nappe stack and the metamorphic conditions recorded by its constitutive rocks. Berger et al. (2010a) described zoisite and kyanite eclogites (∼660 °C, 29 kbar) exhumed at temperatures below 650 °C. They are located close to the contact between LGU and UGU and were included into a Middle Allochthon. Ballèvre et al. (2014) proposed to assign the Groix and Bois de Céné blueschists (<570 °C, up to 17 kbar and also devoid of recrystallization in the amphibolite facies, Ballèvre et al., 2003) to a Middle Allochthon but its structural position is uncertain and debated (see Ballèvre et al., 2009 and also Faure et al., 2005). A Middle Allochthon would thus define as a unit comprising cold HP rocks devoid of Late Devonian amphibolite facies recrystallization and located between LGU and UGU.
The Najac unit is often included within the Upper Gneiss Unit on maps published by several authors (Lardeaux, 2014; Faure et al., 2017; Lotout et al., 2018). However, the UGU, containing most of retrogressed eclogite lenses in the FMC (formed during the 420–400 Ma D0 event of Faure et al., 2009), also include migmatitic paragneisses having experienced temperatures up to 700–750 °C (Middle Devonian D1 event of Faure et al., 2008, 2009) followed by retrogression in the amphibolite facies (Upper Devonian D2 event; Faure et al., 2009). The P-T path of the Najac unit is unusual in the French Massif central (Fig. 9; see Bellot and Roig, 2007; Faure et al., 2009 and Lardeaux, 2014 for reviews on the metamorphic structure and evolution of the French Massif central). Rocks forming the Najac unit have not recorded the D1 and D2 amphibolite facies metamorphic phases preserved in LGU and UGU and instead preserve high-pressure, low temperature (340 °C/GPa at peak pressure) event contemporaneous with a top-to-the-southeast sense of shear. High-pressure rocks included in the Middle Allochthon of the FMC and the AM display metamorphic evolutions similar to the one of the Najac unit, i.e. a HP stage followed by an isothermal exhumation path without recrystallization in the amphibolite facies (Berger et al., 2010a; Ballèvre et al., 2003, 2014). Delor et al. (1986) described glaucophane relics in Najac eclogites and already proposed that they belong to the same tectono-metamorphic unit than the Groix and Bois de Céné units in the Armorican massif. High-pressure rocks from these Middle Allochthon occurrences in Brittany (Guiraud et al., 1987; Ballèvre et al., 2003) are characterized by a cold high pressure metamorphism (<500°, up to 18 kbar; 7–8 °C/km) followed by exhumation at low temperature (<500 °C) that compares to Najac micaschists (Fig. 9a). The base of the Lower Allochthon (Lower Gneiss Unit of Faure et al., 2005) unit in the Armorican massif also contains eclogitic lenses and HP orthogneiss (in the Cellier unit) having quite similar peak conditions (600 °C, 2 GPa; 10 °C/km; Fig. 9a) (Ballèvre et al., 2014) when compared to the Najac unit. However, they cannot be considered as the lateral equivalent of the Najac unit as the latter clearly thrusts over the Lower Gneiss Unit (Fig. 1).
Published ages for HP metamorphism in the Middle Allochthon are not strictly equivalent in different locations. Lotout et al. (2018) performed multi-method dating (U-Pb zircon and apatite; Sm-Nd and Lu-Hf isochrons) on a retrogressed eclogite from Najac and obtained Upper Devonian ages (383–369 Ma) interpreted as the age of high-pressure metamorphism. Sm-Nd, Rb-Sr and Ar-Ar geochronology by Bosse et al. (2005) also yielded 370–355 Ma for high pressure metamorphism and exhumation of the Groix blueschists. Berger et al. (2010a) proposed that the age of HP metamorphism in Middle Allochthon of Limousin is Lower Devonian but this is based on questionable and sparse ages obtained on thin uranium-poor zircon rims surrounding uranium-rich Ordovician cores. Upper Devonian (∼380 Ma) ages were also obtained on these zircon rims but they were tentatively attributed to D1 Late-Devonian high temperature metamorphism recorded in Limousin (cf. Faure et al., 2008; Melleton et al., 2009) while the dated eclogite is almost not affected by retrogression. New careful analyses done in the zircon rims from the same sample investigated by Berger et al. (2010a) yielded younger Upper Devonian ages (work in progress).
Considering the metamorphic evolution, the age and the structural position (thrusting over the Lower Gneiss Unit) of the high-pressure Najac unit, we thus propose that it represents the lateral equivalent of the Groix and Bois de Céné unit in the Armorican massif and the Limousin eclogites of Berger et al. (2010a) and assign this unit to the Middle Allochthon Further exploration of phengitic, biotite-poor garnet micaschists and associated eclogites is needed in the French Massif central to better characterize a potential Middle Allochthon and to correlate it with well-known occurrences of the Armorican massif.
The Laguépie unit records amphibolite facies metamorphism peaking at 710–730 °C, 10 kbar, corresponding to metamorphic conditions obtained in the Upper Gneiss Unit elsewhere in the French Massif central (Burg et al., 1984; Bellot and Roig, 2007; Schulz, 2009; Lardeaux, 2014; Do Couto et al., 2016; Fig. 9b). The UGU hosts retrogressed eclogites enclosed into migmatitic paragneisses, formed during the D0 and D1 events, respectively (Faure et al., 2009; Melleton et al., 2009; Do Couto et al., 2016). High pressure metamorphism and partial melting were followed by retrogression in the amphibolite facies around 600–700 °C, 5–10 kbar during the Upper Devonian/Lower Carboniferous D2 event (Faure et al., 2009). Association of mafic and felsic rocks recrystallized in the amphibolite facies is common in the Leptyno-Amphibolite Complex (LAC), usually attributed to the UGU (see Ledru et al., 1989, 1994 and Lardeaux, 2014) and more rarely to the LGU (Bellot and Roig, 2007). Mafic rocks from the LAC often display relict assemblages attesting for eclogite and HP granulite facies metamorphism (Santallier et al., 1988) and their igneous precursors are thought to have been emplaced in an ocean-continent transition zone (Lardeaux, 2014). If the Laguépie unit belongs to the LAC, it must be envisaged that the some of the mafic-felsic associations can also originate after partial melting of a mafic precursor. The age of partial melting and felsic melt crystallization has been constrained at ca. 363 ± 3 Ma in the Laguépie unit. While Faure et al. (2009) usually ascribe the partial melting event to the 385–375 Ma Devonian D1 phase, U-Pb dating indicates that amphibolite facies (up to 730 °C) partial melting at Laguépie occurred during Late Devonian. It was followed by top-to-the-north shearing under amphibolite to greenschist facies conditions probably during Lowermost Carboniferous corresponding to the kinematic proposed for the D2 event (Faure et al., 2017).
In the Armorican massif, robust P-T estimates by Pitra et al. (2010) yielded peak temperature above 650 °C at pressure conditions ranging from 8 to 11 kbar for migmatitic paragneisses of the eclogite and HP orthogneiss bearing Champtoceaux unit. However the structural position of this units is debated: Faure et al. (2005, 2008) include it into the UGU by correlation with FMC occurrences; Ballèvre et al. (2009) and Pitra et al. (2010) place it at the base of an Upper Allochthon while the upper parts of this allochthon involve a Cadomian basement with low grade metasediments and ophiolites (Faure et al., 2005, 2008; Ballèvre et al., 2009; Ducassou et al., 2011). It is however included within the Lower Allochthon by Ballèvre et al. (2014) by correlation within Iberian massifs. The Laguépie and Champtoceaux units both yield peak temperature conditions around 700 °C and 10 kbar (Fig. 9). Their metamorphic evolutions are thus more comparable to the Upper Gneiss Unit in FMC, as suggested by Faure et al. (2005, 2008). Considering the conditions and age of amphibolite facies metamorphism (363 Ma) along with the deformation post-dating the anatectic stage, the Laguépie units correlates with the LAC in the FMC and the Champtoceaux Unit in the AM, that we tentatively ascribe to the Upper Gneiss Unit as defined in the literature (see Lardeaux, 2014; Fig. 9).
6.3 Geodynamic significance
The results presented in this study and those published recently by Lotout et al. (2018, 2020) are not compatible with the subdivision in tectono-metamorphic phases proposed by Faure et al. (2005, 2008, 2009). In these latter papers, the D0 phase correspond to the formation of HP units between 420 and 400 Ma during the closure of an oceanic domain separating Gondwana and Armorica. However, Lotout et al. (2018) provided Upper Devonian ages for the Najac eclogites and Lotout et al. (2020) obtained Upper Devonian to Early Carboniferous ages for HP metamorphism in Lévézou. These data suggest that HP metamorphism is younger in southern French Massif central compared to other occurrences (Pin and Lancelot, 1982; Ducrot et al., 1983; Paquette et al., 1995). Furthermore, partial melting in UGU as recorded in the Laguépie unit is usually ascribed to the 385–375 Ma D1 event by Faure et al. (2009) but it is dated at 363 Ma at Laguépie. It is however affected by the Late Devonian/Lower Carboniferous D2 top-to-the-north shearing (Faure et al., 2017). These discrepancies suggest that either (i) new and old ages for HP metamorphism should be critically evaluated because dating HP metamorphism is a difficult and challenging task or (ii) metamorphic events are about 20 Myr younger in southern French Massif central compared to northern parts or (iii) that final collision between Armorica and Gondwana occurred during Upper Devonian/Early Carboniferous and not Lower Devonian, as suggested by Lardeaux (2014) and Ballèvre et al. (2009, 2014).
If we consider that Upper Devonian HP/LT metamorphism (Lotout et al., 2018, 2020) is coeval with partial melting in UGU (Melleton et al., 2009; this study) and active margin magmatism as represented by tonalites and diorites intruding the UGU (375–355 Ma; Bernard-Griffiths et al., 1985; Shaw et al., 1993; Bertrand et al., 2001; Pin and Paquette, 2002); these data are compatible with an active subduction system forming a paired metamorphic belt during Late Devonian (Miyashiro, 1967; Brown, 2006). The Najac unit, comprising a basic/ultrabasic intrusion within orthogneisses and micaschists all metamorphosed under eclogite facies conditions, either represents fragments of a continental lower plate or the accretionary prism in the subduction system (proposed for the Groix blueschists, Ballèvre et al., 2014). The UGU, and accordingly, the Laguépie unit, are, in this proposition, part of the upper plate of the subduction system, similarly to what has been proposed by Lardeaux (2014) and Lardeaux et al. (2014). Nappe stacking that caused superimposition of the Najac and Laguépie units occurred after 363 Ma, probably during the Early Carboniferous 345–335 Ma D3 phase of Faure et al. (2009) because the Najac micaschists were not affected by the Late Devonian 700 °C/10 kbar metamorphism observed at Laguépie.
Petrological investigations on metamorphic samples from the Najac and Laguépie units in the southwestern FMC reveal two distinct P-T evolutions. The Najac unit is characterized by syn-kinematic eclogitic metamorphism in micaschists and basic rocks implying subduction of a continental margin at the end of the Devonian (around 377 Ma) followed by cold exhumation in the greenschist facies. The Laguépie unit records amphibolite facies metamorphism (710 °C, 10 kbar) dated at 363 Ma and later affected by deformation and retrogression under amphibolite to greenschist facies conditions. These two units were formerly grouped into the leptyno-amphibolite complex belonging to the Upper Gneiss Unit. Comparison with tectono-metamorphic units in the French Massif central and the Armorican massifs suggest that the Najac unit can be integrated into the HP/LT Middle Allochthon while the Laguépie unit belongs to the Upper Gneiss Unit. The French Massif central consequently preserves the remnants of an Upper Devonian paired metamorphic belt, where the Middle Allochthon represent subducted material attached to the slab or within an accretionary prism while the Upper Gneiss Unit was located within the upper plate of the subduction system. Lower Carboniferous continental collision further led to the stacking of metamorphic units with contrasted pre-Carboniferous histories. The stack, in its current configuration, is showing an apparent inverted metamorphic gradient, well expressed in the Rouergue domain.
The structure of the tectono-metamorphic units near Najac can be considered as a reference for further studies on the structure and evolution of metamorphic units preserved in the French Massif central. Future investigations should focus on obtaining precise P-T-t paths on pre-Carboniferous metamorphic units belonging to the FMC and exploration of phengite-bearing biotite-poor garnet micaschists (locally enclosing eclogites) possibly marking a still poorly defined Middle Allochthon. Altogether, these results should be used to propose an integrated tectono-metamorphic framework that can be useful to test the different geodynamic scenarios proposed for the Variscan orogeny in Western Europe.
This study was partly funded by a SYSTER-TELLUS grant from the INSU-CNRS. Stays of AB at Toulouse were funded by the FP7 IRSES MEDYNA project and an excellence EIFFEL fellowship. Fabienne de Parseval is thanked for making thin sections; Philippe de Parseval and Sophie Gouy supervised the electron microprobe analyses and Thierry Aigouy helped with SEM observations. We acknowledge comments by Michel Faure and an anonymous reviewer as well as editorial handling by Jean-Marc Lardeaux, Olivier Averbuch and Laurent Jolivet.
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Table S1. Tables of mineral chemistry for samples of Najac micaschists and Laguépie amphibolites.
Prograde and retrograde P–T evolution of a Variscan high-temperature eclogite, French Massif Central, Haut-Allier
Structure of lamprophyres: a discriminant marker for Variscan and Alpine tectonics in the Argentera-Mercantour Massif, Maritime Alps


text:
Q: Undefined split method while using request.url I am trying to get the current url of my page and the parameters that go with it. When I manually put the url in, the undefined split method error does not occur. I have tried the following:
request.url
request.original_url
request.fullpath
adding in
id = request.original_url

and adding this function
def original_url
  base_url + original_fullpath
end

What does currently work for me is below, but I cannot have the same url and parameters every time so this method won't work later on.
   #parse current url
    #what I would like below in comment
    #id = request.original_url
    url =   "http://127.0.0.1:3000/reviews/new?id=2"
    uri    = URI.parse(url)
    params = CGI.parse(uri.query)
    id     = params['id'].first

Any help or tips on if I'm missing something would be appreciated.

A: Had the same issue. The absence of query parameters in url was causing it.
url = "http://127.0.0.1:3000/reviews/new" # no query params
uri = URI.parse(url)
query = uri.query # nil
params = CGI.parse(query) # Undefined split Exception

This solves it:
uri = URI.parse(url)
if uri.query
  params = CGI.parse(uri.query)
  id = params['id'].first
end

redpajama_set_name: RedPajamaStackExchange


text:
Explore insights, lessons, and resources from our work
Democracy Fund staff — alongside grantees, researchers, and other field experts — regularly develops resources and shares lessons on strengthening democracy. Here you will find guides, reports, and insights from our team and network.
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redpajama_set_name: RedPajamaCommonCrawl


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text:
Q: Convert query to a Left-Join (?) to include userid's without a match I am trying use a MySQL query to build a leaderboard of users in a game of Bowl Mania (where users each try to predict the winner of each College Football game, and assign a points weighting to each selection).
I have 3 tables:
--games
id   team1   team2   year

--picks
userid  gameid  points

--actResults
gameid   winner

I would like to build a SELECT query that orders each user based on the summer of their "Points" wager for each successfully predicted game (i.e. a successful wager of 5 on gameid=1 earns 5 points, while unsuccessful predictions earn 0).
The query below almost accomplishes what I want, but the only problem is that it does not include users who have zero points (i.e. users who do not have any matches between picks.winners and actResults.winners).
SELECT DISTINCT picks.userid AS Player, SUM( picks.points ) AS Points
FROM picks, games, actResults
WHERE picks.gameid = games.id
AND picks.winner = actResults.winner
AND games.year =  '2014'
AND picks.userid = picks.userid
GROUP BY picks.userid
ORDER BY Points DESC

Desired results would look something like this
Player  Points
User1   10
User4   9
User3   4
User2   0
User5   0

A: The hard part is not the conversion to LEFT JOIN (basically that just involves changing the comma-join to a regular ANSI JOIN, and then inserting the keyword LEFT), but rather, fixing the SUM expression to only add the rows where actResults.winner = picks.winner. Here is one way to do it:
SELECT picks.userid AS Player,
       SUM(CASE WHEN actResults.winner IS NULL
                THEN 0
                ELSE picks.points
            END) AS Points
  FROM picks
  JOIN games
    ON games.id = picks.gameid
  LEFT
  JOIN actResults
    ON actResults.winner = picks.winner
 WHERE games.year = '2014'
 GROUP BY picks.userid
 ORDER BY Points DESC
;

(Another way is to skip the LEFT JOIN entirely, and use an EXISTS expression with a subquery.)

Edited to add: To add an "Available Points" field, as requested in the comments, you could write:
SELECT picks.userid AS Player,
       SUM(CASE WHEN actResults.winner = picks.winner
                THEN picks.points
                ELSE 0
            END) AS Points,
       SUM(CASE WHEN actResults.gameid IS NULL
                THEN picks.points
                ELSE 0
            END) AS AvailablePoints
  FROM picks
  JOIN games
    ON games.id = picks.gameid
  LEFT
  JOIN actResults
    ON actResults.gameid = games.id
 WHERE games.year = '2014'
 GROUP BY picks.userid
 ORDER BY Points DESC
;


text:
TCSO: Another Hoax E-mail Threat Made To Local Schools
By B.J. Hansen	 Published Apr 13, 2018 07:19 am Updated Apr 13, 2018 12:38 pm
Image included in e-mail threat
Sonora, CA — Many school districts in Tuolumne and Calaveras counties last night received an e-mail threatening that a male student would enter campus at the beginning of the day with a bomb in a bag.
Tuolumne County Sheriff's Office spokesperson Andrea Benson reports the e-mail did not mention a school by name, nor say a specific date when the action would occur. She adds that the threat is believed to have come from the group ApopisSquad, the same hacking group responsible for similar threatening type emails sent to school districts across the nation earlier this week.
She adds, "The FBI is aware of the new threat and an investigation is ongoing into the hacking group and hoax emails. Although these emails have been deemed a hoax, our office takes any threat to the safety of our school campuses and students seriously."
The Angels Camp Police Department also confirms that similar emails were sent last night to schools in Calaveras County.
Written by BJ Hansen.


Under the guidelines of the Smart City Mission, a Special Purpose Vehicle (SPV) was formed which would implement the Panaji Smart City roadmap which will lead to the transformation of the city into a smart city. The SPV named 'Imagine Panaji Smart City Development Limited' was announced on 17th August 2016 by Shri. Sidharth Kuncalienker, Vice-Chairman GSIDC, Chief Mentor, Smart City, Chairman EDC and MLA Panaji Constituency in the presence of Shri. Dipak Dessai, Commissioner, CCP and Shri. Swayandipta Pal Chaudhari, Executive-Director Finance, GSIDC and Managing Director & CEO, Imagine Panaji Smart City Development Limited .The Centre had earlier announced the list of 13 cities which made it to the top of the list in the Fast Track Mode of the Smart City Submission of which Panaji won a coveted seat. Panaji is the second city after Dharamshala to incorporate an SPV.
The Imagine Panaji Smart City Development Limited will be governed by a Board of Directors and will plan, appraise, approve, release funds, implement, manage, operate, monitor and evaluate the Smart City development projects as per guidelines formed by the central government. Urban Development Secretary Shri. Sudhir Mahajan, IAS is the Chairman of SPV and Shri. Swayandipta Pal Chaudhari, Executive-Director Finance, GSIDC is the CEO of SPV.


Bill, Kathy, Austin, and Katherine moved to Daytona Beach, Florida in March of 1998. The company Bill was working for closed the Loveland, Colorado office and transferred him to the office in Daytona Beach, Bill's hometown. Even though he was battling melanoma, following lung surgery and brain surgery, he would go into the office the days he was not ill from treatments; or traveling to and from treatments and trials. His friends from high school rallied around Bill. When he was able, they would get together.
As the months progressed, so did Bill's melanoma. In June of 1998, Tim Richardson felt helpless over the fact that his best friend from high school was slipping away and there was nothing that anyone or any medicine could do about it. On one of Tim's visits with Bill in Daytona, he went to the beach to think and pray. As Tim was walking on the beach, he noticed runners participating in a race. Then, at that moment, Tim understood what he had to do. He decided he would gather other high school friends and have a walk/run in Bill's name to help raise money to combat this terrible disease.
Unbelievably, on August 15, 1998 the 1st Annual Bill Walter III Melanoma Research Fund 5K walk/run took place on the beach at Ormond Beach. Bill was there. He was weak, but he was there. The Volusia County Beach Services provided him with a beach wheelchair. He was amazed at the number of participants. 100 runners came out to support the cause. After the race, Tim asked Bill where he would like the money to go if "this thing really takes off." Bill's response was that he would like to help other melanoma patients financially with their travel expenses to and from trials and treatments, and he would like to help in finding a cure for melanoma.
"This thing" has REALLY taken off. The Bill Walter III Melanoma Research Fund 5K walk/run now has a name, RayZ Awareness. At our last event, there were nearly 500 runners and walkers. Many years, RayZ Awareness and skin care protection events are held in Ft. Collins, Colorado. Kathy Walter still works diligently. Since the first race in 1998, we have raised well over $100,000.00 which is helping melanoma patients and promoting and funding melanoma research.
We are a non-profit organization and there are no paid employees. Each and every person who works on our race and those on our Board of Directors gives freely of their time. Each and every dollar that comes to the Bill Walter III Melanoma Research Fund goes directly to research, to educating about melanoma, or to assist melanoma patients. We have donated over $20,000.00 to melanoma patients and we have invested over $50,000.00 in research toward finding a cure. For the last two years BWIIIMRF has partnered with the national Melanoma Research Foundation in bringing together, for the first time, basic scientists who are doing research in melanoma. Because of these symposia, there will be The First Melanoma Research Congress held in Philadelphia in June 2003.
Donna Hiatt of Daytona Beach is our RayZ Awareness Race Director.


For further details of these events see the relevant page on this website.
See bottom of page for Anglian Water Competition Diary 2019.
3rd (Thursday) Invicta Social and Buffet – Arundel House Hotel, Cambridge. 7pm.
2nd (Saturday) 9:30am – 12:30pm – Fly Tying Workshop at Grafham Lodge.
9th and 10th (Sat/Sun) British Fly Tying Fair -Stafford County Showground.
16th (Saturday) 9:30am – 12:30pm – Fly Tying Workshop at Grafham Lodge.
23rd (Saturday) Invicta Annual Dinner – The Wheatsheaf at Perry.
21st (Thursday) Invicta AGM and Anglian Water Update.
4th (Saturday) Invicta Snowbee Floating Line Competition – Grafham Water.
14th (Tuesday) Evening League starts (14 weeks) – Grafham.


All of the researchers featured on our Meet a Scientist Saturdays have been trained through Phipps' science communication workshops. If you are young professional or graduate student in the sciences and you are interested in the workshop or participating in a Meet a Scientist Saturday, check out our websiteor email our science education outreach manager Dr. Maria Wheeler-Dubas for more information.
For this month's Meet a Scientist Saturday, here is a unique opportunity to talk science careers with two folks who are vital to a nationwide research program but don't directly spend time in a lab themselves. Nadia Jones and Jennifer Jones are both a part of the University of Pittsburgh's extension of the National Institute of Health's All of Us program—a massive initiative to better understand human health so that in the future, healthcare decisions can be based more on individual patients rather than broad trends. Jen and Nadia will be in Palm Court on Saturday, August 18, from 1:30-3:30 pm; be sure to stop by!
Nadia: My name is Nadia Jones, and I am thrilled to work at Pitt's Clinical and Translational Science Institute (CTSI). Our team helps bring health sciences to a range of communities. As a Community Engagement Coordinator for the All of Us Pennsylvania Research Program, I get the opportunity to help advocate for diversity in health research on a national scale.
Jen: Hi everyone! My name is Jennifer Jones and I am the Executive Director for the Training and Education Center, as part of the All of Us Research Program. I have a background in health communication, public health and program planning and evaluation. Health literacy is my biggest public health passion.
Why did you get involved in health research?
Nadia: I realized early on that too often, small differences can lead to health disparities. Adequate and accurate representation of diverse communities in health research can help eliminate health disparities and create tailored, more inclusive health care. I jumped at the opportunity to help shine light and improve this issue.
Jen: Public health sits at an interesting crossroad between healthcare, policy, the environment, personal health, community health…it is truly fascinating! I focus on community-engaged research, meaning that community members feel empowered to understand research and are recognized as a key part of the research process.
What is the most exciting thing you've ever done at work?
Nadia: I really enjoy having conversations that many people and institutions tend to avoid. Our Urban League partner, Erricka Hager, and I hosted a roundtable discussion exploring why racial/ethnic minority groups lack a presence in health research. We discussed a range of topics including mistrust, barriers, and historical wrongdoings.
Jen: My team is currently working on national training and educational deliverables about genetics and research ethics. When those get released, it will be awesome to know they are impacting and empowering thousands of people around the country.
Nadia: My favorite part of community engagement for a national research program is having the opportunity to experience the humanity behind the science. I interact with real people. I see their curiosity, skepticism, excitement and indifference. I get to explore those feelings through a genuine, education-driven conversation.
Jen: In my new role as Executive Director, I enjoy thinking about high-level strategies for engagement and education to a wide range of audiences.
If you weren't involved in health research, what would you be?
Nadia: I have an inclination towards advocating for diversity. If I was not involved in health research, you would find me somewhere between the clinical and administrative sectors of health care.
Jen: I would definitely be a doctor…if only I liked chemistry more! I love being in the health field, but a part that focuses on public health and ensuring that researchers think about community as they design, implement and disseminate their research.
Why is science education important?
Nadia: Science education is important because the future of human health and health care depends on it. Let us also not forget that ease of access to education and health resources can make a world of difference. I believe that science and research can help influence not only legislative but also social change.
Jen: Because of ever-advancing technology, science is changing what we know, especially as it relates to our health. Still being early in my career, I am so excited about the discoveries that will be made in the next few decades! What is most important is that those discoveries benefit everyone, which is why I believe in the mission of the All of Us Research Program so much! I encourage everyone to learn more at www.joinallofuspa.org.
Where did you guys go to school?


X-Large - $49.99 Only 7 left!
Ah, Daddy Pig. He's the everyman in Peppa Pig. He's stuck in an office job and he eats more cake and cookies than one man should and pays the price for it. (Sorry, Mr. Pig, we know you like to tell people that your tummy is all muscle, but we're not buying it.) He gets a little grumpy when he can't find his glasses and he hates working out. He sounds pretty relatable. We'd hang out with him after work if he asked us, since he seems like our kind of pig.
So, are you a little like Daddy Pig, the everypig? Then, maybe it's time you turned yourself into the funny character from Peppa Pig! Based on the adorable cartoon series, this adult Daddy Pig costume comes with a turquoise top, complete with a matching tie attached to the top. The tummy even looks a little pudgy, much like the real Daddy Pig's "muscles". You also get the Daddy Pig headpiece, which has all of Daddy Pig's features, like some fake beard hairs and glasses attached to the face. You'll be ready to become head of the house while wearing it.
This officially licensed costume also makes for a great family costume idea, since we also carry Mummy Pig and Peppa Pig costumes to perfectly complement this outfit. You may, however, feel a strong urge to eat a little too many cookies when you wear this (to gain some extra muscles, of course).
Looks just like Daddy Pig. The tummy is too funny. I would go up a size if you are in between sizes. Doesn't have a tail like the rest of the family which I found strange.


Now that Sydney and I can walk, trot, and canter with rhythm and relaxation, my trainer started us on a new exercise that includes some work down the long sides.
I am sure you're horrified to think that we've been stuck at A, but the truth is, we sort of have been. In my own arena, I utilize the whole "court." I do a walk warm up around the outside and then do a variety of figures that include circles at A or C, serpentines, shallow loops, and changes across the diagonal.
My arena with the "court" laid out with poles.
Over the last three years, I've used all of the space in JL's arena too, but at different times. Her arena is a large oval with room to do flat work at either end. The middle portion is filled with an array of fences. For the most part, we work at the end closest to the barn. It's set back from the road, and other horses are comfortably close. It's also wider than a 20 x 60 dressage court which means that I can do figure eights (two, 15-meter circles?) with an opportunity to also ride some straight lines.
A partial view of the barn end of JL's arena - Photo by Lillian.
For Wednesday's lesson, we decided that I had the necessary skills to start working on longer lines into a turn, like you would do in a full length court. The exercise doesn't focus on a specific gait, but rather on maintaining control of the outside shoulder so that the horse makes the turn without a loss of rhythm.
On an OTTB who doesn't like any lapses in my application of the rules, this turned out to be quite the challenge. We tried it twice at the canter, but since I wasn't quite prepared, Sydney was allowed to get too fast which made him think that everything was going to hell in a hand basket. We ended up doing it at the trot for this lesson so that I understood the purpose more clearly.
Here's how it went: we picked up the trot and did a 20-meter circle at the barn end of the arena. Tracking left, I then made the turn down the long side through a narrow "chute" that had jumps to our left and the rail to our right. As we approached the other working end of the arena, we were to make a left turn (not using the rail) and come back down the other long side through another narrow chute created by fences and the rail.
JL told me to be prepared for a horse that was going to race through the chute and then lose the ability to make the left turn at the end. She was right. The exercise showed how heavy he can be on the outside rein and how much I have to work to get him to lighten up.
This exercise really worried Sydney. JL explained that he knew we were doing something different and wasn't sure that the rules were going to be the same. Our number one rule is no rushing. Slow and thoughtful is what we're trying to teach him. So when we started down the long side and I let him pick up speed, it freaked him out. JL had me stop him with the outside rein to remind him that nothing had changed.
We worked for a while on halting in the chute at both the walk and trot to remind Sydney that none of this work required rushing. By the end of the lesson, his ears were once again Eeyore floppy and his stride opened back up. We rode the open ends in a nice rhythmic trot that we were able to hold and carry through the chute. Sydney was so light on the outside rein that I was able to send him sideways so that he could bend around my inside leg as he made the turns.
It seems silly to be excited about using the long sides, but even Christian Schacht, the German clinician with whom I've been riding this last year or so, would recognize how difficult this exercise was for Sydney. I hope that we'll be doing it at the canter next week, but I won't be disappointed if we have to do it at the trot for a while. To ride it successfully, Sydney needs to be able to trust that I will be able to help him stay balanced and safe. That means I better get it together ASAP so that I can actually do that!
Sounds like a great ride! You guys are really understanding each other!
We're getting there. I am so lucky to have found a trainer who understands TBs. Everything we do now is focused on his mind. It is only when my aids are crystal clear that he is happy. JL focuses a LOT of time and energy on explaining things to the horse in a way that they can understand.
With Speedy, I am can be a bit wishy-washy or inconsistent. It won't fry his brain. With Sydney, everything has to be just so. Any time something is unclear, we simply step back and break it down into very simple parts. Once he understands the rule, he expects me to follow the rule every single time.
Holy cow that totally cracked me up. Our dear ottbs do have their quirks, which generally result in our having to be become better, fairer riders.
And I hate to bore everyone, but I am simply overwhelmed with gratitude at the change that has come over this horse (and obviously over me too!).
I don't know if I have truly conveyed how scary he was to ride. And it wasn't just me who thought he was a bit much. My trainer felt like it would have been okay to send him on as well. She had doubts as to whether we could/would ever get through to him. Even the German trainer with whom I ride described Sydney as a horse with a destroyed mind.
It is nice, isn't it? We work hard to keep it that way though. It gets watered every day (we drag the sprinklers around) and my BO drags it as needed to keep the little whoop-de-dos level. It's also REALLY big, at least 40-meters wide (enough for two dressage courts). It's not quite long enough, but I have enough space to set up a 20 x 50 court with a lot of room around the outside for lunging, etc.