The variscan front and the midi fault between the channel and the meuse river

The ECORS seismic profile allows a new insight into the deep geology of northern France. Various geological data, such as ancient coal mines, surface mapping and boreholes, are used to interpret the seismic profile. A new cross-section, directly superimposed on the ECORS seismic profile (Cambrai-Dreux), is compared with a previous one, drawn along the Meuse River through the Ardenne Massif. The cylindrism and length-balancing hypotheses are discussed by comparing the two cross-sections. The main geological results are: (a) the emplacement of the Dinant Nappe is later than most of its internal deformation; and (b) major folding and thrusting give an approximate 30–35% shortening, without taking into account the internal deformation (minor folding and cleavage) and the unknown net translation vector of the Dinant Nappe (50 km at least, possibly 150 km).     

The structural evolution of the Paleozoic of the Pyrenees

Five deformationphases occurring on a regional scale have been found in the Paleozoic sequence of the Pyrenees. The first phase was responsible for the development of large concentric folds in the southern and northern borders of the axial zone. The second or main phase has lead to the differentiation in suprastructure and infrastructure. Folds have E-W axes and are accompanied by cleavage or schistosity. The next phase has N-S axes and its occurrence is restricted to the infrastructure. The third cleavage phase is a conjugate system with vertical NW and NE striking axial planes of folds. Like the N-S phase it indicates E-W compression. The fourth cleavage phase has again an E-W direction like the main phase. The intrusion of the granites can be related to this structural history. A final phase consists of tilting and fanning of the cleavage of the suprastructure, accompanied by the formation of knickzones.

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Zusammenfassung Im Paläozoikum der Pyrenäen konnten fünf verschiedene Deformationsphasen über große Gebiete hinweg festgestellt werden. Die erste hat im Süden und Norden der Axialzone sehr große N-S bis NE-SW gerichtete Biegefalten verursacht. Die zweite, aber erste Schieferurigsphase ist in dem epizonalen Schiefergebirge oder Oberbau und in dem meso- bis katazonalen Unterbau verschiedenartig entwickelt. In beiden Fällen streichen jedoch die Faltenachsen E-W, und es liegt eine N-S-Einengung vor. Die folgende Phase ist auf die metamorphen Gebiete beschränkt und wird von N-S gerichteten Falten mit flacher Schieferung begleitet. Die dritte Schieferungsphase besteht aus zwei gleichzeitigen Scherfaltensystemen in NW- und NE-Richtung. Sie weist wie die vorhergehende Phase auf eine Einengung in E-W-Richtung hin. Die vierte Phase hat E-W gerichtete Falten mit Schieferung hervorgerufen und ist wie die Hauptphase eine N-S-Zusarnmenstauung. Die Intrusion der Granite kann in diese tektonische Entwicklung eingeordnet werden. Während einer späten Phase sind die Schieferungsflächen zu einem großen Fächer verstellt worden. Das Auftreten von Knickzonen ist mit diesem Auseinanderfallen der Schieferung verbunden.

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Résumé Dans le Paléozoique des Pyrénées cinq phases de déformation peuvent être reconnues. La première phase a formé des plis concentriques sans schistosité et se trouve près de la bordure nord et sud de la zone axiale. Les quatre phases suivantes sont accompagnées d'une schistosité. La phase principale a causé une différentiation entre supra- et infrastructure, tous les deux avec des plis E-W. La deuxième phase synschisteuse ne se trouve que dans l'infra-structure et est caractérisée par des plis N-S. Une phase suivante consiste d'une système conjugée de plis avec direction des plans axiaux des plis NW et NE. La dernière phase a produit des plis E-W. L'intrusion des granites peut être datée dans cet histoire tectonique. Une phase tardive a causé la formation d'un gros structure en éventail des plans de clivage du suprastructure.

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Structural geology of the Lys-Caillaouas massif,Central Pyrenees. Evidence for a large scale recumbent fold of late Variscan age

Abstract

A review of data on the Lys-Caillaouas massif leads to a re-interpretation of its Variscan structural evolution. During a first phase of N-S shortening upright folds with steep axial plane foliations were formed. Subsequent regional metamorphism was followed by porphyroblast rotation and formation of gently dipping crenulation cleavages. During this event a N-closing recumbent fold at the scale of the massif developed, with relatively undeformed first phase foliations in the upper limb (suprastrucfure) and highly deformed and transposed foliations in the lower limb (infrastructure). This recumbent fold is argued to result from temperature induced gravity collapse of a crustal block previously having subvertical planes of anisotropy.     

Geology in the Pyrenees

M.D. Jones runs special–interest, geology and natural history holidays to the Pyrenees, Spain, North Africa, Iceland and elsewhere, and is a part–time tutor in the Department of Adult Education at the University of Leicester.     

The influence of the evolution of the Pyrenees on adjacent basins

Important thicknesses of syn- and post-orogenic sediments are observed in the southern part of the Aquitaine Basin and in the north of the Ebro Basin. Their deposition cannot be explained only as a result of the extensional history of the Early Cretaceous, thus the influence of the compression associated with the Pyrenees formation upon the subsidence of these basins is studied.Europe and Iberia are considered to behave as two semi-infinite elastic plates. The evolution through time of the sedimentary thicknesses is explained by the deflections of these two plates induced not only by the topographic load of the Pyrenees but also by additional forces (10¹² N/m) that may have their origin in the formation of a cold lithospheric root during the shortening.A series of calculations is presented for an approximately north-south profile across the Aquitaine Basin, the Pyrenees and the Ebro Basin; a good fit for the shape of the basins and the gravity anomalies was obtained, with flexural rigidities of 1.5·10^23. Nm for the northern plate and the outer part of the southern plate, and 1.4·10²¹ Nm for the inner part, of the southern plate.     

Wollastonite formation during variscan post-tectonic cooling in the Schwarzwald, Germany

Summary Metaquartzdioritic plagioclase-biotite-quartz-gneiss at Artenberg, Schwarzwald, Germany, contains up to 10 cm wide calcite veins partially replaced and surrounded by a zoned calcsilicate sequence. The calcsilicate veins consist of two parts: (a) a zoned mineral sequence of reaction products deposited in the vein itself (wollastonite, garnet, clinopyroxene, quartz with relics of calcite) and (b) a zoned alteration sequence in the wall rock gneiss extending from the vein-gneiss contact several cm into the plagioclase-bearing gneiss (hornblende, chlorite). Based on hornblende-plagioclase thermobarometry and on chlorite stability, the P-T conditions of calcsilicate formation are estimated to be about 450 °C at c. 2 kbar.The zoned mineral sequence formed by a bi-metasomatic reaction in an open system of the hydrothermal carbonate with the orthogneiss in the presence of an externally derived fluid. The reaction was started by H₂O and SiO₂ infiltration along the vein-gneiss contact. The stability of wollastonite at the above P-T conditions records an X_{CO 2}, of the fluid phase below 0.05. Chemical potential gradients of Ca, Al, Fe, Mg and probably Si between vein and gneiss resulted in diffusional mass transfer perpendicular to the vein-gneiss contact. The sequence of stable calcsilicate minerals suggests Ca diffusion from vein to gneiss, while Fe, Mg and Al were transported in the opposite direction, from gneiss to vein. It is inferred that the calcsilicates formed during Variscan post-tectonic cooling.

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Die bildung von wollastonit während der variskischen abkühlung im Schwarzwald, Deutschland

Zusammenfassung Metaquarzdioritische Plagioklas-Biotit-Quarz-Gneise vom Steinbruch Artenberg bei Steinach, Schwarzwald, enthalten etwa 10 cm breite Calcit-Gänge, die von einer zonierten Kalksilikat-Vergesellschaftung teilweise ersetzt und umrandet werden. Die Kalksilikat-Gänge bestehen dann aus zwei Teilen: (a) eine zonierte Mineralsequenz aus Reaktionsprodukten im Gang selbst (Wollastonit, Granat, Klinopyroxen, Quarz mit Relikten von Calcit) und (b) eine zonierte Alterationssequenz im Nebengesteins-Gneis, die vom Gang-Gneis-Kontakt einige Zentimeter in den Gneis hinein reicht (Hornblende, Chlorit). Hornblende-Plagioklas-Thermobarometrie und Chlorit-Stabilität zeigen P-T Bedingungen während der Kalksilikat-Bildung von etwa 2 kbar und 450 °C an.Die zonierte Mineralsequenz bildete sich bei der bi-metasomatischen Reaktion in einem offenen System von hydrothermalem Gangkarbonat mit dem Orthogneis in der Anwesenheit eines externen Fluids. Die Reaktion begann durch die Infiltration von H₂O und SiO₂ entlang des Gang-Gneis-Kontaktes. Die Stabilität von Wollastonit bei den obigen P-T-Bedingungen zeigt, daß die Fluidphase weniger als 5 Mol-% CO₂ enthielt. Chemische Potential-Gradienten von Ca, Al, Fe, Mg und möglicherweise Si führten zu diffusivem Elementtransport senkrecht zum Gang-Gneis-Kontakt. Die Abfolge der Kalksilikat-Vergesellschaftungen zeigt, daß Ca vom Gang zum Gneis, Fe, Mg und Al dagegen in umgekehrter Richtung diffundierten. Die Kalksilikate bildeten sich wahrscheinlich während der posttektonischen Abkühlung in der Folge der variskischen Orogenese.

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The geology of the Morecambe gas field

The subsurface of the Irish Sea contains one of the United Kingdom's most important gas fields, the Morecambe Field, owned by British Gas. Approximately 10% of the UK's daily consumption of natural gas will be supplied by this giant accumulation trapped within fluvial deposits of the Lower Triassic Sherwood Sandstone Formation.