Linking temperature estimates and microstructures in deformed polymineralic mantle rocks

To constrain deformation temperatures of mantle shear zones, we studied a strike-slip shear zone (Hilti massif, Semail ophiolite, Oman) and focused on the interaction between microstructural mechanisms and chemical equilibration processes. Quantitative microfabric analysis on harzburgites with different deformation intensity (porphyroclastic tectonite, mylonite, and ultramylonite) was combined with orthopyroxene geothermometry. The average grain size of all phases decreases with decreasing shear zone thickness. Dynamic recrystallization of porphyroclasts in combination with dissolution-precipitation and nucleation result in small-sized, chemically equilibrated pyroxenes. The composition of orthopyroxene was used to calculate deformation temperatures. In the case of the porphyroclastic tectonites, the chemical composition of orthopyroxene has been reset by diffusion yielding temperature estimates of 880-900 degrees C. The mylonites were deformed by dislocation creep of olivine and show a broad range of calculated temperatures, which result from a combination of grain size reduction and inheritance of equilibrium compositions from earlier high-temperature events and diffusion. In mylonites, diffusion profiles combined with geothermometry and grain size analysis indicate a mylonitic deformation temperature of 800-900 degrees C possibly followed by diffusion. In ultramylonites, the smallest grains (<30 mu m) reveal equilibration at temperatures of similar to 700 degrees C during the last stages of ductile deformation, which was dominated by diffusion creep of olivine. Our results provide a crucial link between temperature and evolution of microstructures from dislocation creep to diffusion creep in mantle shear zones.

Juxtaposition of melt impregnation and high-temperature shear zones in the upper mantle; field and petrological constraints from the Lanzo peridotite (Northern Italy)

Results of a field and microstructural study between the northern and the central bodies of the Lanzo plagioclase peridotite massif (NW Italy) indicate that the spatial distribution of deformation is asymmetric across kilometre-scale mantle shear zones. The southwestern part of the shear zone (footwall) shows a gradually increasing degree of deformation from porphyroclastic peridotites to mylonite, whereas the northeastern part (hanging wall) quickly grades into weakly deformed peridotites. Discordant gabbroic and basaltic dykes are asymmetrically distributed and far more abundant in the footwall of the shear zone. The porphyroclastic peridotite displays porphyroclastic zones and domains of igneous crystallization whereas mylonites are characterized by elongated porphyroclasts, embedded between fine-grained, polycrystalline bands of olivine, plagioclase, clinopyroxene, orthopyroxene, spinel, rare titanian pargasite, and domains of recrystallized olivine. Two types of melt impregnation textures have been found: (1) clinopyroxene porphyroclasts incongruently reacted with migrating melt to form orthopyroxene plagioclase; (2) olivine porphyroclasts are partially replaced by interstitial orthopyroxene. The meltrock reaction textures tend to disappear in the mylonites, indicating that deformation in the mylonite continued under subsolidus conditions. The pyroxene chemistry is correlated with grain size. High-Al pyroxene cores indicate high temperatures (11001030C), whereas low-Al neoblasts display lower final equilibration temperatures (860C). The spinel Cr-number [molar Cr/(Cr Al)] and TiO2 concentrations show extreme variability covering almost the entire range known from abyssal peridotites. The spinel compositions of porphyroclastic peridotites from the central body are more variable than spinel from mylonite, mylonite with ultra-mylonite bands, and porphyroclastic rocks of the northern body. The spinel compositions probably indicate disequilibrium and would favour rapid cooling, and a faster exhumation of the central peridotite body, relative to the northern one. Our results indicate that melt migration and high-temperature deformation are juxtaposed both in time and space. Meltrock reaction may have caused grain-size reduction, which in turn led to localization of deformation. It is likely that melt-lubricated, actively deforming peridotites acted as melt focusing zones, with permeabilities higher than the surrounding, less deformed peridotites. Later, under subsolidus conditions, pinning in polycrystalline bands in the mylonites inhibited substantial grain growth and led to permanent weak zones in the upper mantle peridotite, with a permeability that is lower than in the weakly deformed peridotites. Such an inversion in permeability might explain why actively deforming, fine-grained peridotite mylonite acted as a permeability barrier and why ascending mafic melts might terminate and crystallize as gabbros along actively deforming shear zones. Melt-lubricated mantle shear zones provide a mechanism for explaining the discontinuous distribution of gabbros in oceancontinent transition zones, oceanic core complexes and ultraslow-spreading ridges.

Equilibration and disequilibration between monazite and garnet: indication from phase-composition and quantitative texture analysis

The integration of information which can be gained from accessory [i.e. age (t)] and rock-forming minerals [i.e. temperature (T) and pressure (P)] requires a more profound understanding of the equilibration kinetics during metamorphic processes. This paper presents an approach comparing conventional P-T estimate from equilibrated assemblages of rock-forming minerals with temperature data derived from yttrium-garnet-monazite (YGM) and yttrium-garnet-xenotime (YGX) geothermometry. Such a comparison provides an initial indication on differences between equilibration of major and trace elements. Regarding this purpose, two migmatites, two polycyclic and one monocyclic gneiss from the Central Alps (Switzerland, northern Italy) were investigated. While the polycyclic samples exhibit trace-element equilibration between monazite and garnet grains assigned to the same metamorphic event, there are relics of monazite and garnet obviously surviving independent of their textural position. These observations suggest that surface processes dominate transport processes during equilibration of those samples. The monocyclic gneiss, on the contrary, displays rare isolated monazite with equilibration of all elements, despite comparably large transport distances. With a nearly linear crystal-size distribution of the garnet grain population, growth kinetics, related to the major elements, were likely surface-controlled in this sample. In contrast to these completely equilibrated examples, the migmatites indicate disequilibrium between garnet and monazite with a change in REE patterns on garnet transects. The cause for this disequilibrium may be related to a potential disequilibrium initiated by a changing bulk chemistry during melt segregation. While migmatite environments are expected to support high transport rates (i.e. high temperatures and melt presence), the evolution of equilibration in migmatites is additionaly related to change in chemistry. As a key finding, surface-controlled equilibration kinetics seem to dominate transport-controlled processes in the investigated samples. This may be decisive information towards the understanding of age data derived from monazite.

Cold fission: splitting the pombe cell at room temperature.

The mechanisms responsible for cytokinesis and its coordination with other events of the cell cycle are poorly understood. Genetic studies of cytokinesis in fission yeast are one useful approach to this problem. A number of conditional mutants of fission yeast that show defects in the formation of the septum of cytokinesis have been identified. Cloning of the genes affected in these mutants has begun to shed light upon the elements required to direct the construction of the division septum and also upon how the initiation of septum formation may be coordinated with mitosis.

Understanding the low-temperature limitations to forest growth through calibration of a forest dynamics model with tree-ring data

The sensitivity of altitudinal and latitudinal tree-line ecotones to climate change, particularly that of temperature, has received much attention. To improve our understanding of the factors affecting tree-line position, we used the spatially explicit dynamic forest model TreeMig. Although well-suited because of its landscape dynamics functions, TreeMig features a parabolic temperature growth response curve, which has recently been questioned. and the species parameters are not specifically calibrated for cold temperatures. Our main goals were to improve the theoretical basis of the temperature growth response curve in the model and develop a method for deriving that curve's parameters from tree-ring data. We replaced the parabola with an asymptotic curve, calibrated for the main species at the subalpine (Swiss Alps: Pinus cembra, Larix decidua, Picea abies) and boreal (Fennoscandia: Pinus sylvestris, Betula pubescens, P. abies) tree-lines. After fitting new parameters, the growth curve matched observed tree-ring widths better. For the subalpine species, the minimum degree-day sum allowing, growth (kDDMin) was lowered by around 100 degree-days; in the case of Larix, the maximum potential ring-width was increased to 5.19 mm. At the boreal tree-line, the kDDMin for P. sylvestris was lowered by 210 degree-days and its maximum ring-width increased to 2.943 mm; for Betula (new in the model) kDDMin was set to 325 degree-days and the maximum ring-width to 2.51 mm; the values from the only boreal sample site for Picea were similar to the subalpine ones, so the same parameters were used. However, adjusting the growth response alone did not improve the model's output concerning species' distributions and their relative importance at tree-line. Minimum winter temperature (MinWiT, mean of the coldest winter month), which controls seedling establishment in TreeMig, proved more important for determining distribution. Picea, P. sylvestris and Betula did not previously have minimum winter temperature limits, so these values were set to the 95th percentile of each species' coldest MinWiT site (respectively -7, -11, -13). In a case study for the Alps, the original and newly calibrated versions of TreeMig were compared with biomass data from the National Forest Inventor), (NFI). Both models gave similar, reasonably realistic results. In conclusion, this method of deriving temperature responses from tree-rings works well. However, regeneration and its underlying factors seem more important for controlling species' distributions than previously thought. More research on regeneration ecology, especially at the upper limit of forests. is needed to improve predictions of tree-line responses to climate change further.

Time and temperature dependant changes in red blood cell analytes used for testing recombinant erythropoietin abuse in sports.

There has been a long debate since the introduction of blood analysis prior to major sports events, to find out whether blood samples should be analysed right away on the site of competition or whether they should be transported and analysed in an anti-doping laboratory. Therefore, it was necessary to measure blood samples and compare the results obtained right after the blood withdrawal with those obtained after a few hours delay. Furthermore, it was interesting to determine the effect of temperature on the possible deterioration of red blood cell analytes used for testing recombinant erythropoietin abuse. Healthy volunteers were asked to give two blood samples and one of these was kept at room temperature whereas the second one was put into a refrigerator. On a regular basis, the samples were rolled for homogenisation and temperature stabilisation and were analysed with the same haematological apparatus. The results confirmed that blood controls prior to competition should be performed as soon as possible with standardised pre-analytical conditions to avoid too many variations notably on the haematocrit and the reticulocyte count. These recommendations should ideally also be applied to the all the blood controls compulsory for the medical follow up, otherwise unexplainable values could be misinterpreted and could for instance lead to a period of incapacity.

Body temperature regulation and outcome after cardiac arrest and therapeutic hypothermia.

OBJECTIVE: Therapeutic temperature modulation is recommended after cardiac arrest (CA). However, body temperature (BT) regulation has not been extensively studied in this setting. We investigated BT variation in CA patients treated with therapeutic hypothermia (TH) and analyzed its impact on outcome. METHODS: A prospective cohort of comatose CA patients treated with TH (32-34°C, 24h) at the medical/surgical intensive care unit of the Lausanne University Hospital was studied. Spontaneous BT was recorded on hospital admission. The following variables were measured during and after TH: time to target temperature (TTT=time from hospital admission to induced BT target <34°C), cooling rate (spontaneous BT-induced BT target/TTT) and time of passive rewarming to normothermia. Associations of spontaneous and induced BT with in-hospital mortality were examined. RESULTS: A total of 177 patients (median age 61 years; median time to ROSC 25 min) were studied. Non-survivors (N=90, 51%) had lower spontaneous admission BT than survivors (median 34.5 [interquartile range 33.7-35.9]°C vs. 35.1 [34.4-35.8]°C, p=0.04). Accordingly, time to target temperature was shorter among non-survivors (200 [25-363]min vs. 270 [158-375]min, p=0.03); however, when adjusting for admission BT, cooling rates were comparable between the two outcome groups (0.4 [0.2-0.5]°C/h vs. 0.3 [0.2-0.4]°C/h, p=0.65). Longer duration of passive rewarming (600 [464-744]min vs. 479 [360-600]min, p<0.001) was associated with mortality. CONCLUSIONS: Lower spontaneous admission BT and longer time of passive rewarming were associated with in-hospital mortality after CA and TH. Impaired thermoregulation may be an important physiologic determinant of post-resuscitation disease and CA prognosis. When assessing the benefit of early cooling on outcome, future trials should adjust for patient admission temperature and use the cooling rate rather than the time to target temperature.

Deep accidental hypothermia with core temperature below 24°c presenting with vital signs.

Abstract Pasquier, Mathieu, Noemi Zurron, Barbara Weith, Pierre Turini, Fabrice Dami, Pierre-Nicolas Carron, and Peter Paal. Deep accidental hypothermia with core temperature below 24°C presenting with vital signs. High Alt Med Biol. 15:58-63, 2014.-Background: According to the Swiss hypothermia clinical staging, patients with stage III are unconscious with preserved vital signs, with core temperature usually between 24° and 28°C. With stage IV, vital signs are absent with core temperature <24°C. Aims: To describe a patient presenting with HT stage III with vital signs but a core temperature of <24°C, and to search for similar patients in the medical literature. Materials and methods: MEDLINE was used to search for cases of deep accidental hypothermia (<24°C) and preserved vital signs. Results: We found 22 cases in addition to our case (n=23). Median age was 44 years (IQR 36; range 4-83) and median core temperature 22°C (IQR 1.7; 17-23.8). Vital signs were often minimal. Seven patients developed ventricular fibrillation (VF). Twenty patients survived with excellent neurological outcome. Conclusions: Vital signs can be present in hypothermic patients with core temperature <24°C. In deeply hypothermic patients, a careful check and prolonged check of vital functions should be made, as vital signs may be minimal. The clinical Swiss staging remains valuable in the prehospital evaluation of hypothermic patients; its correlation with core temperature should be better defined.

Natural evidence for rapid abiogenic hydrothermal generation of CH4

Although recent hydrothermal experiments imply that abiogenic methane (CH4) generation from hydrothermal reduction of CO2 can occur, evidence from natural systems was still lacking. Based on the chemical and isotopic equilibrium signatures of low-temperature fumarolic gas discharges, we are able to provide hard evidence for its natural occurrence, namely in three subduction-related bi-phase hydrothermal systems of the Mediterranean, whose temperatures range from 260 to 470 degrees C. The attainment of equilibrium and the time spans of recent volcanic dormancy allowed us to calculate minimum rates for chemical and isotopic equilibration. These are significantly higher than those previously reported and might be due to the presence of a saturated water vapor phase in the investigated systems. The fact that nature provides conditions enabling relatively fast production of hydrocarbons from CO2 strongly supports the concerns that were recently raised from laboratory experiments. These address the use of the carbon isotope composition of reduced carbon in Archean sediments as a tracer of early life and the occurrence of CH4 on extraterrestrial planets as a bioindicator. In view of the potential role of abiogenic CH4 as a precursor of life, we also present an estimate of abiogenic hydrothermal CH4 fluxes throughout the Archean. It is not expected that these fluxes exceeded 80 Mt/yr during the past 4.0 Ga. This, however, would have been enough to facilitate HCN production on the prebiotic Earth. (C) 2007 Elsevier Ltd. All rights reserved.

Intra-individual variation in body temperature and pectoral muscle size in nestling Alpine swifts Apus melba in response to an episode of inclement weather

The Alpine swift (Apus melba) forages on insects caught exclusively on the wing, implying that dependent nestlings face acute food shortage in periods of cold and rainy weather. Therefore, there should be strong selection on nestling swifts to evolve physiological strategies to cope with periods of undernutrition. We have investigated intra-individual changes in nestling pectoral muscle and body temperature in response to a 1-week period of inclement weather. The pectoral muscle is the largest reserves of proteins, and nestlings have to devote a large amount of energy in the maintenance of body temperature. The results show that nestling pectoral muscle size and body temperature were significantly reduced during the episode of inclement weather. Assuming that these physiological changes are adaptive, our study suggests that nestling swifts spare energy by a pronounced reduction (up to 18 degrees C) in body temperature and use proteins from the pectoral muscle as a source of extra energy to survive prolonged periods of fasting.

Finding the right interactional temperature: do colder patients need more warmth in physician communication style?

Being aware of which communication style should be adopted when facing more difficult patients is important for physicians; it can help prevent patient reactions of dissatisfaction, mistrust, or non-adherence that can be detrimental to the process of care. Past research suggests that less agreeable patients are especially critical towards, and reactive to, their physician's communication style, compared to more agreeable patients. On the basis of the literature, we hypothesized that less agreeable patients would react more negatively than agreeable patients to lower levels of affiliativeness (i.e., warmth, friendliness) in the physicians, in terms of satisfaction with the physician, trust in the physician, and determination to adhere to the treatment. Thirty-six general practitioners (20 men/16 women) working in their own practice in Switzerland were filmed while interacting with 69 patients (36 men/33 women) of different ages (M = 50.7; SD = 18.19; range: 18-84) and presenting different medical problems (e.g., back pain, asthma, hypertension, diabetes). After the medical interview, patients filled in questionnaires measuring their satisfaction with the physician, their trust in the physician, their determination to adhere to the treatment, and their trait of agreeableness. Physician affiliativeness was coded on the basis of the video recordings. Physician gender and dominance, patient gender and age, as well as the gravity of the patient's medical condition were introduced as control variables in the analysis. Results confirmed our hypothesis for satisfaction and trust, but not for adherence; less agreeable patients reacted more negatively (in terms of satisfaction and trust) than agreeable patients to lower levels of affiliativeness in their physicians. This study suggests that physicians should be especially attentive to stay warm and friendly with people low in agreeableness because those patients' satisfaction and trust might be more easily lowered by a cold or distant physician communication style.

Application of low temperature thermochronology to understanding cooling and exhumation in the Central Swiss Alps

THESIS ABSTRACT : Low-temperature thermochronology relies on application of radioisotopic systems whose closure temperatures are below temperatures at which the dated phases are formed. In that sense, the results are interpreted as "cooling ages" in contrast to "formation ages". Owing to the low closure-temperatures, it is possible to reconstruct exhumation and cooling paths of rocks during their residence at shallow levels of the crust, i.e. within first ~10 km of depth. Processes occurring at these shallow depths such as final exhumation, faulting and relief formation are fundamental for evolution of the mountain belts. This thesis aims at reconstructing the tectono-thermal history of the Aar massif in the Central Swiss Alps by means of zircon (U-Th)/He, apatite (U-Th)/He and apatite fission track thermochronology. The strategy involved acquisition of a large number of samples from a wide range of elevations in the deeply incised Lötschen valley and a nearby NEAT tunnel. This unique location allowed to precisely constrain timing, amount and mechanisms of exhumation of the main orographic feature of the Central Alps, evaluate the role of topography on the thermochronological record and test the impact of hydrothermal activity. Samples were collected from altitudes ranging between 650 and 3930 m and were grouped into five vertical profiles on the surface and one horizontal in the tunnel. Where possible, all three radiometric systems were applied to each sample. Zircon (U-Th)/He ages range from 5.1 to 9.4 Ma and are generally positively correlated with altitude. Age-elevation plots reveal a distinct break in slope, which translates into exhumation rate increasing from ~0.4 to ~3 km/Ma at 6 Ma. This acceleration is independently confirmed by increased cooling rates on the order of 100°C/Ma constrained on the basis of age differences between the zircon (U-Th)/He and the remaining systems. Apatite fission track data also plot on a steep age-elevation curve indicating rapid exhumation until the end of the Miocene. The 6 Ma event is interpreted as reflecting tectonically driven uplift of the Aar massif. The late Miocene timing implies that the increase of precipitation in the Pliocene did not trigger rapid exhumation in the Aar massif. The Messinian salinity crisis in the Mediterranean could not directly intensify erosion of the Aar but associated erosional output from the entire Alps may have tapered the orogenic wedge and caused reactivation of thrusting in the Aar massif. The high exhumation rates in the Messinian were followed by a decrease to ~1.3 km/Ma as evidenced by ~8 km of exhumation during last 6 Ma. The slowing of exhumation is also apparent from apatite (U-Th)1He age-elevation data in the northern part of the Lötschen valley where they plot on a ~0.5km/Ma line and range from 2.4 to 6.4 Ma However, from the apatite (U-Th)/He and fission track data from the NEAT tunnel, there is an indication of a perturbation of the record. The apatite ages are youngest under the axis of the valley, in contrast to an expected pattern where they would be youngest in the deepest sections of the tunnel due to heat advection into ridges. The valley however, developed in relatively soft schists while the ridges are built of solid granitoids. In line with hydrological observations from the tunnel, we suggest that the relatively permeable rocks under the valley floor, served as conduits of geothermal fluids that caused reheating leading to partial Helium loss and fission track annealing in apatites. In consequence, apatite ages from the lowermost samples are too young and the calculated exhumation rates may underestimate true values. This study demonstrated that high-density sampling is indispensable to provide meaningful thermochronological data in the Alpine setting. The multi-system approach allows verifying plausibility of the data and highlighting sources of perturbation. RÉSUMÉ DE THÈSE : La thermochronologie de basse température dépend de l'utilisation de systèmes radiométriques dont la température de fermeture est nettement inférieure à la température de cristallisation du minéral. Les résultats obtenus sont par conséquent interprétés comme des âges de refroidissement qui diffèrent des âges de formation obtenus par le biais d'autres systèmes de datation. Grâce aux températures de refroidissement basses, il est aisé de reconstruire les chemins de refroidissement et d'exhumation des roches lors de leur résidence dans la croute superficielle (jusqu'à 10 km). Les processus qui entrent en jeu à ces faibles profondeurs tels que l'exhumation finale, la fracturation et le faillage ainsi que la formation du relief sont fondamentaux dans l'évolution des chaînes de montagne. Ces dernières années, il est devenu clair que l'enregistrement thermochronologique dans les orogènes peut être influencé par le relief et réinitialisé par l'advection de la chaleur liée à la circulation de fluides géothermaux après le refroidissement initial. L'objectif de cette thèse est de reconstruire l'histoire tectono-thermique du massif de l'Aar dans les Alpes suisses Centrales à l'aide de trois thermochronomètres; (U-Th)/He sur zircon, (U-Th)/He sur apatite et les traces de fission sur apatite. Afin d'atteindre cet objectif, nous avons récolté un grand nombre d'échantillons provenant de différentes altitudes dans la vallée fortement incisée de Lötschental ainsi que du tunnel de NEAT. Cette stratégie d'échantillonnage nous a permis de contraindre de manière précise la chronologie, les quantités et les mécanismes d'exhumation de cette zone des Alpes Centrales, d'évaluer le rôle de la topographie sur l'enregistrement thermochronologique et de tester l'impact de l'hydrothermalisme sur les géochronomètres. Les échantillons ont été prélevés à des altitudes comprises entre 650 et 3930m selon 5 profils verticaux en surface et un dans le tunnel. Quand cela à été possible, les trois systèmes radiométriques ont été appliqués aux échantillons. Les âges (U-Th)\He obtenus sur zircons sont compris entre 5.l et 9.4 Ma et sont corrélés de manière positive avec l'altitude. Les graphiques représentant l'âge et l'élévation montrent une nette rupture de la pente qui traduisent un accroissement de la vitesse d'exhumation de 0.4 à 3 km\Ma il y a 6 Ma. Cette accélération de l'exhumation est confirmée par les vitesses de refroidissement de l'ordre de 100°C\Ma obtenus à partir des différents âges sur zircons et à partir des autres systèmes géochronologiques. Les données obtenues par traces de fission sur apatite nous indiquent également une exhumation rapide jusqu'à la fin du Miocène. Nous interprétons cet évènement à 6 Ma comme étant lié à l'uplift tectonique du massif de l'Aar. Le fait que cet évènement soit tardi-miocène implique qu'une augmentation des précipitations au Pliocène n'a pas engendré cette exhumation rapide du massif de l'Aar. La crise Messinienne de la mer méditerranée n'a pas pu avoir une incidence directe sur l'érosion du massif de l'Aar mais l'érosion associée à ce phénomène à pu réduire le coin orogénique alpin et causer la réactivation des chevauchements du massif de l'Aar. L'exhumation rapide Miocène a été suivie pas une diminution des taux d'exhumation lors des derniers 6 Ma (jusqu'à 1.3 km\Ma). Cependant, les âges (U-Th)\He sur apatite ainsi que les traces de fission sur apatite des échantillons du tunnel enregistrent une perturbation de l'enregistrement décrit ci-dessus. Les âges obtenus sur les apatites sont sensiblement plus jeunes sous l'axe de la vallée en comparaison du profil d'âges attendus. En effet, on attendrait des âges plus jeunes sous les parties les plus profondes du tunnel à cause de l'advection de la chaleur dans les flancs de la vallée. La vallée est creusée dans des schistes alors que les flancs de celle-ci sont constitués de granitoïdes plus durs. En accord avec les observations hydrologiques du tunnel, nous suggérons que la perméabilité élevée des roches sous l'axe de la vallée à permi l'infiltration de fluides géothermaux qui a généré un réchauffement des roches. Ce réchauffement aurait donc induit une perte d'Hélium et un recuit des traces de fission dans les apatites. Ceci résulterait en un rajeunissement des âges apatite et en une sous-estimation des vitesses d'exhumation sous l'axe de la vallée. Cette étude à servi à démontrer la nécessité d'un échantillonnage fin et précis afin d'apporter des données thermochronologiques de qualité dans le contexte alpin. Cette approche multi-système nous a permi de contrôler la pertinence des données acquises ainsi que d'identifier les sources possibles d'erreurs lors d'études thermochronologiques. RÉSUMÉ LARGE PUBLIC Lors d'une orogenèse, les roches subissent un cycle comprenant une subduction, de la déformation, du métamorphisme et, finalement, un retour à la surface (ou exhumation). L'exhumation résulte de la déformation au sein de la zone de collision, menant à un raccourcissement et un apaissessement de l'édifice rocheux, qui se traduit par une remontée des roches, création d'une topographie et érosion. Puisque l'érosion agit comme un racloir sur la partie supérieure de l'édifice, des tentatives de corrélation entre les épisodes d'exhumation rapide et les périodes d'érosion intensive, dues aux changements climatiques, ont été effectuées. La connaissance de la chronologie et du lieu précis est d'une importance capitale pour une quelconque reconstruction de l'évolution d'une chaîne de montagne. Ces critères sont donnés par un retraçage des changements de la température de la roche en fonction du temps, nous donnant le taux de refroidissement. L'instant auquel les roches ont refroidit, passant une certaine température, est contraint par l'application de techniques de datation par radiométrie. Ces méthodes reposent sur la désintégration des isotopes radiogéniques, tels que l'uranium et le potassium, tous deux abondants dans les roches de la croûte terrestre. Les produits de cette désintégration ne sont pas retenus dans les minéraux hôtes jusqu'au moment du refroidissement de la roche sous une température appelée 'de fermeture' , spécifique à chaque système de datation. Par exemple, la désintégration radioactive des atomes d'uranium et de thorium produit des atomes d'hélium qui s'échappent d'un cristal de zircon à des températures supérieures à 200°C. En mesurant la teneur en uranium-parent, l'hélium accumulé et en connaissant le taux de désintégration, il est possible de calculer à quel moment la roche échantillonnée est passée sous la température de 200°C. Si le gradient géothermal est connu, les températures de fermeture peuvent être converties en profondeurs actuelles (p. ex. 200°C ≈ 7km), et le taux de refroidissement en taux d'exhumation. De plus, en datant par système radiométrique des échantillons espacés verticalement, il est possible de contraindre directement le taux d'exhumation de la section échantillonnée en observant les différences d'âges entre des échantillons voisins. Dans les Alpes suisses, le massif de l'Aar forme une structure orographique majeure. Avec des altitudes supérieures à 4000m et un relief spectaculaire de plus de 2000m, le massif domine la partie centrale de la chaîne de montagne. Les roches aujourd'hui exposées à la surface ont été enfouies à plus de 10 km de profond il y a 20 Ma, mais la topographie actuelle du massif de l'Aar semble surtout s'être développée par un soulèvement actif depuis quelques millions d'années, c'est-à-dire depuis le Néogène supérieur. Cette période comprend un changement climatique soudain ayant touché l'Europe il y a environ 5 Ma et qui a occasionné de fortes précipitations, entraînant certainement une augmentation de l'érosion et accélérant l'exhumation des Alpes. Dans cette étude, nous avons employé le système de datation (U-TH)/He sur zircon, dont la température de fermeture de 200°C est suffisamment basse pour caractériser l'exhumation du Néogène sup. /Pliocène. Les échantillons proviennent du Lötschental et du tunnel ferroviaire le plus profond du monde (NEAT) situé dans la partie ouest du massif de l'Aar. Considérés dans l'ensemble, ces échantillons se répartissent sur un dénivelé de 3000m et des âges de 5.1 à 9.4 Ma. Les échantillons d'altitude supérieure (et donc plus vieux) documentent un taux d'exhumation de 0.4 km/Ma jusqu'à il y a 6 Ma, alors que les échantillons situés les plus bas ont des âges similaires allant de 6 à 5.4 Ma, donnant un taux jusqu'à 3km /Ma. Ces données montrent une accélération dramatique de l'exhumation du massif de l'Aar il y a 6 Ma. L'exhumation miocène sup. du massif prédate donc le changement climatique Pliocène. Cependant, lors de la crise de salinité d'il y a 6-5.3 Ma (Messinien), le niveau de la mer Méditerranée est descendu de 3km. Un tel abaissement de la surface d'érosion peut avoir accéléré l'exhumation des Alpes, mais le bassin sud alpin était trop loin du massif de l'Aar pour influencer son érosion. Nous arrivons à la conclusion que la datation (U-Th)/He permet de contraindre précisément la chronologie et l'exhumation du massif de l'Aar. Concernant la dualité tectonique-érosion, nous suggérons que, dans le cas du massif de l'Aar, la tectonique prédomine.