Neonatal and adult ICU ventilators to provide ventilation in neonates, infants, and children: a bench model study.

BACKGROUND: Using a bench test model, we investigated the hypothesis that neonatal and/or adult ventilators equipped with neonatal/pediatric modes currently do not reliably administer pressure support (PS) in neonatal or pediatric patient groups in either the absence or presence of air leaks. METHODS: PS was evaluated in 4 neonatal and 6 adult ventilators using a bench model to evaluate triggering, pressurization, and cycling in both the absence and presence of leaks. Delivered tidal volumes were also assessed. Three patients were simulated: a preterm infant (resistance 100 cm H2O/L/s, compliance 2 mL/cm H2O, inspiratory time of the patient [TI] 400 ms, inspiratory effort 1 and 2 cm H2O), a full-term infant (resistance 50 cm H2O/L/s, compliance 5 mL/cm H2O, TI 500 ms, inspiratory effort 2 and 4 cm H2O), and a child (resistance 30 cm H2O/L/s, compliance 10 mL/cm H2O, TI 600 ms, inspiratory effort 5 and 10 cm H2O). Two PS levels were tested (10 and 15 cm H2O) with and without leaks and with and without the leak compensation algorithm activated. RESULTS: Without leaks, only 2 neonatal ventilators and one adult ventilator had trigger delays under a given predefined acceptable limit (1/8 TI). Pressurization showed high variability between ventilators. Most ventilators showed TI in excess high enough to seriously impair patient-ventilator synchronization (> 50% of the TI of the subject). In some ventilators, leaks led to autotriggering and impairment of ventilation performance, but the influence of leaks was generally lower in neonatal ventilators. When a noninvasive ventilation algorithm was available, this was partially corrected. In general, tidal volume was calculated too low by the ventilators in the presence of leaks; the noninvasive ventilation algorithm was able to correct this difference in only 2 adult ventilators. CONCLUSIONS: No ventilator performed equally well under all tested conditions for all explored parameters. However, neonatal ventilators tended to perform better in the presence of leaks. These findings emphasize the need to improve algorithms for assisted ventilation modes to better deal with situations of high airway resistance, low pulmonary compliance, and the presence of leaks.

Etat de stress post-traumatique chez les mères et les pères d'enfants prématurés : similitudes et différences

Rapport de synthèse : Cette étude réalisée conjointement par les services de pédopsychiatrie et de néonatologie du Centre Hospitalier Universitaire Vaudois (CHUV), Lausanne, Suisse, s'inscrit dans un groupe de publications issues d'un projet portant sur les représentations parentales et le devenir de 1a prématurité, financée par le Fonds National de la Recherche Scientifique entre 1998 et 2002 (FNRS 32-49712.96), soutenue par la Fondation de la Psychiatrie pour la Petite Enfance. Elle à pour objectifs d'évaluer et de compazer la présence de symptômes de stress post-traumatique; en fonction de la gravité de la prématurité, chez les mères et chez les pères de bébés nés prématurément. Population et Méthode : en fonction du score de risque périnatal (PERI) du bébé, les parents des prématurés (âge gestationnel < 34 semaines) ont été divisés en deux groupes : les parents de prématurés à faible risque (n = 16) et à haut risque (n = 26). Les symptômes d'intrusion et d'évitement, de l'état de stress post-traumatique, ont été évalués chez les parents à l'aide d'un questionnaire rempli par les parents, l'Impact of Event Scale (IES). Leurs réponses ont été comparées à un groupe contrôle de parents de nouveau-nés à terme (n = 24). Les différences entre les réponses des mères et des pères, ont été analysées. Résultats : les parents de bébés prématurés sont plus à risque que les parents de nouveau-nés à terme, de présenter des symptômes de stress post-traumatique. Les mères en lien avec le fait même de la prématurité du bébé, les pères en lien avec la gravité de la prématurité. Les mèrés et les pères des prématurés des deux groupes (prématurés à faible risque, prématurés à haut risque) décrivent des symptômes d'intrusion, alors que les symptômes d'évitement sont décrits par toutes les mères, mais seulement par les pères de prématurés à haut risque périnatal. Le vécu particulier des parents, ainsi que les enjeux différents pour les mères et les pères lors d'une naissance prématurée, sont ainsi mis en évidence. La prise en compte de ces différences devrait influencer les interventions des pédopsychiatres et des équipes de néonatologie qui interviennent auprès des parents et guident la construction des liens avec le bébé né prématurément. Publiée par la revue «Neuropsychiatrie de l'enfance et de l'adolescence », aux éditions Elsevier Masson sous le titre : « Etat de stress post-traumatique chez les mères et chez les pères d'enfants prématurés : similitudes et différences» ; numéró 57 (2009) 385-391.

The Tertiary structural and thermal evolution of the central Alps - Compressional and extensional structures in an orogenic belt

The Western Alpine Are has been created during the Cretaceous and the Tertiary orogenies. The interference patterns of the Tertiary structures suggest their formation during continental collision of the European and the Adriatic Plates, with an accompanying anticlockwise rotation of the Adriatic indenter. Extensional structures are mainly related to ductile deformation by simple shear. These structures developed at a deep tectonic level, in granitic crustal rocks, at depths in excess of 10 km. In the early Palaeogene period of the Tertiary Orogeny, the main Tertiary nappe emplacement resulted from a NW-thrusting of the Austroalpine, Penninic and Helvetic nappes. Heating of the deep zone of the Upper Cretaceous and Tertiary nappe stack by geothermal heat flow is responsible for the Tertiary regional metamorphism, reaching amphibolite-facies conditions in the Lepontine Gneiss Dome (geothermal gradient 25 degrees C/ km). The Tertiary thrusting occurred mainly during prograde metamorphic conditions with creation of a penetrative NW-SE-oriented stretching lineation, X(1) (finite extension), parallel to the direction of simple shear. Earliest cooling after the culmination of the Tertiary metamorphism, some 38 Ma ago, is recorded by the cooling curves of the Monte Rosa and Mischabel nappes to the west and the Suretta Nappe to the east of the Lepontine Gneiss Dome. The onset of dextral transpression, with a strong extension parallel to the mountain belt, and the oldest S-vergent `'backfolding'' took place some 35 to 30 Ma ago during retrograde amphibolite-facies conditions and before the intrusion of the Oligocene dikes north of the Periadriatic Line. The main updoming of the Lepontine Gneiss Dome started some 32-30 Ma ago with the intrusion of the Bergell tonalites and granodiorites, concomitant with S-vergent backfolding and backthrusting and dextral strike-slip movements along the Tonale and Canavese Lines (Argand's Insubric phase). Subsequently, the center of main updoming migrated slowly to the west, reaching the Simplon region some 20 Ma ago. This was contemporaneous with the westward migration of the Adriatic indenter. Between 20 Ma and the present, the Western Aar Massif-Toce culmination was the center of strong uplift. The youngest S-vergent backfolds, the Glishorn anticline and the Berisal syncline fold the 12 Ma Rb/Sr biotite isochron and are cut by the 11 Ma old Rhone-Simplon Line. The discrete Rhone-Simplon Line represents a late retrograde manifestation in the preexisting ductile Simplon Shear Zone. This fault zone is still active today. The Oligocene-Neogene dextral transpression and extension in the Simplon area were concurrent with thrusting to the northwest of the Helvetic nappes, the Prealpes (35-15 Ma) and with the Jura thin-skinned thrust (11-3 Ma). It was also contemporaneous with thrusting to the south of the Bergamasc (> 35-5 Ma) and Milan thrusts (16-5 Ma).

Effect of expiratory positive airway pressure on sleep disordered breathing.

STUDY OBJECTIVES: We sought to determine the effect of expiratory positive airway pressure on end expiratory lung volume (EELV) and sleep disordered breathing in obstructive sleep apnea patients. DESIGN: Observational physiology study PARTICIPANTS: We studied 10 OSA patients during sleep wearing a facial mask. We recorded 1 hour of NREM sleep without treatment (baseline) and 1 hour with 10 cm H2O EPAP in random order, while measuring EELV and breathing pattern. RESULTS: The mean EELV change between baseline and EPAP was only 13.3 mL (range 2-25 mL). Expiratory time was significantly increased with EPAP compared to baseline 2.64 +/- 0.54 vs 2.16 +/- 0.64 sec (P = 0.002). Total respiratory time was longer with EPAP than at baseline 4.44 +/- 1.47 sec vs 3.73 +/- 0.88 sec (P = 0.3), and minute ventilation was lower with EPAP vs baseline 7.9 +/- 4.17 L/min vs 9.05 +/- 2.85 L/min (P = 0.3). For baseline (no treatment) and EPAP respectively, the mean apnea+hypopnea index (AHI) was 62.6 +/- 28.7 and 56.8 +/- 30.3 events per hour (P = 0.4). CONCLUSION: In OSA patients during sleep, the application of 10 cm H2O EPAP led to prolongation of expiratory time with only marginal increases in FRC. These findings suggest important mechanisms exist to avoid hyperinflation during sleep.

Time resolved construction of a bimodal laccolith (Torres del Paine, Patagonia)

Granitic and mafic magma pulses were sequentially accreted in the spectacularly exposed shallow crustal Torres del Paine laccolith, in southern Patagonia. This 12.5 Ma pluton forms a composite intrusion with a subvertical feeding system in the west and a laccolith in the east. A key unknown in the formation of sill complexes is how individual magma pulses are assembled over time and the geometry and localization of their feeding system. High resolution zircon CA-ID-TIMS U-Pb dating shows that the laccolith grew first by under-accretion of granitic sills over 90 +/- 30 ka, linked to a `sheet-like' feeding system, followed by underplating of mafic sills after similar to 20 ka of quiescence. In the mafic sills complex, individual sills were injected by over-accretion during 41 +/- 11 ka. Our data show that successive granitic and mafic magmas emplacement generated a volume of similar to 88 km(3) in 162 +/- 11 ka. (C) 2012 Elsevier B.V. All rights reserved.

Trazodone increases arousal threshold in obstructive sleep apnoea.

A low arousal threshold is believed to predispose to breathing instability during sleep. The present authors hypothesised that trazodone, a nonmyorelaxant sleep-promoting agent, would increase the effort-related arousal threshold in obstructive sleep apnoea (OSA) patients. In total, nine OSA patients, mean+/-sd age 49+/-9 yrs, apnoea/hypopnoea index 52+/-32 events.h(-1), were studied on 2 nights, one with trazodone at 100 mg and one with a placebo, in a double blind randomised fashion. While receiving continuous positive airway pressure (CPAP), repeated arousals were induced: 1) by increasing inspired CO(2) and 2) by stepwise decreases in CPAP level. Respiratory effort was measured with an oesophageal balloon. End-tidal CO(2 )tension (P(ET,CO(2))) was monitored with a nasal catheter. During trazodone nights, compared with placebo nights, the arousals occurred at a higher P(ET,CO(2)) level (mean+/-sd 7.30+/-0.57 versus 6.62+/-0.64 kPa (54.9+/-4.3 versus 49.8+/-4.8 mmHg), respectively). When arousals were triggered by increasing inspired CO(2) level, the maximal oesophageal pressure swing was greater (19.4+/-4.0 versus 13.1+/-4.9 cm H(2)O) and the oesophageal pressure nadir before the arousals was lower (-5.1+/-4.7 versus -0.38+/-4.2 cm H(2)O) with trazodone. When arousals were induced by stepwise CPAP drops, the maximal oesophageal pressure swings before the arousals did not differ. Trazodone at 100 mg increased the effort-related arousal threshold in response to hypercapnia in obstructive sleep apnoea patients and allowed them to tolerate higher CO(2) levels.

Volutrauma activates the clotting cascade in the newborn but not adult rat.

Coagulopathy and alveolar fibrin deposition are common in sick neonates and attributed to the primary disease, as opposed to their ventilatory support. Hypothesizing that high tidal volume ventilation activates the extrinsic coagulation pathway, we air ventilated newborn and adult rats at low (10 ml/kg) or high (30 ml/kg) tidal volume and compared them with age-matched nonventilated controls. Blood was collected at the end of the experiment for measurement of clot time, tissue factor, and other coagulation factor content. Similar measurements were obtained from lung lavage material. The newborn clot time (44+/-1) was lower and plasma tissue factor content higher (103.4+/-0.4) than adults (88+/-4 s and 26.6+/-1.4 units; P<0.01). High, but not low, tidal volume ventilation of newborns for as little as 15 min significantly reduced clot time and increased plasma tissue factor content (P<0.01). High volume ventilation increased plasma factor Xa (0.1+/-0.1 to 1.6+/-0.4 nM; P<0.01) and thrombin (1.3+/-0.2 to 2.2+/-0.4 nM; P<0.05) and decreased antithrombin (0.12+/-0.01 to 0.05+/-0.01; P<0.01) in the newborn. Lung lavage material of high volume-ventilated newborns showed increased (P<0.01) factor Xa and thrombin. No changes in these parameters were observed in adult rats that were high volume ventilated for up to 90 min. Compared with adults, newborn rats have a greater propensity for volutrauma-activated intravascular coagulation. These data suggest that mechanical ventilation promotes neonatal thrombosis via lung tissue factor release.

Bitumens in the late Variscan hydrothermal vein-type uranium deposit of Pribram, Czech Republic: Sources, radiation-induced alteration, and relation to mineralization

The late Variscan (275-278 Ma) Pribram uranium deposit is one of the largest known accumulations of uraniferous bitumens in hydrothermal veins. The deposit extends along the northwestern boundary of the Central Bohemian pluton (345-335 Ma) with low-grade metamorphosed Late Proterozoic and unmetamorphosed Cambrian rocks. From a net uranium production of 41,742 metric tons (t), more than 6,000 t were extracted from bitumen-uraninite ores during 43 years of exploration and mining. Three morphological varieties of solid bitumen are recognized: globular, asphaltlike, and cokelike. While the globular bitumen is uranium free, the other two types are uraniferous. The amount of bitumen in ore veins gradually decreases toward the contact with the plutonic body and increases with depth. Two types of bitumen microtextures are recognized using high-resolution transmission electron microscopy: amorphous and microporous, the former being less common in uraniferous samples. A lower Raman peak area ratio (1,360/1,575 cm(-1)) in mineralized bitumens (0.9) compared with uranium-free samples (2.0) indicates a lower degree of microtextural organization in the latter The H/C and O/C atomic ratios in uranium-free bitumens (0.9-1.1 and 0.09, respectively) are higher than those in mineralized samples (H/C = 0.3-0.8, O/C = 0.03-0.09). The chloroform extractable matter yield is Very low in uranium-free bitumens (0.30-0.35% of the total organic carbon,TOC) and decreases with uranium content increase. The extracted solid uraniferous bitumen infrared spectra show depletion in aliphatic CH2 and CH3 groups compared to uranium-free samples. The concentration of oxygen-bearing functional groups relative to aromatic bonds in the IR spectra of uranium-free and mineralized bitumen, however, do not differ significantly. C-13 NMR confirmed than the aromaticity of a uraniferous sample is higher (F-ar = 0.61) than in the uranium-free bitumen (F-ar = 0.51). Pyrolysates from uraniferous and nonuraniferous bitumens do not differ significantly, being predominantly cresol, alkylphenols, alkylbenzenes, and alkylnaphthalenes. The liquid pyrolysate yield decreases significantly with increasing uranium content. The delta(13)C Values of bulk uranium-free bitumens and low-grade uraniferous, asphaltlike bitumens range from -43.6 to 52.3 per mil. High-grade, cokelike, uraniferous bitumens are more C-13 depleted (54.5 to -58.4 parts per thousand). In contrast to the very light isotopic ratios of the high-grade uraniferous cokelike bitumen bulk carbon, the individual n-alkanes and isoprenoids (pristane and phytane) extracted from the same sample are significantly C-13 enriched. The isotopic composition of the C13-24 n-alkanes extracted from the high-grade uraniferous sample (delta(13)C = -28.0 to 32.6 parts per thousand) are heavier compared with the same compounds in a uranium-free sample (delta(13)C = 31.9 to 33.8 parts per thousand). It is proposed that the bitumen source was the isotopically light (delta(13)C = 35.8 to 30.2 parts per thousand) organic matter of the Upper Proterozoic host rocks that were pyrolyzed during intrusion of the Central Bohemian pluton. The C-13- depleted pyrolysates were mobilized from the innermost part of the contact-metamorphic aureole, accumulated in structural traps in less thermally influenced parts of the sedimentary complex and were later extracted by hydrothermal fluids. Bitumens at the Pribram deposit are younger than the main part of the uranium mineralization and were formed through water-washing and radiation-induced polymerization of both the gaseous and liquid pyrolysates. Direct evidence for pyrolysate reduction of uranium in the hydrothermal system is difficult to obtain as the chemical composition of the original organic fluid phase was modified during water-washing and radiolytic alteration. However, indirect evidence-e.g., higher O/C atomic ratios in uranium-free bitumens (0.1) relative to the Upper Proterozoic source rocks (0.02-0.05), isotopically very light carbon in associated whewellite (delta(13)C = 31.7 to -28.4 parts per thousand), and the striking absence of bitumens in the pre-uranium, hematite stage of the mineralization-indicates that oxidation of organic fluids may have contributed to lowering of aO(2) and uraninite precipitation.

Respiratory variability in mechanically ventilated patients. Critical Care 2011

Introduction: Increased respiratory pattern variability is associated with improved oxygenation. Pressure support (PS) is a widely used partial-assist mechanical ventilation (MV) mode, in which each breathing cycle is initiated by flow or pressure variation at the airway due to patient inspiratory effort. Neurally adjusted ventilatory assist (NAVA) is relatively new and uses the electrical activity of the diaphragm (Eadi) to deliver ventilatory support proportional to the patient's inspiratory demand. We hypothesize that respiratory variability should be greater with NAVA compared with PS.Methods: Twenty-two patients underwent 20 minutes of PS followed by 20 minutes of NAVA. Flow and Eadi curves were used to obtain tidal volume (Vt) and ∫Eadi for 300 to 400 breaths in each patient. Patient-specific cumulative distribution functions (CDF) show the percentage Vt and ∫Eadi within a clinically defined (±10%) variability band for each patient. Values are normalized to patient-specific medians for direct comparison. Variability in Vt (outcome) is thus expressed in terms of variability in ∫Eadi (demand) on the same plot.Results: Variability in Vt relative to variability in ∫Eadi is significantly greater for NAVA than PS (P = 0.00012). Hence, greater variability in outcome Vt is obtained for a given demand in ∫Eadi, under NAVA, as illustrated in Figure 1 for a typical patient. A Fisher 2 × 2 contingency analysis showed that 45% of patients under NAVA had a Vt variability in equal proportion to ∫Eadi variability, versus 0% for PS (P < 0.05).Conclusions: NAVA yields greater variability in tidal volume, relative to ∫Eadi demand, and a better match between Vt and ∫Eadi. These results indicate that NAVA could achieve improved oxygenation compared with PS when sufficient underlying variability in ∫Eadi is present, due to its ability to achieve higher tidal volume variability from a given variability in ∫Eadi.

Cardiovascular patterns associated with appetitive and defensive activation during affective picture viewing

Descriptors: cardiovascular patterns, emotion, affective pictures In this study we assessed blood pressure (BP), heart rate (HR), stroke volume (SV), cardiac output (CO), and total peripheral resistance (TPR) in response to 13 picture series in 18 men and 19 women in order to investigate their hemodynamic responses associated with activation of the appetitive and defensive motivational systems underlying emotional experience. Skin conductance level (SCL) was also recorded. BP and SV increased with increasing self-rated arousal both for appetitive and defensive activation, whereas HR decelerated more in response to negative than positive and neutral pictures. TPR showed a general increase from baseline to picture processing but was unrelated to self-rated valence and arousal. These findings suggest that affective modulation of the cardiovascular response to affective pictures is primarily myocardial. The observed response pattern is consistent with a configuration of cardiac sympathetic-parasympathetic coactivation. The relationships between self-reported arousal, BP and SV were mainly exhibited by men suggesting that increases in the sympathetic inotropic effect to the heart with increasing self-rated arousal might be larger in men than in women. In contrast, SCL covaried positively with self-rated arousal both in men and women. This suggests that sex differences in the affective modulation of the responses to pictures may be restricted to specific cardiovascular parameters and support the contention that the sympathetic nervous system does not discharge as a whole.

Petrology and chemistry of the Chalten Plutonic Complex and implications on the magmatic and tectonic evolution of the Southernmost Andes (Patagonia) during the Miocene

Résumé Scientific:Pétrologie et Géochimie du Complexe Plutonique de Chaltén et les conséquences pour l'évolution magmatique et tectonique du Andes du Sud (Patagonia) pendant le MiocèneLe sujet de cette thèse est le Complexe Plutonique de Chaltén (CHPC), situé à la frontière entre le Chili et l'Argentine, en Patagonie (49°15'S). Ce complexe s'est mis en place au début du Miocène, dans un contexte de changements tectoniques importants. La géométrie et la vitesse de migration des plaques en Patagonie a été modifiée suite l'ouverture de la plaque Farallon il y a 25Ma (Pardo-Casas and Molnar 1987) et la subduction de la ride active du Chili sous la plaque sud-américaine il y a 14Ma (Cande and Leslie 1986). Les effets de cette reconfiguration tectonique sur la morphologie et le magmatisme de la plaque supérieure sont encore sujets à discussion. Dans ce contexte, un groupe d'intrusions miocènes - telle que le CHPC - est particulièrement intriguant, car en position transitionnelle entre le batholithe patagonien et l'arc volcanique cénozoïque et récent à l'ouest, et les laves de plateau de Patagonie à l'est (Fig. 1). A cause de leur position tectonique transitoire, ces plutons isolés hors du batholithe représentent un endroit clé pour comprendre les interactions entre la tectonique à large échelle et le magmatisme en Patagonie. Ici, je présente de nouvelles données de terrain, petrologiques, géochimiques et géochronologiques dans le but de caractériser la nature du CHPC, qui était largement inconnu avant cette étude, dans le but de tester l'hypothèse de migration de l'arc et erosion par subduction.Les résultats de l'investigation géochimique (chapitre 2) montrent que le CHPC n'est qu'un exemple parmi les plutons isolés d'arrière arc ave une composition calco-alcaline caractéristique, c-à-d une signature d'arc. La plupart de ces plutons isolés ont une composition alcaline. Le CHPC, contrairement, a une signature calco-alcaline avec Κ intermédiaire, tel que le batholithe patagonien et la plupart des roches volcaniques quaternaires liées à l'arc le long des Andes.De nouvelles données géochronologiques U-Pb de haute précision sur des zircons, acquis par TIMS, sur le CHPC donnent des âges entre 17.0 et 16.4Ma. Les âges absolus sont en accord avec la séquence intrusive déduite des relations de terrain (chapitre 1). Ces données sont les premières contraintes d'âge U-Pb sur le CHPC. Elles montrent clairement que l'histoire magmatique du CHPC n'a pas de lien direct avec la subduction de la ride à cette latitude (Cande and Leslie 1986), car le complexe est au moins 6Ma plus ancien.Une comparaison en profondeur avec les autres intrusions d'âge Miocène en Patagonie révèlent - pour la première fois - une évolution temporelle intéressante. Il y a une tendance E-W distincte au magmatisme calco-alcalin entre 20-16Ma avec une diminution de l'âge vers l'est - le CHPC est l'expression la plus orientale de cette tendance. Je suggère que la relation espace-temps reflète une migration vers l'est (vers le continent) de l'arc magmatique. Je propose que le facteur principal contrôlant cette migration est la subduction rapide suite à la reconfiguration de la vitesse des plaques tectoniques après l'ouverture la plaque Farallon (à ~26Ma) qui résulterait en une déformation importante ainsi qu'à des taux élevés d'érosion dans la fosse de subduction.Les rapports d'isotopes radiogéniques (Pb, Sr, Nd) élevés, une signature 6018 basse et un rapport Th/La élevé sont des paramètres distinctifs pour les roches mafiques du CHPC. Le modèle isotopique présenté (chapitre 2) suggère que cette signature reflète une contamination de la source, dans le coin de manteau, plutôt qu'une contamination crustale. La signature des éléments en trace du CHPC indiquent que le coin de manteau a été contaminé par des composés terrigènes, le plus vraisemblablement par des sédiments paléozoïques.Les travaux de terrain, la pétrographie et la géothermobarométrie ont été utilisés dans le but de comprendre l'histoire interne du CHPC (chapitre 3). Ces données suggèrent deux niveaux distincts de cristallisation : l'un dans la croûte moyenne (6 à 4.5kbar) et l'autre à un niveau peu profond (3.5 à 2kbar). La modélisation isotopique AFC de la contamination crustale indique des taux variables d'assimilation, qui ne sont pas corrélés avec le degré de différenciation. Cela suggère que différents volumes de magma se sont différenciés en profondeur, de façon indépendante. Cela implique que le CHPC se serait formés en plusieurs puises de magmas provenant d'au moins trois sources différentes. Les textures des granodiorites et des granites indiquent des teneurs élevées en cristaux avant la mise en place et, par conséquent, des températures d'emplacement faibles. Les observations de terrain montrent que les roches mafiques sont déformées, alors que ce n'est pas le cas pour les granodiorites et granites (plus jeunes). La déformation des roches mafiques est encore sujet de recherche, afin de savoir si elle est liée à la déformation régionale en régime compressif ou à l'emplacement lui-même. Cependant, la mise en place de grand volume de magma felsique riche en cristaux suggère un régime d'extension.Scientific Abstract:Petrology and chemistry of the Chaltén Plutonic Complex and implications on the magmatic and tectonic evolution of the Southernmost Andes (Patagonia) during the MioceneThe subject of this thesis is the Chaltén Plutonic Complex (CHPC) located at the frontier between Chile and Argentina in Patagonia (at 49° 15 'Southern latitude). This complex intruded during early Miocene in a context of major tectonics changes. The plate geometry of Patagonia has been modified by changes in the plate motions after the break up of the Farallôn plate at 25Ma (Pardo-Casas and Molnar 1987) and by the subduction of the Chile spreading Ridge beneath South-America at 14 Ma (Cande and Leslie 1986). The effects of this tectonic setting on the morphology and the magmatism of the overriding plate are a matter of on-going discussion. Particularly intriguing in this context is a group of isolated Miocene intrusions - like the CHPC - which are located in a transitional position between the Patagonian Batholith and the Cenozoic and Recent volcanic arc in the West, and the Patagonian plateau lavas in the East (Fig. 1). Due to their transient tectonic position these isolated plutons outside the batholith represent a key to understanding the interaction between global-scale tectonics and magmatism in Patagonia. Here, I present new field, penological, geochemical and geochronological data to characterize the nature of the CHPC, which was largely unknown before this study, in order to test the hypothesis of time- transgressive magmatism.The results of the geochemical investigation (Chapter 2) show that the CHPC is only one among these isolated back-arc plutons with a characteristic calc-alkaline composition, i.e. arc signature. Most of these isolated intrusives have an alkaline character. The CHPC, in contrast, has a medium Κ calc-alkaline signature, like the Patagonian batholith and most of the Quaternary arc-related volcanic rocks along the Andes.New high precision TIMS U-Pb zircon dating of the CHPC yield ages between 17.0 to 16.4 Ma. The absolute ages support the sequence of intrusion relations established in the field (Chapter 1). These data are the first U-Pb age constraints on the CHPC, and clearly show that the magmatic history of CHPC has no direct link to the subduction of the ridge, since this complex is at least 6 Ma older than the time of collision of the Chile ridge at this latitude (Cande and Leslie 1986).An in-depth comparison with other intrusion of Miocene age in Patagonia reveals - for the first time - an interesting temporal pattern. There is a distinct E-W trend of calc-alkaline magmatism between 20-16 Ma with the younging of ages in the East - the CHPC is the easternmost expression of this trend. I suggest that this time-space relation reflects an eastward (landward) migration of the magmatic arc. I propose that main factor controlling this migration is the fast rates of subduction after the major reconfigurations of the plate tectonic motions after the break up of the Farallôn Plate (at -26 ) resulting in strong deformation and high rates of subduction erosion.High radiogenic isotope ratios (Pb, Sr, Nd) ratios, low 5018 signature and high Th/La ratios in mafic rocks are distinctive features of the CHPC. The presented isotopic models (Chapter 2) suggest that this signature reflects source contamination of the mantle wedge rather than crustal contamination. The trace element signature of the CHPC indicates that the mantle wedge was contaminated with a terrigenous component, most likely from Paleozoic sediments.Fieldwork, petrography and geothermobarometry were used to further unravel the internal history of the CHPC (Chapter 3). These data suggest two main levels of crystallization: one a mid crustal levels (6 to 4.5 kbar) and other a shallow level (3.5 to 2 kbar). Isotopic AFC modeling of crustal contamination indicate variable rates of assimilation, which are not correlated with the degree of differentiation. This suggests that different batches of magma differentiate independently at depths. This implies that the CHPC would have formed by several pulses of magmas from at least 3 different sources. Textures of granodiorites and granites indicate a high content of crystals previous to the emplacement and consequently low emplacement temperatures. Field observations show that the mafic rocks are deformed, whereas the (younger) granodiorites and granites are not. It is still subject of investigation whether the deformation of the mafic rocks is related to regional deformation during a compressional regime or to the emplacement it self. However, the emplacement of huge amount of crystal rich felsic magmas suggests an extensional regime.Résumé Grand PublicPétrologie et Géochimie du Complexe Plutonique de Chaltén et les conséquences pour l'évolution magmatique et tectonique du Andes du Sud (Patagonia) pendant le MiocèneLe Complexe Plutonique de Chaltén (CHPC) est un massif montagneux situé à 49°S à la frontière entre le Chili et l'Argentine, en Patagonie (région la plus au sud de l'Amérique du Sud). Il est composé de montagnes qui peuvent atteindre plus de 3000 mètres d'altitude, telles que le Cerro Fitz Roy (3400m) et le Cerro Torre (3100m). Ces montagnes sont composées de roches plutoniques, c.-à-d. des magmas qui se sont refroidis et ont cristallisés sous la surface terrestre.La composition chimique de ces roches montre que les magmas, qui ont formé ce complexe plutonique, font partie d'un volcanisme d'arc. Celui-ci se forme lorsqu'une plaque océanique plonge sous une plaque continentale. Les géologues appellent ce processus « subduction ». Dans un tel scénario, le manteau terrestre, qui se fait prendre entre ces deux plaques, fond pour former ainsi du magma. Ce magma remonte à travers la plaque continentale vers la surface. Si celui-ci atteint la surface, il forme les roches volcaniques, comme par exemple des laves. S'il n'atteint pas la surface, le magma se refroidit pour former finalement les roches plutoniques.Le long de la marge ouest d'Amérique du Sud, la plaque Nazca - qui se situe au sud-est de la plaque océanique pacifique - passe en dessous de la plaque d'Amérique du Sud. La bordure ouest du sud de la plaque sud-américaine a également été affectée par d'autres processus tectoniques, tels que des changements dramatiques dans les déplacements de plaques (il y a 25Ma) et la collision de la ride du Chili (depuis 15 Ma jusqu'à aujourd'hui). Ces caractéristiques tectoniques et magmatiques font de cette région un haut lieu pour les géologues. La plaque Nazca, s'est formée suite à l'ouverture d'une plaque océanique plus ancienne, il y a 25Ma. Cette ouverture est liée aux vitesses de subduction les plus rapides jamais connues. La ride du Chili est l'endroit où le sol de l'Océan Pacifique s'ouvre, formant deux plaques océaniques : les plaques Nazca et Antarctique. La ride du Chili subducte sous la plaque sud-américaine depuis 15Ma, en association avec la formation de grands volumes de magma ainsi que des changements morphologiques importants. La question de savoir lequel de ces changements tectoniques globaux affecte la géologie et la géographie de Patagonie a été, et est encore, discutée pendant de nombreuses années. De nombreux chercheurs suggèrent que la plupart des caractéristiques morphologiques et magmatiques en Patagonie sont liés à la subduction de la ride du Chili, mais cette suggestion est encore débattue comme le montre notre étude.Le batholithe de Patagonie du sud (SPB) est un énorme massif composé de roches plutoniques et il s'étend tout au long de la côte ouest de Patagonie (au sud de 47°S). Ces roches correspondent certainement aux racines d'un ancien arc volcanique, qui a été soulevé et érodé. Le CHPC, ainsi que d'autres petites intrusions dans la région, se situe dans une position exotique, à 100km à l'est du SPB. Certains chercheurs suggèrent que ces intrusions pourraient être liées à la subduction de la ride du Chili.Afin de débattre de cette problématique, nous avons utilisé différentes méthodes géochronologiques pour déterminer l'âge du CHPC et le comparer (a) à l'âge des roches intrusives similaires du SPB et (b) à l'âge de la collision de la ride du Chili. Dans ce travail, nous prouvons que le CHPC s'est formé au moins 7Ma avant la collision avec la ride du Chili. Sur la base des âges du CHPC et de la composition chimique de ses roches et minéraux, nous proposons que le CHPC fait partie d'un arc volcanique ancien. La migration de l'arc volcanique plus profondément dans le continent résulte de la grande vitesse de subduction entre 25 et lOMa. Des caractéristiques évidentes pour un tel processus - telles qu'une déformation importante et une vitesse d'érosion élevée - peuvent être rencontrées tout au long de la bordure ouest de l'Amérique du sud.

Validation française d'un questionnaire de stress post-traumatique destiné aux parents d'enfants présentant un risque périnatal élevé = French validation of the "Perinatal PTSD Questionnaire" assessing parent's posttraumatic stress reactions following the birth of a high risk infant.

(from the journal abstract) Objectives: The birth of a high risk infant--such as a very or extremely premature infant--can represent an important traumatic experience for parents. R. DeMier, M. Hynan et al's "Perinatal PTSD Questionnaire" aims at exploring, retrospectively, parent's posttraumatic stress reactions following the birth of a high risk infant. This paper describes the French validation of this questionnaire. Methods: Fifty-two families with a very or extremely premature infant and 25 families with a full term infant responded to the "Perinatal PTSD Questionnaire" and the "Impact of Event Scale" when children were 18 months old. Results: Parents of high risk infants can present posttraumatic stress reactions such as intrusion, avoidance or arousal symptoms. The French version of the "Perinatal PTSD Questionnaire" has satisfactory psychometric properties. Conclusions: As posttraumatic reactions are not directly related to objective descriptions of the stressful event, it may be essential to the liaison child psychiatrist to consider individual posttraumatic reactions in order to optimise preventive intervention with the parents. A questionnaire should not replace a clinical interview, however it may represent a useful screening tool. Also, this questionnaire should be useful for research purposes. (PsycINFO Database Record (c) 2005 APA, all rights reserved)

The automatic selection of ventilation parameters during the initial phase of mechanical ventilation.

OBJECTIVE: To test a method that allows automatic set-up of the ventilator controls at the onset of ventilation. DESIGN: Prospective randomized crossover study. SETTING: ICUs in one adult and one children's hospital in Switzerland. PATIENTS: Thirty intubated stable, critically ill patients (20 adults and 10 children). INTERVENTIONS: The patients were ventilated during two 20-min periods using a modified Hamilton AMADEUS ventilator. During the control period the ventilator settings were chosen immediately prior to the study. During the other period individual settings were automatically determined by the ventilatior (AutoInit). MEASUREMENTS AND RESULTS: Pressure, flow, and instantaneous CO2 concentration were measured at the airway opening. From these measurements, series dead space (V(DS)), expiratory time constant (RC), tidal volume (VT, total respiratory frequency (f(tot), minute ventilation (MV), and maximal and mean airway pressure (Paw, max and Paw, mean) were calculated. Arterial blood gases were analyzed at the end of each period. Paw, max was significantly less with the AutoInit ventilator settings while f(tot) was significantly greater (P < 0.05). The other values were not statistically significant. CONCLUSIONS: The AutoInit ventilator settings, which were automatically derived, were acceptable for all patients for a period of 20 min and were not found to be inferior to the control ventilator settings. This makes the AutoInit method potentially useful as an automatic start-up procedure for mechanical ventilation.

Metamorphism and kinetics in the Torres del Paine contact aureole

Contact aureoles provide an excellent geologic environment to study the mechanisms of metamorphic reactions in a natural system. The Torres del Paine (TP) intrusion is one of the most spectacular natural laboratories because of its excellent outcrop conditions. It formed in a period from 12.59 to 12.43 Ma and consists of three large granite and four smaller mafic batches. The oldest granite is on top, the youngest at the bottom of the granitic complex, and the granites overly the mafic laccolith. The TP intruded at a depth of 2-3 km into regional metamorphic anchizone to greenschist facies pelites, sandstones, and conglomerates of the Cerro Toro and Punta Barrosa formations. It formed a thin contact aureole of 150-400 m width. This thesis focuses on the reaction kinetics of the mineral cordierite in the contact aureole using quantitative textural analysis methods. First cordierite was formed from chlorite break¬down (zone I, ca. 480 °C, 750 bar). The second cordierite forming reaction was the muscovite break-down, which is accompanied by a modal decrease in biotite and the appearance of k- feldspar (zone II, 540-550 °C, 750 bar). Crystal sizes of the roundish, poikiloblastic cordierites were determined from microscope thin section images by manually marking each crystal. Images were then automatically processed with Matlab. The correction for the intersection probability of each crystal radius yields the crystal size distribution in the rock. Samples from zone I below the laccolith have the largest crystals (0.09 mm). Cordierites from zone II are smaller, with a maximum crystal radius of 0.057 mm. Rocks from zone II have a larger number of small cordierite crystals than rocks from zone I. A combination of these quantitative analysis with numerical modeling of nucleation and growth, is used to infer nucleation and growth parameters which are responsible for the observed mineral textures. For this, the temperature-time paths of the samples need to be known. The thermal history is complex because the main body of the intrusion was formed by several intrusive batches. The emplacement mechanism and duration of each batch can influence the thermal structure in the aureole. A possible subdivision of batches in smaller increments, so called pulses, will focus heat at the side of the intrusion. Focusing all pulses on one side increases the contact aureole size on that side, but decreases it on the other side. It forms a strongly asymmetric contact aureole. Detailed modeling shows that the relative thicknesses of the TP contact aureole above and below the intrusion (150 and 400 m) are best explained by a rapid emplacement of at least the oldest granite batch. Nevertheless, temperatures are significantly too low in all models, compared to observed mineral assemblages in the hornfelses. Hence, an other important thermal mechanisms needs to take place in the host rock. Clastic minerals in the immature sediments outside the contact aureole are hydrated due to small amounts of expelled fluids during contact metamorphism. This leads to a temperature increase of up to 50 °C. The origin of fluids can be traced by stable isotopes. Whole rock stable isotope data (6D and δ180) and chlorine concentrations in biotite document that the TP intrusion induced only very small amounts of fluid flow. Oxygen whole rock data show δ180 values between 9.0 and 10.0 %o within the first 5 m of the contact. Values increase to 13.0 - 15.0 %o further away from the intrusion. Whole rock 6D values display a more complex zoning. First, host rock values (-90 to -70 %o) smoothly decrease towards the contact by ca. 20 %o, up to a distance of ca. 150 m. This is followed by an increase of ca. 20 %o within the innermost 150 m of the aureole (-97.0 to -78 %o at the contact). The initial decrease in 6D values is interpreted to be due to Rayleigh fractionation accompanying the dehydration reactions forming cordierite, while the final increase reflects infiltration of water-rich fluids from the intrusion. An over-estimate on the quantity and the corresponding thermal effect yields a temperature increase of less than 30 °C. This suggests that fluid flow might have contributed only for a small amount to the thermal evolution of the system. A combination of the numerical growth model with the thermal model, including the hydration reaction enthalpies but neglecting fluid flow and incremental growth, can be used to numerically reproduce the observed cordierite textures in the contact aureole. This yields kinetic parameters which indicate fast cordierite crystallization before the thermal peak in the inner aureole, and continued reaction after the thermal peak in the outermost aureole. Only small temperature dependencies of the kinetic parameters seem to be needed to explain the obtained crystal size data. - Les auréoles de contact offrent un cadre géologique privilégié pour l'étude des mécanismes de réactions métamorphiques associés à la mise en place de magmas dans la croûte terrestre. Par ses conditions d'affleurements excellentes, l'intrusion de Torres del Paine représente un site exceptionnel pour améliorer nos connaissances de ces processus. La formation de cette intrusion composée de trois injections granitiques principales et de quatre injections mafiques de volume inférieur couvre une période allant de 12.50 à 12.43 Ma. Le plus vieux granite forme la partie sommitale de l'intrusion alors que l'injection la plus jeune s'observe à la base du complexe granitique; les granites recouvrent la partie mafique du laccolite. L'intrusion du Torres del Paine s'est mise en place a 2-3 km de profondeur dans un encaissant métamorphique. Cet encaissant est caractérisé par un métamorphisme régional de faciès anchizonal à schiste vert et est composé de pélites, de grès, et des conglomérats des formations du Cerro Toro et Punta Barrosa. La mise en place des différentes injections granitiques a généré une auréole de contact de 150-400 m d'épaisseur autour de l'intrusion. Cette thèse se concentre sur la cinétique de réaction associée à la formation de la cordiérite dans les auréoles de contact en utilisant des méthodes quantitatives d'analyses de texture. On observe plusieurs générations de cordiérite dans l'auréole de contact. La première cordiérite est formée par la décomposition de la chlorite (zone I, environ 480 °C, 750 bar), alors qu'une seconde génération de cordiérite est associée à la décomposition de la muscovite, laquelle est accompagnée par une diminution modale de la teneur en biotite et l'apparition de feldspath potassique (zone II, 540-550 °C, 750 bar). Les tailles des cristaux de cordiérites arrondies et blastic ont été déterminées en utilisant des images digitalisées des lames minces et en marquant individuellement chaque cristal. Les images sont ensuite traitées automatiquement à l'aide du programme Matlab. La correction de la probabilité d'intersection en fonction du rayon des cristaux permet de déterminer la distribution de la taille des cristaux dans la roche. Les échantillons de la zone I, en dessous du lacolite, sont caractérisés par de relativement grands cristaux (0.09 mm). Les cristaux de cordiérite de la zone II sont plus petits, avec un rayon maximal de 0.057 mm. Les roches de la zone II présentent un plus grand nombre de petits cristaux de cordiérite que les roches de la zone I. Une combinaison de ces analyses quantitatives avec un modèle numérique de nucléation et croissance a été utilisée pour déduire les paramètres de nucléation et croissance contrôlant les différentes textures minérales observées. Pour développer le modèle de nucléation et de croissance, il est nécessaire de connaître le chemin température - temps des échantillons. L'histoire thermique est complexe parce que l'intrusion est produite par plusieurs injections successives. En effet, le mécanisme d'emplace¬ment et la durée de chaque injection peuvent influencer la structure thermique dans l'auréole. Une subdivision des injections en plus petits incréments, appelés puises, permet de concentrer la chaleur dans les bords de l'intrusion. Une mise en place préférentielle de ces puises sur un côté de l'intrusion modifie l'apport thermique et influence la taille de l'auréole de contact produite, auréole qui devient asymétrique. Dans le cas de la première injection de granite, une modélisation détaillée montre que l'épaisseur relative de l'auréole de contact de Torres del Paine au-dessus et en dessous de l'intrusion (150 et 400 m) est mieux expliquée par un emplacement rapide du granite. Néanmoins, les températures calculées dans l'auréole de con¬tact sont trop basses pour que les modèles thermiques soient cohérants par rapport à la taille de cette auréole. Ainsi, un autre mecanisme exothermique est nécessaire pour permettre à la roche encais¬sante de produire les assemblages observés. L'observation des roches encaissantes entourant les granites montre que les minéraux clastiques dans les sédiments immatures au-dehors de l'auréole sont hydratés suite à la petite quantité de fluide expulsée durant le métamorphisme de contact et/ou la mise en place des granites. Les réactions d'hydratation peuvent permettre une augmentation de la température jusqu'à 50 °C. Afin de déterminer l'origine des fluides, une étude isotopique de roches de l'auréole de contact a été entreprise. Les isotopes stables d'oxygène et d'hydrogène sur la roche totale ainsi que la concentration en chlore dans la biotite indiquent que la mise en place des granites du Torres del Paine n'induit qu'une circulation de fluide limitée. Les données d'oxygène sur roche totale montrent des valeurs δ180 entre 9.0 et 10.0%o au sein des cinq premiers mètres du contact. Les valeurs augmentent jusqu'à 13.0 - 15.0 plus on s'éloigne de l'intrusion. Les valeurs 5D sur roche totale montrent une zonation plus complexe. Les valeurs de la roche encaissante (-90 à -70%o) diminuent progressivement d'environ 20%o depuis l'extérieur de l'auréole jusqu'à une distance d'environ 150 m du granite. Cette diminution est suivie par une augmentation d'environ 20%o au sein des 150 mètres les plus proches du contact (-97.0 à -78%o au contact). La diminution initiale des valeurs de 6D est interprétée comme la conséquence du fractionnement de Rayleigh qui accompagne les réactions de déshydratation formant la cordiérite, alors que l'augmentation finale reflète l'infiltration de fluide riche en eau venant de l'intrusion. A partir de ces résultats, le volume du fluide issu du granite ainsi que son effet thermique a pu être estimé. Ces résultats montrent que l'augmentation de température associée à ces fluides est limitée à un maximum de 30 °C. La contribution de ces fluides dans le bilan thermique est donc faible. Ces différents résultats nous ont permis de créer un modèle thermique associé à la for¬mation de l'auréole de contact qui intègre la mise en place rapide du granite et les réactions d'hydratation lors du métamorphisme. L'intégration de ce modèle thermique dans le modèle numérique de croissance minérale nous permet de calculer les textures des cordiérites. Cepen¬dant, ce modèle est dépendant de la vitesse de croissance et de nucléation de ces cordiérites. Nous avons obtenu ces paramètres en comparant les textures prédites par le modèle et les textures observées dans les roches de l'auréole de contact du Torres del Paine. Les paramètres cinétiques extraits du modèle optimisé indiquent une cristallisation rapide de la cordiérite avant le pic thermique dans la partie interne de l'auréole, et une réaction continue après le pic thermique dans la partie la plus externe de l'auréole. Seules de petites dépendances de température des paramètres de cinétique semblent être nécessaires pour expliquer les don¬nées obtenues sur la distribution des tailles de cristaux. Ces résultats apportent un éclairage nouveau sur la cinétique qui contrôle les réactions métamorphiques.

Geological transect across the Northwestern Himalaya in eastern Ladakh and Lahul (A model for the continental collision of India and Asia)

The detailed geological mapping and structural study of a complete transect across the northwestern Himalaya allow to describe the tectonic evolution of the north Indian continental margin during the Tethys ocean opening and the Himalayan Orogeny. The Late Paleozoic Tethys rifting is associated with several tectonomagmatic events. In Upper Lahul and SE Zanskar, this extensional phase is recorded by Lower Carboniferous synsedimentary transtensional faults, a Lower Permian stratigraphic unconformity, a Lower Permian granitic intrusion and middle Permian basaltic extrusions (Panjal Traps). In eastern Ladakh, a Permian listric normal fault is also related to this phase. The scarcity of synsedimentary faults and the gradual increase of the Permian syn-rift sediment thickness towards the NE suggest a flexural type margin. The collision of India and Asia is characterized by a succession of contrasting orogenic phases. South of the Suture Zone, the initiation of the SW vergent Nyimaling-Tsarap Nappe corresponds to an early phase of continental underthrusting. To the S, in Lahul, an opposite underthrusting within the Indian plate is recorded by the NE vergent Tandi Syncline. This structure is associated with the newly defined Shikar Beh Nappe, now partly eroded, which is responsible for the high grade (amphibolite facies) regional metamorphism of South Lahul. The main thrusting of the Nyimaling-Tsarap Nappe followed the formation of the Shikar Beh Nappe. The Nyimaling-Tsarap Nappe developed by ductile shear of the upper part of the subducted Indian continental margin and is responsible for the progressive regional metamorphism of SE Zanskar, reaching amphibolite facies below the frontal part of the nappe, near Sarchu. In Upper Lahul, the frontal parts of the Nyimaling-Tsarap and Shikar Beh nappes are separated by a zone of low grade metamorphic rocks (pumpellyite-actinolite facies to lower greenschist facies). At high structural level, the Nyimaling-Tsarap Nappe is characterized by imbricate structures, which grade into a large ductile shear zone with depth. The related crustal shortening is about 87 km. The root zone and the frontal part of this nappe have been subsequently affected by two zones of dextral transpression and underthrusting: the Nyimaling Shear Zone and the Sarchu Shear Zone. These shear zones are interpreted as consequences of the counterclockwise rotation of the continental underthrusting direction of India relative to Asia, which occurred some 45 and 36 Ma ago, according to plate tectonic models. Later, a phase of NE vergent `'backfolding'' developed on these two zones of dextral transpression, creating isoclinal folds in SE Zanskar and more open folds in the Nyimaling Dome and in the Indus Molasse sediments. During a late stage of the Himalayan Orogeny, the frontal part of the Nyimaling-Tsarap Nappe underwent an extension of about 15 km. This phase is represented by two types of structures, responsible for the tectonic unroofing of the amphibolite facies rocks of the Sarchu area: the Sarchu high angle Normal Fault, cutting a first set of low angle normal faults, which have been created by reactivation of older thrust planes related to the Nyimaling-Tsarap Nappe.