Tab. 1 Mole % CO2 and 13C values of CO2 at baseline and at the final monitoring event for the eight observation wells

During CO2 storage operations in mature oilfields or saline aquifers it is desirable to trace the movement of injected CO2 for verification and safety purposes. We demonstrate the successful use of carbon isotope abundance ratios for tracing the movement of CO2 injected at the Cardium CO2 Storage Monitoring project in Alberta between 2005 and 2007. Injected CO2 had a d13C value of -4.6±1.1 per mil that was more than 10 per mil higher than the carbon isotope ratios of casing gas CO2 prior to CO2 injection with average d13C values ranging from -15.9 to -23.5 per mil. After commencement of CO2 injection, d13C values of casing gas CO2 increased in all observation wells towards those of the injected CO2 consistent with a two-source end-member mixing model. At four wells located in a NE-SW trend with respect to the injection wells, breakthrough of injected CO2 was registered chemically (>50 mol % CO2) and isotopically 1-6 months after commencement of CO2 injection resulting in cumulative CO2 fluxes exceeding 100000 m**3 during the observation period. At four other wells, casing gas CO2 contents remained below 5 mol % resulting in low cumulative CO2 fluxes (<2000 m**3) throughout the entire observation period, but carbon isotope ratios indicated contributions between <30 and 80% of injected CO2. Therefore, we conclude that monitoring the movement of CO2 in the injection reservoir with geochemical and isotopic techniques is an effective approach to determine plume expansion and to identify potential preferential flow paths provided that the isotopic composition of injected CO2 is constant and distinct from that of baseline CO2.

Bacteriemias en Mayores de 65 años : resultados de un análisis comparativo

Objetivos: Evaluar parámetros clínicos, bacteriológicos y morbimortalidad en pacientes mayores de 65 años con bacteriemia (Grupo A) y compararlos con aquellas ocurridas en menores de 65 años (grupo B) hospitalizados en un servicio de clínica médica. Material y métodos: Estudio protocolizado, descriptivo y observacional, desde 1989-2006. Criterios de inclusión: dos o más hemocultivos positivos. Análisis estadístico con Epi Info 6.4 . Resultados: Se identificaron 668 bacteriemias: 258 (38,6%) en A y 410 (61,4%) en B. La edad media fue de 74,2 años (DS±7.01) y de 47,2 años (DS±13.7) respectivamente. No hubo diferencias en la permanencia media: 19,1 días (DS±17.07) en A y 19,9 (DS±18,1) en B, ni en el origen nosocomial (40,7 vs 44%). Los focos pulmonar (31 vs 21,2%)(p<0,008) y urinario (27 vs 18,8%)(p=0.017) fue más frecuentes en A. La fiebre >de 38 ºC fue menos frecuente en A (83,8 vs 90,9%)(p=0.0068), mientras que la hipotensión arterial (40,8 vs 32,2%)(p=0.03), oliguria (41,7 vs 30,9%)(p=0.005) y encefalopatía (54,5 vs 39,4%)(p=0.00014) fueron mas comunes en A. Los bacilos gram negativos predominaron en A (46 vs 37%)(p<0.01) con diferencias entre A.baumani (9,16 vs 4,6%) y E.coli (54,1 vs 42,7%)(p<0.05) y en B fueron más frecuentes por S.aureus MS (34.39 vs 24,63)(p=0.01). El shock séptico (33,9 vs 22,4%) y nuevas insuficiencias de órganos (31,1 vs 20,1%) prevalecieron en A (p<0,001). La mortalidad fue de 34,49% para A y de 23,41% para B (p=0,018) Conclusiones: Las bacteriemias en pacientes internados mayores de 65 años comparadas con las ocurridas en pacientes. de menor edad, se caracterizaron significativamente por tener predominio del foco pulmonar y urinario, de hipotensión arterial, oliguria y encefalopatía, de bacteriemia por BGN, principalmente A. baumanii y E. coli; mayor desarrollo de shock séptico, menor frecuencia de fiebre >38°C y de bacteriemia por MSS A, y significativa mayor mortalidad.

Geochemistry of DSDP Hole 83-504B minerals

Leg 83 of the Deep Sea Drilling Project has deepened Hole 504B to over 1 km into basement, 1350 m below the seafloor (BSF). The hole previously extended through 274.5 m of sediment and 561.5 m of pillow basalts altered at low temperature (< 100°C), to 836 m BSF. Leg 83 drilling penetrated an additional 10 m of pillows, a 209-m transition zone, and 295 m into a sheeted dike complex. Leg 83 basalts (836-1350 m BSF) generally contain superimposed greenschist and zeolite-facies mineral parageneses. Alteration of pillows and dikes from 836 to 898 m BSF occurred under reducing conditions at low water/rock ratios, and at temperatures probably greater than 100°C. Evolution of fluid composition resulted in the formation of (1) clay minerals, followed by (2) zeolites, anhydrite, and calcite. Alteration of basalts in the transition zone and dike sections (898-1350 m BSF) occurred in three basic stages, defined by the opening of fractures and the formation of characteristic secondary minerals. (1) Chlorite, actinolite, pyrite, albite, sphene, and minor quartz formed in veins and host basalts from partially reacted seawater (Mg-bearing, locally metal-and Si-enriched) at temperatures of at least 200-250°C. (2) Quartz, epidote, and sulfides formed in veins at temperatures of up to 380°C, from more evolved (Mg-depleted, metal-, Si-, and 18O-enriched) fluids. (3) The last stage is characterized by zeolite formation: (a) analcite and stilbite formed locally, possibly at temperatures less than 200°C followed by (b) formation of laumontite, heulàndite, scolecite, calcite, and prehnite from solutions depleted in Mg and enriched in Ca and 18O, at temperatures of up to 250°C. The presence of small amounts of anhydrite locally may be due to ingress of relatively unaltered seawater into the system during Stage 3. Alteration was controlled by the permeability of the crust and is characterized by generally incomplete recrystallization and replacement reactions among secondary minerals. Secondary mineralogy in the host basalts is strongly controlled by primary mineralogy. The alteration of Leg 83 basalts can be interpreted in terms of an evolving hydrothermal system, with (a) changes in solution composition because of reaction of seawater fluids with basalts at high temperatures; (b) variations in permeability caused by several stages of sealing and reopening of cracks; and (c) a general cooling of the system, caused either by the cooling of a magma chamber beneath the spreading center and/or the movement of the crust away from the heat source. The relationship of the high-temperature alteration in the transition zone and dike sections to the low-temperature alteration in the overlying pillow section remains uncertain.