ALBERT

Description: Dolomite occurs in a wide range of rock compositions, from peridotites to mafic eclogites and metasediments, up to mantle depths of more than 200 km. At low-temperatures dolomite is ordered ( R ), but transforms with increasing temperature into a disordered higher symmetry structure ( R c ). To understand the thermodynamics of dolomite, we have investigated temperature, pressure, kinetics, and compositional dependence of the disordering process in Fe-bearing dolomites. To avoid quench effects, in situ X-ray powder diffraction experiments were performed at 300–1350 K and 2.6–4.2 GPa. The long-range order parameter s , quantifying the degree of ordering, has been determined using structural parameters from Rietveld refinement and the normalized peak area variation of superstructure Bragg peaks characterizing structural ordering/disordering. Time-series experiments show that disordering occurs in 20–30 min at 858 K and in a few minutes at temperatures ≥999 K. The order parameter decreases with increasing temperature and X Fe . Complete disorder is attained in dolomite at ~1240 K, 100–220 K lower than previously thought, and in an ankeritic-dolomite s.s. with an X Fe of 0.43 at temperatures as low as ~900 K. The temperature-composition dependence of the disorder process was fitted with a phenomenological approach intermediate between the Landau theory and the Bragg-Williams model and predicts complete disorder in pure ankerite to occur already at ~470 K. The relatively low-temperature experiments of this study also constrain the breakdown of dolomite to aragonite+Fe-bearing magnesite at 4.2 GPa to temperature lower than ~800 K favoring an almost straight Clapeyron-slope for this disputed reaction.

Description: The deep crustal magmatic history of arc volcanoes is obscured by diversity in mantle inputs, modest isotopic contrast between magma and wall-rock, and overprinting processes in the middle and upper crust. To identify and quantify processes in the deep arc crust, we investigated the evolution of the mafic composite North Sister Volcano, the oldest and most mafic of the Three Sisters Volcanic Field of the central Oregon Cascade arc. Here, intra-arc extension limits the degree of magma interaction with the mid- to upper crust and the range in primitive magmas delivered from the mantle is known. North Sister Volcano has produced low-K basaltic andesitic magmas (0·5–0·8 wt % K 2 O) for ~400 kyr during four central-vent eruptive stages and along the late, 11 km long Matthieu Lakes Fissure. Although restricted in bulk composition (53–55 wt % SiO 2 ), North Sister basaltic andesites from different stages cluster into elemental and isotopic groups. Over time, North Sister basaltic andesites generally have decreasing compatible elements, such as Ni (from 112 to 40 ppm), and increasing Al 2 O 3 and TiO 2 . Concurrently, incompatible elements remain the same or decrease (e.g. from 302 to 247 ppm Ba). Isotopic variations at North Sister are small, but systematically progress toward more mantle-like ratios with time; 87 Sr/ 86 Sr decreases (from 0·70369 to 0·70356), and 144 Nd/ 143 Nd increases (from 0·51285 to 0·51292). We present a multi-stage petrological model for the evolution of North Sister magmas to account for: (1) the generation of low-K basaltic andesite; (2) geochemical variations within the eruptive stages; (3) evolution of the magma system over time to more mantle-like compositions. The earliest and most isotopically ‘crust-like’ (highest 87 Sr/ 86 Sr and lowest 143 Nd/ 144 Nd) North Sister magma is consistent with two-component mixing of regionally typical mantle-derived, low-K tholeiites with partial melts of the crust. Crustal melts must be high in SiO 2 and Al 2 O 3 , and most probably result from low-degree melting of plagioclase–clinopyroxene amphibole-bearing gabbro at high pressure. Variations in highly compatible elements within compositional groups (e.g. 60 ppm Ni within a single group) reflect fractionation of plagioclase, olivine, and clinopyroxene and recharge by more primitive basaltic andesite that overprint longer-term variations between groups. To understand the evolution of the North Sister basaltic andesite magmas through time, we use an energy-constrained model that balances assimilation of refractory gabbroic wall-rocks and abundant recharge by mantle-derived low-K tholeiites. These complementary processes allow Sr and Nd isotopic ratios to become more like those of the regional basalts while maintaining high Ni concentrations. Low-K basaltic andesites like those of North Sister Volcano are found along the Oregon Cascade arc and they imply that low-K tholeiitic magmas interact with a refractory mafic underplate along its length. Dominantly basaltic andesite volcanoes are common in arcs and provide insight into the extensive, albeit compositionally cryptic mafic underplating and intraplating that affects arc crust.

Description: Phase assemblages, melting relations and melt compositions of a dry carbonated pelite (DG2) and a carbonated pelite with 1·1 wt % H 2 O (AM) have been experimentally investigated at 5·5–23·5 GPa and 1070–1550°C. The subsolidus mineralogies to 16 GPa contain garnet, clinopyroxene, coesite or stishovite, kyanite or corundum, phengite or potassium feldspar (≤8 GPa with and without H 2 O, respectively), and then K-hollandite, a Ti phase and ferroan dolomite/Mg-calcite or aragonite + ferroan magnesite at higher pressures. The breakdown of clinopyroxene at 〉16 GPa causes Na-rich Ca-carbonate containing up to 11 wt % Na 2 O to replace aragonite and leads to the formation of an Na-rich CO 2 fluid. Further pressure increase leads to typical Transition Zone minerals such as the CAS phase and one or two perovskites, which completely substitute garnet at the highest investigated pressure (23·5 GPa). Melting at 5·5–23·5 GPa yields alkali-rich magnesio-dolomitic (DG2) to ferro-dolomitic (AM) carbonate melts at temperatures 200–350°C below the mantle geotherm, lower than for any other studied natural composition. Melting reactions are controlled by carbonates and alkali-hosting phases: to 16 GPa clinopyroxene remains residual, Na is compatible and the magnesio- to ferro-dolomitic carbonate melts have extremely high K 2 O/Na 2 O ratios. K 2 O/Na 2 O weight ratios decrease from 26–41 at 8 GPa to 1·2 at 16 GPa when K-hollandite expands its stability field with increasing pressure. At 〉16 GPa, Na is repartitioned between several phases, and again becomes incompatible as at 〈3 GPa, leading to Na-rich carbonate melts with K 2 O/Na 2 O ratios 1. This leaves the pressure interval of c . 4–15 GPa for ultrapotassic metasomatism. Comparison of the solidus with typical subducting slab-surface temperatures yields two distinct depths of probable carbonated pelite melting: at 6–9 GPa where the solidus has a negative Clapeyron slope between the intersection of the silicate and carbonate melting reactions at ~5 GPa, and the phengite or potassium feldspar stability limit at ~9 GPa. The second opportunity is related to possible slab deflection along the 660 km discontinuity, leading to thermal relaxation and partial melting of the fertile carbonated pelites, thus recycling sedimentary CO 2 , alkalis and other lithophile and strongly incompatible elements back into the mantle.

Description: Carbonatite and silicate rocks occurring within a single magmatic complex may originate through liquid immiscibility. We thus experimentally determined carbonatite/silicate melt partition coefficients ( D carbonate melt/silicate melt , hereafter D ) for 45 elements to understand their systematics as a function of melt composition and to provide a tool for identifying the possible conjugate nature of silicate and carbonatite magmas. Static and, when necessary, centrifuging piston cylinder experiments were performed at 1–3 GPa, 1150–1260°C such that two well-separated melts resulted. Bulk compositions had Na K, Na ~ K, and Na K; for the latter we also varied bulk H 2 O (0–4 wt %) and SiO 2 contents. Oxygen fugacities were between iron–wüstite and slightly below hematite–magnetite and were not found to exert significant control on partitioning. Under dry conditions alkali and alkaline earth elements partition into the carbonatite melt, as did Mo and P ( D Mo 〉8, D P = 1·6–3·3). High field strength elements (HFSE) prefer the silicate melt, most strongly Hf ( D Hf = 0·04). The REE have partition coefficients around unity with D La/Lu = 1·6–2·3. Transition metals have D 〈 1 except for Cu and V ( D Cu ~ 1·3, D V = 0·95–2). The small variability of the partition coefficients in all dry experiments can be explained by a comparable width of the miscibility gap, which appears to be flat-topped in our dry bulk compositions. For all carbonatite and silicate melts, Nb/Ta and Zr/Hf fractionate by factors of 1·3–3·0, in most cases much more strongly than in silicate–oxide systems. With the exception of the alkalis, partition coefficients for the H 2 O-bearing systems are similar to those for the anhydrous ones, but are shifted in favour of the carbonatite melt by up to an order of magnitude. An increase of bulk silica and thus SiO 2 in the silicate melt (from 35 to 69 wt %) has a similar effect. Two types of trace element partitioning with changing melt composition can be observed. The magnitude of the partition coefficients increases for the alkalis and alkaline earths with the width of the miscibility gap, whereas partition coefficients for the REE shift by almost two orders of magnitude from partitioning into the silicate melt ( D La = 0·47) to strongly partitioning into the carbonatite melt ( D La = 38), whereas D La / D Lu varies by only a factor of three. The partitioning behavior can be rationalized as a function of ionic potential ( Z / r ). Alkali and alkaline earth elements follow a trend, the slope of which depends on the K/Na ratio and H 2 O content. Contrasting the sodic and potassic systems, alkalis have a positive correlation in D vs Z / r space in the potassic case and Cs to K partition into the silicate melt in the presence of H 2 O. For the divalent third row transition metals on the one hand and for the tri- and tetravalent REE and HFSE on the other, two trends of negative correlation of D vs Z / r can be defined. Nevertheless, the highest ionic strength network-modifying cations (V, Nb, Ta, Ti and Mo) do not follow any trend; understanding their behavior would require knowledge of their bonding environment in the carbonatite melt. Strong partitioning of REE into the carbonatite melt ( D REE = 5·8–38·0) occurs only in H 2 O-rich compositions for which carbonatites unmix from evolved alkaline melts with the conjugate silicate melt being siliceous. We thus speculate that upon hydrous carbonatite crystallization, the consequent saturation in fluids may lead to hydrothermal systems concentrating REE in secondary deposits.

Description: Ionization of the atmosphere due to precipitating solar energetic particles as well as magnetospheric particles is a major source of thermospheric electron density. In this paper we evaluate numerical simulations of the 3-D spatial and temporal electron densities produced by these particle populations through a comparison with incoherent scatter radar observations. The 3-D precipitation patterns are determined with the Atmospheric Ionization Module Osnabrück (AIMOS). We use a version of the general circulation and chemistry model Hamburg Model of the Neutral and Ionized Atmosphere (HAMMONIA) enhanced by ion chemistry to calculate the impact of particle ionization on the electron density. These modeled data are compared to radar observations from European Incoherent Scatter Svalbard and Tromsø as well as the incoherent scatter radar stations at Millstone Hill and Sondrestrom. Particle precipitation is severely affected by geomagnetic disturbance and latitude. Therefore, different locations (inside the polar cap and at auroral latitudes) and geomagnetic conditions are included in the comparison. The main results of the paper can be summarized as follows: (1) as expected, particle forcing will significantly improve modeled electron density in comparison to results of the radar measurements; (2) in particular nighttime comparisons of the electron density are affected; here the particle forcing will account for a boost of 2 to 3 orders of magnitude.

Description: The origin of pyroxenites and their relation to melt migration in the mantle have been investigated in two pyroxenite-rich zones in the Beni Bousera massif. Based on combined field, microtextural, mineralogical and geochemical observations, the pyroxenites were separated into four types. Type-I Cr-diopside websterites contain bright green diopside and have primitive bulk Ni, Cr and Mg-number. Their trace element systematics are characterized by slight light rare earth element (LREE) enrichment compared with the middle (MREE) and heavy (H)REE, and negative high field strength element (HFSE) anomalies in bulk-rock and mineral compositions suggesting that they result from melting of metasomatized mantle. Trace element concentrations of melts calculated to be in equilibrium with Type-I cpx have a subduction-like signature and show a close similarity to certain lavas erupted in the Alboran Basin. Calculated mineral equilibration temperatures of ~1200 to 1350°C are close to the basalt liquidus and higher than for other pyroxenite types in Beni Bousera, which generally yield 〈1100°C. Type-II spinel websterites are also primitive, but contain augitic clinopyroxene; their whole-rock compositions are characterized by high Ti, Ni, and Mg-number, intermediate Cr and trace element patterns with LREE depletion over the MREE and HREE. Type-III garnet pyroxenites, which include the famous diamond-pseudomorph-bearing garnet pyroxenites, are more evolved than Types-I and -II and have low and variable Mg-number correlating with an Fe-enrichment trend. High bulk-rock and garnet HREE to LREE ratios result from high-pressure fractionation of garnet and augitic cpx at calculated pressures of 〉45 to 20–30 kbar. Type-III pyroxenites display strong variations of LREE and HFSE depletion and strong bulk Nb/Ta fractionation. Calculated melts in equilibrium with augitic cpx are variably enriched in incompatible trace elements similar to intraplate basalts. Type-IV pyroxenites are composed of green diopside, opx, garnet and plagioclase and/or spinel. Whole-rocks have high Na 2 O, CaO and Al 2 O 3 concentrations and high Mg-number, are HREE depleted, and have positive Eu and Sr anomalies. Garnets are characterized by low HREE/MREE and positive Eu anomalies. The absence of bulk-rock HREE enrichment indicates a metamorphic origin for this garnet, which is corroborated by the presence of Al-rich metamorphic spinels. Relict magmatic plagioclase indicates a shallower (〈10 kbar) crustal origin for these pyroxenites. Their metamorphic assemblage yields temperatures and pressures of 800–980°C and 14 kbar, indicating a pressure increase during the metamorphic overprint. The whole-rock geochemistry of Type-IV pyroxenites is comparable with that of rocks from the lower crustal section of the Kohistan (northern Pakistan) paleo-arc, indicating a possible origin of these rocks as cumulates in the deeper arc crust and subsequent delamination into the underlying mantle.

Description: Recycling of volatiles at subduction zones is a key step in the Earth’s geochemical cycle. Some subducted CO 2 is remobilized in island-arc magmas, but most of it is recycled into the deeper mantle. Calcite-olivine-bearing veins in the mantle rocks of the Kohistan Paleo-Island Arc (North Pakistan) contain some of the best gem quality olivines worldwide. The O, C, and Sr isotopy of the vein minerals indicate that these veins formed from H 2 O-CO 2 fluids partly equilibrated with the mantle. Fe-Mg borate inclusions in gem olivine indicate that the fluid contained substantial B. Trace element concentrations of the vein minerals show patterns relatively enriched in La, Ce, Ta, Cu, and Zn, indicating that these elements were mobile in the vein fluids. These veins provide evidence that CO 2 may be mobilized by dissolution of carbonates in fore-arcs and that B- and HFSE-rich reservoirs may form through secondary deposition. Reprocessing of such veins could play an important role in C, B, and HFSE recycling, making these elements not necessarily a direct indicator of the slab devolatilization processes.

Description: The Mars Science laboratory (MSL) made a successful landing at Gale crater early August 2012. MSL has an environmental instrument package called the Rover Environmental Monitoring Station (REMS) as a part of its scientific payload. REMS comprises instrumentation for the observation of atmospheric pressure, temperature of the air, ground temperature, wind speed and direction, relative humidity (REMS-H), and UV measurements. We concentrate on describing the REMS-H measurement performance and initial observations during the first 100 MSL sols as well as constraining the REMS-H results by comparing them with earlier observations and modelling results. The REMS-H device is based on polymeric capacitive humidity sensors developed by Vaisala Inc. and it makes use of transducer electronics section placed in the vicinity of the three (3) humidity sensor heads. The humidity device is mounted on the REMS boom providing ventilation with the ambient atmosphere through a filter protecting the device from airborne dust. The final relative humidity results appear to be convincing and are aligned with earlier indirect observations of the total atmospheric precipitable water content. The water mixing ratio in the atmospheric surface layer appears to vary between 30 and 75 ppm. When assuming uniform mixing, the precipitable water content of the atmosphere is ranging from a few to 6 precipitable micrometers.

Description: Based on Optically Stimulated Luminescence (OSL) and radiocarbon dating we establish chronologies of colluviation and alluviation in different floodplain sections of the northwestern Wetterau loess basin (Germany). Similar to some other European valley floors, Holocene floodplain aggradation is marked by two important breaks: (1) a millennial-scale delay between the Neolithic agricultural colluviation and floodplain aggradation. In loess catchments agricultural colluviation started at about 7000 cal. BP and anthropogenic floodplain aggradation only at about 2200 ± 200 cal. BP; (2) a centennial-scale variability in a temporary rise in rates of anthropogenic floodplain aggradation (up to 3.6 ± 1.7 mm/yr) during the High Middle Ages in directly neighbouring reaches. Independent archaeologic, historic, and vegetation records document distinct agricultural histories of hillsides and floodplains and highlight the importance of hydrosedimentary connectivity as compared with land use intensity. The late Iron Age start of alluviation can be linked to the introduction of an integrated land use system with intense cultivation on hillsides and immediate neighbouring floodplains. The centennial-scale variability of medieval peak aggradation is a result of the successive introduction (or temporal failure) of hydraulic water milling infrastructure. Using palaeoecological and geomorphological information for reconstructing cause and consequence of sediment redistribution in coupled human–natural systems requires firm information about the spatial organisation and technological abilities that are associated with socio-agricultural transformations.