Current covers of AGU Journals. For older covers, see the archives of each journal. High resolution images are available in the issue information PDF of each issue.
In Booth et al., image (a–e) slope maps of the surface evolution of the Oso landslide predicted by a nonlinear model of hillslope sediment flux (equation(1)). Figure6a is 2014 lidar data, while Figures 6b–6e are model results. For comparison, (f) a lidar-derived slope map of the landslide directly southeast of the Oso landslide with a similar size and shape and a predicted age of ~5000 cal years B.P. is presented.
In Forouta et al., the emission of particulate matter with diameter less than 10 microns (PM10) due to dust outbreaks over the southwestern United States in March 7, 2011 (top left), March 21, 2011 (top right), April 3, 2011 (bottom left), and May 29, 2011 (bottom right). The results (in gm-3) are obtained using a newly developed windblown dust scheme implemented in the Community Multiscale Air Quality (CMAQ) modeling system
Two errors were discovered in the originally published version. The units specified in the first footnote of Table A1 have been corrected. In addition, all instances of “(cm^2 s str)^-1” on page 19 have been replaced with “(cm^-2 sr)”. The corrected paper should be considered the version of record.
In Rutte et al., image shows (a–d) Panoramic views of the Muskol dome. Distortion increases toward the image edges. Figures 4a and 4b are along section A in Figure 8. Thrusts and north vergent, recumbent, isoclinal folds in Figure 4d are in left part of Figure 4c. (e–h) Fault scarps in colluvial and alluvial deposits and range front normal faults along the active Sarez-Karakul graben system.
A hot flow anomaly generates global ULF waves in the magnetosphere. Reflected ions (white arrows) from Earth’s bow shock are trapped by a tangential discontinuity (purple dashed line) and drift along it, interact with the incident solar wind ions and form a hot plasma region (yellow region) called Hot Flow Anomaly (HFA). The hot plasma region expands and form shocks (blue arrows) on two sides of the structure. In this study, an HFA was observed by Cluster 1 spacecraft, generating ULF waves in the magnetosphere globally (the red dashed lines represent the undisturbed magnetic field lines, the red solid lines represent the magnetic field lines with ULF waves).
Ceres has plenty of permanently shadowed regions (mapped in blue) at the present day when its obliquity is small. However, due to obliquity changes in the past, only few permanent shadows remain.
Wind-blown dune sand can wear away the Martian surface and uncover geologic units, which haven’t been exposed to prolonged spa
Overview of sampled outcrops: A = the Monte Cagnero section, with approximate locations of the
Rupelian-Chattian boundary (RCB) and the biotite-rich layer (BRL) at 142.8 m; B = BRL at 145.8 m in the Monte Cagnero section;
C = the Massignano
section, with approximate locations of the Eocene-Oligocene boundary (EOB), and sampled BRL; D = BRL at 5.8 m in the Massignano
section; E = the
Pieve d’Accinelli section with approximate location of the B2 BRL (sample PAC-B2 in this study) and the RCB.
The estimated linkages of stream water quality with the land use and hydrologic drivers identify the management targets and priorities to achieve healthy coastal-urban stream ecosystems.
image shows alternative model results. We vary the initial conditions by scanning through different configuration
of initial thicknesses of lithosphere, full crust, and upper crust within the transverse inherited domain of the Turkana region
. (a) Initial crustal thickness of 30 km. (b) Initial
crustal thickness of 25 km. All other parameters and layer thicknesses are kept identical to model A1. Images show strain rate
patterns after 15 Myr of stretching, equivalent
to 60 km of extension. In the lower left corner of each image we plot the yield strength profile of the transverse central regi
on at the onset of rifting. Lithospheric strength
is controlled by the interplay of lithospheric thickness and radiogenic heat production within the upper crust. The initial str
ength controls rift localization and leads to five
different types of rift linkage after 15 Myr indicated in the upper right corner of each image. Initial strength of each layer
within the central domain of all models is also
provided in supporting information Table S2. Animations of six characteristic models representing key aspects of rift linkage a
re given in the supporting information as Movies
S1 to S6.
In Stets et al., Stets et al. investigated the effects of carbonate buffering and metabolism on carbon dioxide (CO2) and dissolved inorganic carbon (DIC) concentrations in river networks. Carbonate buffering is less prominent in low alkalinity (a.) as compared with high alkalinity (b.) watersheds. Carbonate buffering decreases the rate of CO2 exchange across the air-water interface by decreasing the CO2 gradient, thereby affecting both the CO2 and DIC pools. Increased buffering and lags in CO2 exchange cause excess dissolved inorganic carbon (ΔDIC) to be higher in the small streams of high alkalinity watersheds (c.) as inputs from groundwater and negative net ecosystem production in small streams equilibrate more slowly in the high alkalinity watersheds. CO2 excess (ΔCO2) is high in the smallest streams of low alkalinity watersheds (d.). Rapid exchange with the atmosphere depletes CO2 pools, causing ΔCO2 to be lower in mid-sized streams of low alkalinity watersheds. Differences in carbonate buffering create spatial differences in CO 2 and DIC dynamics at the landscape scale.
40 years later: Viking missions continue to yield new results.
Temperature perturbations at ~40 km, ~50 km, and ~60 km at 11:00LT 4 October 2013 in the data of Modern Era Retrospective Analysis for Research and Applications (MERRA), revealing atmospheric gravity wave oscillations that most likely initiated equatorial plasma bubbles in the
ionosphere. The red dotted lines represent the magnetic equator.
annual-mean precipitation response between 40N and 40S to increased CO
Pryor et al. [DOI: 10.1002/2016JD025854] computed fluxes of ultra-fine particles (UFP) above and below the canopy of a mature deciduous
Two eddy-covariance flux towers at the Harvard Forest in New England where the hemlock woolly adelgid (Adelges tsugae) infestation has resulted in eastern hemlock (Tsuga canadensis) mortality (photo by David A. Orwig).
(left) STA-COR1 observation with representative PFSS field lines overplotted showing the faint white-light signature of the eruption X point [adapted from Lynch et al., 2010]. (right) Synthetic white-light ratio image at t = 174 h from ϕSTA perspective showing the stealth CME simulation X point structure.