Search Results

You are looking at 31 - 40 of 906 items for :

  • Geographic location/entity x
  • All content x
Clear All
Joseph E. Trainor, Danielle Nagele, Brenda Philips, and Brittany Scott

tornado warning includes several key pieces of information, including a geographic area, a valid time, the duration, and text describing the potential hazard, its path, and advice for protective action. In current practice, local NWS warning forecast offices (WFOs) issue the initial tornado warning, and then the warning information is disseminated to the public through broadcast media, outdoor sirens, social media, call-out systems, word of mouth, texting, or phone calls. NWS, Red Cross, and Federal

Full access
Marius Årthun, Paul R. Holland, Keith W. Nicholls, and Daniel L. Feltham

cavity is dominated by the eddy (denoted E1) entering at the western end of the polynya ( Fig. 8 ). This eddy then flows in a southeastward direction with cyclonic motion to the west and anticyclonic motion on the east (not shown). During the 60 days that the model was run, three other large eddies (E2–E4) are seen to propagate into the sub–ice shelf cavity, eventually merging to form a larger inflow branch of HSSW. The location of the inflow is shifted as the salinity front moves westward ( Fig. 4

Full access
H. K. Ha, A. K. Wåhlin, T. W. Kim, S. H. Lee, J. H. Lee, H. J. Lee, C. S. Hong, L. Arneborg, G. Björk, and O. Kalén

top of the mooring does not reach the surface gives a comparatively small error since the surface water is close to freezing temperature. In order to estimate the heat flux from the mooring data, an effective width of the inflow must be assumed. The trough has been transected twice at this location, in 2008 ( Wåhlin et al. 2010 ) and 2010 ( Fig. 2a ). Both transects show a warm current spread out over about 100 km and isopycnals approximately parallel to the bottom. Effective widths for these

Full access
Daniel C. Jones, Takamitsu Ito, Thomas Birner, Andreas Klocker, and David Munday

everywhere in the Southern Ocean, by one or two orders of magnitude in most locations (see Fig. 6a ). This is consistent with the findings of Tulloch et al. (2011) , wherein the authors used the Ocean Comprehensible Atlas (OCCA) to show that the surface relative vorticity is smaller than β nearly everywhere in the global ocean by at least an order of magnitude ( Forget 2010 ). Fig . 6. Depth-averaged relative vorticity gradient in the Southern Ocean scaled by β . Zonal and meridional velocity fields

Full access
A. K. Wåhlin, O. Kalén, K. M. Assmann, E. Darelius, H. K. Ha, T. W. Kim, and S. H. Lee

lines with arrows depict the general circulation pattern and cooling of the warm deep water ( Ha et al. 2014 ). Bathymetry is from Arndt et al. (2013) . The inset shows the location of the study region in Antarctica. Table 1. Mooring: coordinates, depth, deployment periods, and instrumentation. The ADCP’s were both 150-kHz instruments from RDI deployed upward looking at the bottom to measure current velocity profiles. The observed velocity data were processed using the WinADCP software. The

Full access
Sutara H. Suanda and John A. Barth

numerical models ( Kurapov et al. 2003 ; Osborne et al. 2011 ). Semidiurnal internal tides are weaker during the weakly stratified winter months ( Erofeeva et al. 2003 ), and realistic simulations to isolate locations of barotropic-to-baroclinic semidiurnal energy conversion found that these locations showed little intraseasonal variation ( Osborne et al. 2011 ). In this work, moored velocity and density observations at mid- and inner-shelf locations are used to quantify internal tidal variability over

Full access
Emma Howard, Andrew McC. Hogg, Stephanie Waterman, and David P. Marshall

drag, with free-slip sidewalls. Fig . 1. (a) The meridional wind stress profile (N m −2 ) and (b) the physical domain. Colors indicate domain depth (m). Shading shows the location of the sponge regions in the buoyancy-forced simulations. Zonal flow in this model is forced in two ways. First, wind forcing is applied via a constant eastward wind stress that contributes to the momentum budget of the upper layer. The distribution of the wind stress does not vary zonally and is greatest at the center of

Full access
F. Sévellec, A. C. Naveira Garabato, J. A. Brearley, and K. L. Sheen

system, so that a single snapshot is enough to determine the vertical flow. However, the equation requires a fine spatial discretization (i.e., spatial derivatives along the three spatial dimensions). It has been shown to be extremely useful in the atmosphere, where radiosondes capture accurately the three-dimensional system’s state on a global scale at a given instant (but repeated measurements at the same location are impossible, that is, time derivatives are not measurable). In the ocean, spatial

Full access
Alice M. Grimm and C. J. C. Reason

interval 0.3 × 10 6 m 2 s −1 ), and (d) vertically integrated moisture flux (arrows, m g s −1 kg −1 ) and its divergence (contour interval is 0.75 × 10 −2 g s −1 kg −1 ). Dark (light) gray shading indicates confidence levels higher than 90% for negative (positive) anomalies, and only significant moisture fluxes are shown. Zero isolines are not shown. (e) Influence function for summer basic state for the easternmost action center numbered in (c). The values shown in each location are proportional

Full access
Jürgen Grieser and Francesca Terenzi

hazard intensity of event i at location n within its footprint. All property exposure that lies within the footprint area of an event gets hit by it. The damage that an event causes to a specific property at a given location, or an exposed subject at risk, depends on its structural characteristics represented by the specific vulnerability of this subject. The loss due to each individual event can be calculated if all the exposure hit by the event, the local intensity of the event at the

Full access