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10,                             PROGRAM OVERVIEW
11,
11,The SHARP Workstation (Skew T/Hodograph Analysis and Research Program) is a  
11,graphics-oriented package of programs that allows interactive analysis and
11,modification of sounding data. The software generates Skew T plots and
11,hodographs, and presents a wealth of sounding-derived information in
11,graphical and numerical format.
11,
11,Thermodynamic, wind and/or storm motion characteristics of the sounding can
11,easily be modified to portray suspected or anticipated conditions. An
11,operator can then view the effects of each modification on numerous derived
11,parameters and convective indices. This "Spreadsheet" capability provides
11,meteorologists with an ability to quickly survey a variety of alternatives,
11,and adds to the potential for diagnosing possible storm type and convective
11,trends in real-time. SHARP should be implemented into a forecast methodology
11,involving additional applications software, information and analysis.
11,
11,The program can also be used to create user-defined datafiles for eventual   
11,input into most commercial spreadsheet and database software. An added
11,ability to quickly access archived information allows SHARP to be used 
11,as a powerful research tool. In addition, comprehensive on-line help screens
11,provide an extensive list of current thunderstorm forecasting topics.
10,                            PARAMETER SCREENS
10,
14,After analyzing RAOB (or modified) data, the program presents (or updates) a 
14,wealth of information, including thermodynamic variables, convective indices,
14,and wind shear parameters. Comprehensive summaries are presented on four
14,numeric screens, with an options menu at the bottom of each screen.
10,
11,* The main screen presents CONVECTIVE POTENTIAL and WIND/STORM TYPE data.
11,
11,* The second screen represents the STORM ENVIRONMENT. It contains
11,  mean SHEAR (positive, negative, and total), storm-relative absolute        
11,  HELICITY (positive, negative and total), normalized HELICITY (rel), mean   
11,  VORTICITY (horizontal and streamwise), and mean storm-relative INFLOW      
11,  (total storm INFLOW and streamwise INFLOW) for specified layers.
11,
11,* The third parameter screen contains THERMODYNAMIC DATA and LAYER AVERAGE
11,  DATA. The THERMODYNAMIC DATA section contains temperature (T), dew point
11,  (Td), dew point depression (Tdd), mixing ratio (w), theta-e (TH-E), and
11,  relative humidity (RH) at specified levels. LAYER AVERAGE DATA contains the
11,  mean T, Td, Theta, TH-E, Theta-w (TH-W), w, and RH for specified layers.
11,
11,* The fourth screen contains WIND LEVEL DATA and PRESSURE LEVEL DATA.
10,                    PARAMETER SCREEN SUB-MENU OPTIONS
11,
14,(F1)-Print
11,* Prints (to the printer) a comprehensive list of meteorological data        
11,  associated with the observed or most recently modified sounding.
11,
14,(F2)-Main Menu
11,* Returns the Main Menu.
11,
14,(F3)-Skew T
11,* Displays the Skew T screen and the requested sounding.
11,
14,(F4)-Hodograph
11,* Displays the Hodograph screen and the requested hodograph.
11,
14,(F5)-Next Screen
11,* Pages through the parameter screens.
11,
14,(F7)-Help
11,* Accesses the on-line Help screens.
11,
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10,                     The CONVECTIVE POTENTIAL Screen
11,
14,K-Index
11,
11,* Represents thunderstorm potential as a function of vertical temperature    
11,  lapse rate (850T - 500T), low-level moisture content (850Td), and depth of 
11,  the moist layer (700Tdd).
11,
10,* K = (850T - 500T) + 850Td - 700Tdd
11,
11,* The K-Index favors non-severe convection, especially heavy rain-producing
11,  convection. Threshold values vary with season, location, and synoptic     
11,  setting. However, K values between 31 and 35 generally favor scattered     
11,  thunderstorm development east of the Rocky Mountains. Values over 35       
11,  indicate a potential for numerous thunderstorms, and pose an additional    
11,  flood threat, especially when a series of storms train over the same area.
11,
14,Precip Water (PW, inches)
11,
11,* Measures the depth of liquid water at the surface that would result after
11,  precipitating all of the water vapor in a vertical column. The SHARP       
11,  calculation uses a vertical column extending from the surface to 300 mb.
10,                         CONVECTIVE POTENTIAL - continued
11,
14,Showalter Index ( SWI, Celsius)
11,
11,* Calculated by lifting a parcel adiabatically from 850 mb to 500 mb. The    
11,  algebraic difference between the parcel and environmental temperatures at 
11,  500 mb represents the SWI.
11,
11,* The SWI is especially useful when a shallow cool airmass below 850 mb      
11,  conceals greater convective potential aloft. However, the SWI will continue
11,  to underestimate the convective potential for cool layers extending above  
11,  850 mb.
11,
11,* Since the SWI doesn't reflect near surface conditions, values will be      
11,  deceptively stable when moist layers exist below 850 mb.
11,
11,* The SWI is useful when tornadic potential is high, because the moist layer
11,  almost always extends above 850 mb during violent tornado outbreaks.
11,
11,* Increasing energy for parcel ascent is associated with greater negative    
11,  values of the SWI. SWI values between -4 and -6 indicate very unstable     
11,  conditions, and values below -6 show extreme instability.
10,                         CONVECTIVE POTENTIAL - continued
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14,LI (Lifted Index, Celsius)
11,
11,* A representative low-level parcel (LPL) is lifted adiabatically to 500 mb. 
11,  The algebraic difference between the parcel and sounding temperatures at   
11,  500 mb denotes the LI. Since the LI accounts for moisture below 850 mb, it 
11,  provides more reliable stability information than the SWI. Greater negative
11,  values of LI indicate increasing energy available for parcel ascent.
11,
14,LPL (Lifted Parcel Level; ft AGL, mb)
11,
11,* SHARP offers four options for defining the parcel to be lifted; PMAX (the  
11,  most unstable parcel within the lowest 150 mb), SFC (surface), MEAN (the   
11,  parcel with the mean thermal [potential temperature] and moisture [mixing  
11,  ratio] properties of the lowest 100 mbs) and SELECT (user-defined). After  
11,  selecting one of the lift options, the LPL (lifted parcel level) denotes   
11,  the level of the parcel used in subsequent buoyancy-related calculations.
11,
14,Tropopause (ft, AGL)
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11,* The tropopause height is taken directly from mandatory RAOB data.
10,                         CONVECTIVE POTENTIAL - continued
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14,Equilibrium Level (EL, ft)
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11,* The height (AGL) where a buoyantly rising parcel of saturated air again    
11,  becomes equal in temperature to the surrounding environment. Beyond this   
11,  point, the parcel becomes colder than the ambient environment, and         
11,  encounters the inhibiting effects of negative buoyancy.
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11,* Under the right conditions, severe storm tops can overshoot the EL by a 
11,  considerable distance without reaching the tropopause. Conversely,         
11,  non-severe storm tops can rise above the tropopause without overshooting   
11,  the EL. Consequently, the EL provides more meaningful information than the 
11,  tropopause for evaluating the strength of convective updrafts. 
11,
14,Max Parcel Level (MPL, ft)
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11,* The height on a Skew T (AGL) where the negative area above the EL          
11,  (encountered by an adiabatically rising parcel) becomes equal to the       
11,  positive area between the level of free convection (LFC) and the EL. This  
11,  marks the point where the momentum gained from kinetic energy is gone, and 
11,  signifies the highest attainable level of the convective updraft.
10,                         CONVECTIVE POTENTIAL - continued
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14,Wet-Bulb Zero (WBZ, ft)
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11,* WBZ heights between 7000 ft and 10500 ft (AGL) correlate well with large   
11,  hail at the surface when storms develop in an airmass primed for strong   
11,  convection. Higher values infer mid and upper level stability, and also    
11,  indicate a large melting area for falling hail. Lower WBZ heights indicate 
11,  that the low-level atmosphere is too cool and stable to support large hail.
11,
14,B+ (j/kg)
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11,* B+ represents Convective Available Potential Energy (CAPE), and defines the
11,  vertically integrated positive buoyancy of an adiabatically rising parcel. 
11,  Since CAPE is proportional to the kinetic energy that the parcel gains     
11,  while it is warmer than the surrounding environment, it provides the best  
11,  measure of latent instability. Increasing values of CAPE generally lead to 
11,  progressively vigorous convection. However, severe storms can form in      
11,  environments showing weak to moderate CAPE, especially if SR Helicity      
11,  values are high (see ENERGY/HELICITY Index). B+ is represented by SHARP as 
11,  the area between the parcel ascent curve and the environmental temperature 
11,  curve, from the LFC to the EL.
10,                         CONVECTIVE POTENTIAL - continued
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14,B- Area (j/kg)
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11,* B- represents the cumulative effect of atmospheric layers that are warmer  
11,  than a parcel (LPL) moving vertically along an adiabat. Low-level parcel   
11,  ascent is often inhibited by such stable layers near the surface (see Cap  
11,  Strength). If natural processes fail to destabilize the lower levels, an   
11,  input of energy from forced lift will be required to move the negatively   
11,  buoyant parcels to their LFC. Since B- is proportional to the amount of    
11,  kinetic energy that a parcel loses to buoyancy while it is colder than the 
11,  surrounding environment, it also contributes to the downward momentum of   
11,  descending air.
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14,Max UVV (Maximum Upward Vertical Velocity, m/s)
11,
11,* From parcel theory, Max UVV represents the greatest upward velocity that a 
11,  non-entraining parcel (LPL) can attain while rising adiabatically through a
11,  given sounding environment. Max UVV is determined by converting CAPE to   
11,  kinetic energy.
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10,* Max UVV = (2 * CAPE)^1/2
10,                         CONVECTIVE POTENTIAL - continued
11,
14,Cap Strength (Celsius)
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11,* Cap Strength (also known as the "lid" or "cap") measures the ability of    
11,  stable air aloft to inhibit low-level parcel ascent. Empirical studies show
11,  that a cap greater than 2C often precludes deep convection in the absence
11,  of strong dynamical or forced lift, even when instability is excessive.
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11,* On the other hand, the generation and ultimate release of extreme          
11,  instability often depends on the ability of a strong cap to prevent        
11,  overturning of the airmass by numerous, but ordinary convection. Without a 
11,  cap, convection tends to be widespread but less intense, because developing
11,  storms must compete for a limited amount of available moisture. By         
11,  preventing widespread convection, a strong cap allows low-level heat and   
11,  moisture to increase over a period of time. This delay in the onset of     
11,  convection increases the severe potential for a limited number of cells    
11,  that manage to punch through the cap, or reach the boundary separating     
11,  capped from uncapped regions. Severe storms often form along these lid     
11,  boundaries, where release of the latent instability is favored. As a       
11,  result, storms showing rapid growth within or very near a strongly capped  
11,  region often become severe.
10,                         CONVECTIVE POTENTIAL - continued
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14,Total Totals Index (TT, Celsius)
11,
11,* The TT combines the effects of vertical temperature lapse rate (Vertical   
11,  Totals Index, VT) and low-level moisture (Cross Totals Index, CT) to      
11,  estimate the potential for severe convection in a given environment.
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10,* VT = 850T - 500T   CT = 850Td - 500T   TT = (850T - 500T) + (850 Td - 500T)
11,
11,* When the TT exceeds 50 (east of the Rocky Mountains), the environment can  
11,  generally support a few severe thunderstorms, and isolated tornadoes. TT   
11,  values over 52 indicate a potential for scattered to numerous              
11,  thunderstorms, few to scattered severe storms, and a few tornadoes.        
11,  Environments exhibiting TT values greater than 56 can support numerous     
11,  thunderstorms, scattered severe storms, and scattered tornadoes.
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11,* High lapse rates, a source of low-level moisture, and cold 500 mb          
11,  temperatures will yield large values of TT. However, high lapse rates can  
11,  produce a large TT, with little supporting low-level moisture. The sounding
11,  must be examined carefully to ascertain the validity of the TT for a       
11,  given environment.
10,                         CONVECTIVE POTENTIAL - continued
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14,SWEAT Index (Severe WEAther Threat Index)
11,
11,* The SWEAT Index evaluates severe weather potential by combining the     
11,  effects of low-level moisture (850 Td), convective instability (TT), jet   
11,  maxima (850 and 500 mb wind speed), and warm advection (veering directional
11,  shear between 850 and 500 mb).
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11,* The SWEAT Index was designed to discriminate between ordinary and
11,  severe convection by incorporating thermodynamic information (850 mb Td and
11,  TT Index) and kinematic information (low and mid-level flow characteristics
11,  showing strong windfields and veering directional shear). 
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11,* SWEAT values above 300 indicate a potential for severe storm development;  
11,  values over 400 favor tornadic storms, providing a trigger exists for      
11,  releasing the potential instability.
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11,* SWEAT values can change dramatically during any 12 hour period. As a       
11,  result, the SWEAT index is most effective if index values remain high at   
11,  the onset of convective development.
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10,                         CONVECTIVE POTENTIAL - continued
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14,700 - 500mb LR (700 - 500 mb Lapse Rate, degrees C/km)
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11,* Used for evaluating the contribution of mid-tropospheric lapse
11,  rate to convective instability. Lapse rate information can also  
11,  be used for anticipating convective instability, when a region of
11,  high lapse rates is projected over an area exhibiting abundant low-level   
11,  moisture.
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14,TEI (Theta-e Index; degrees, Kelvin)
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11,* The TEI represents the greatest decrease in equivalent potential           
11,  temperature measured in a layer beginning at or below 700 mb. Consequently,
11,  the TEI evaluates the potential for elevated convection, and adds insight  
11,  where surface-based indices fail. The TEI can provide useful information   
11,  for diagnosing the potential for short-fused flooding events, especially  
11,  when warm, moist unstable air south of a warm or stationary front is forced
11,  isentropically over the frontal boundary by significant low-level winds    
11,  (e.g. greater than 20-30 kts). A TEI equal to or exceeding 5-10 degrees (C)
11,  indicates a potential for elevated convection, especially when isentropic  
11,  lift is probable.
10,                       WIND / STORM TYPE Parameters
11,
14,Mean Wind (0-6 km, direction/knots)
11,
11,* Represents a density weighted mean wind for the layer.
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14,Storm Motion (direction/knots)
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11,* Research indicates a strong relationship between the strength of a storm's 
11,  inflow and the ensuing convection (e.g. single, multi, supercell). As a    
11,  result, the rotational characteristics of developing storms are critically 
11,  dependant on their movement through the environment. Deviant storm motion  
11,  can foster a storm-relative environment favoring supercell organization by 
11,  providing the storm with strong low-level inflow and substantial streamwise
11,  vorticity (available shear vorticity in line with the storm inflow).
11,
11,* SHARP calculates an initial Storm Motion 30 degrees to the right of the    
11,  0-6 km mean wind, with 75 percent of its magnitude. This motion represents 
11,  the helicity potential that can be realized by a supercell deviating to the
11,  right of the 0-6 km mean wind, and is used for determining an initial      
11,  estimate of storm relative helicity (SR Helicity). Initial Storm Motion   
11,  can then be modified to reflect updated radar information.
10,                      WIND / STORM TYPE - continued
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14,BRN (Bulk Richardson Number)
11,
10,* BRN = B+/BRN Shear
11,
11,* The atmospheric response to forcing is strongly influenced by instability  
11,  (B+) and by vertical wind shear (BRN Shear). The BRN measures the relative 
11,  importance of these two parameters, and correlates well with observed storm
11,  type (e.g. single, multi, supercell), especially for B+ between 1500 and   
11,  3500 j/kg. BRN's less than 45 tend to support supercell structures, but    
11,  multicellular convection is favored over 45. While the BRN has shown some  
11,  value as a predictor of storm type, it is a poor predictor of storm        
11,  rotation because BRN Shear is a "bulk" measure (e.g. it doesn't address the
11,  specific effects of directional and speed shear components). SR Helicity   
11,  can be used with the BRN to assess storm rotation potential.
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14,BRN Shear (m/s)^2
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11,* Represents the vertical wind shear used in the BRN calculation. BRN Shear  
11,  is calculated by taking the vector difference between the 0-6 km density   
11,  weighted mean wind and the 0-500 meter density weighted mean wind.
10,                      WIND / STORM TYPE - continued
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14,SR Helicity (Storm-Relative absolute Helicity, 0-3 km, (m/s)^2)
11,
11,* SR Helicity depicts a summation of streamwise vorticity (shear vorticity in
11,  line with the storm inflow) through the storm inflow layer and measures the
11,  rotation potential that can be realized by a storm moving through the      
11,  vertically sheared environment. As such, SR Helicity is critically         
11,  dependant on existing shear vorticity, on storm motion and on the strength 
11,  of the inflow.
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11,* As a storm moves through the environment, the updraft tilts low-level shear
11,  vorticity into vertical vorticity if the inflow is sufficiently strong, and
11,  if the shear vorticity is sufficiently streamwise (in line with the storm  
11,  inflow). Significant streamwise vorticity (and SR Helicity) is likely when 
11,  strong storm inflow veers sharply with height within the lowest 2 or 3 km. 
11,  Accordingly, storms that can take advantage of strong inflow (greater than 
11,  20 kts), and significant storm-relative directional shear (greater than 70 
11,  degrees within the inflow layer), have greater potential for rotation.
11,
11,* SHARP calculates SR Helicity as an area bounded by the hodograph and the   
11,  storm inflow vectors at the top and bottom of the measured layer.
10,                      WIND / STORM TYPE - continued
11,
14,Pos Shr (0-3 km AGL, 10-3 s-1)
11,
11,* Positive shear (Pos Shear) represents a summation of 500 meter hodograph   
11,  shear segments showing clockwise curvature through the lowest 3 km of the  
11,  sounding. As such, Pos Shear measures the component of the mean            
11,  inflow-layer shear thought to contribute materially to updraft rotation.
11,  Pos Shear is determined by dividing the cumulative length of all hodograph 
11,  shear segments showing neutral or clockwise curvature, by the depth of the 
11,  layer. Pos Shr can provide useful information on the structure of the      
11,  vertical wind shear, but it doesn't represent important features of the    
11,  storm reference frame. Parameters such as SR Helicity should be used with  
11,  Pos Shear to assess rotation potential.
11,
14,SR Dir Shr (storm-relative directional shear; 0-3 km AGL, degrees)
11,
11,* SR Dir Shr portrays the directional difference between the storm inflow  
11,  vectors at the surface and 3 km. Large SR Dir Shr within this inflow layer 
11,  (generally greater than 70 degrees) contributes to storm rotation by       
11,  providing a potential for significant streamwise vorticity. However, no    
11,  amount of SR Dir Shr can compensate for weak inflow (less than 20 kts).
10,                      WIND / STORM TYPE - continued
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14,Energy/Helicity Index (EHI)
11,
11,* A balance between CAPE and SR Helicity within a given environment          
11,  apparently contributes to the formation of strongly rotating updrafts for  
11,  storms that persist. As a result, large values of CAPE are not essential   
11,  for violent tornado outbreaks. Intense rotating updrafts can form with     
11,  relatively weak instability if SR Helicity is high. On the other hand,     
11,  marginal SR Helicity can still support storm rotation if CAPE is large.
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11,* The EHI is based on empirical studies involving strong and violent         
11,  tornadoes, and represents potential tornadic intensity as a function of    
11,  CAPE and SR Helicity. Operational utility of the EHI is still untested, but
11,  values above 1 indicate a potential for strong tornadoes (F2, F3) when     
11,  additional severe weather indicators are present. Violent tornadoes
11,  (F4, F5) favor EHI values around 5.
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14,* As with any index, the EHI can only have operational value if it is used 
14,  in a broader context involving other sources of information and analyses.  
14,  No index (or group of indices) can or should be used as stand alone        
14,  measures for diagnosing the complexities of an atmospheric environment.
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14,                CONVECTIVE POTENTIAL and WIND / STORM TYPE
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10,                       The STORM ENVIRONMENT Screen
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14,SHEAR (10-3 S-1)
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11,* SHEAR contains mean layer values of positive shear (pos), negative
11,  shear (neg), and total shear (tot) for 0-1, 2, 3, 4, 5, and 6 km (AGL).
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11,* Vertical wind shear represents the change in the wind (direction/speed)    
11,  with height. This change in velocity is portrayed on the hodograph as  
11,  the shear vector, and implies baroclinicity. Stronger shear implies greater
11,  baroclinicity, and suggests important ageostrophic processes. A backing    
11,  (counterclockwise turning) vertical wind profile indicates cold advection. 
11,  However, veering (clockwise turning) winds often imply warm advection,     
11,  upward vertical motion, and destabilizing processes.
11,
11,* Weak vertical shear supports limited convective scale organization, and    
11,  generally leads to single or multicell storms. Increasing vertical shear   
11,  favors progressively better organization (multicell-supercell), especially 
11,  when the storm-relative environment contains an optimum blend of strong    
11,  veering flow, CAPE, and low-level forcing. Since violent tornadoes are     
11,  spawned by highly organized supercells, strong inflow shear and substantial
11,  directional shear represent key elements in tornadic environments.
10,                      STORM ENVIRONMENT - continued
11,
14,VORTICITY (10-1 S-1)
11,
11,* The VORTICITY section of the STORM ENVIRONMENT screen contains mean     
11,  layer values of horizontal vorticity (horiz) and streamwise vorticity      
11,  (streamwise) for 0-500, 1000, 1500, 2000, and 3000 meters (AGL).
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11,* Horizontal (shear induced) vorticity results mostly from vertical changes  
11,  in the horizontal wind; the horizontal vorticity vector is oriented 90     
11,  degrees to the left of the layer shear vector, but equal in magnitude.
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11,* For a given storm motion, streamwise vorticity refers to the component of  
11,  horizontal vorticity in line with the storm inflow, and represents the     
11,  amount of shear vorticity available for translation into a rotating storm  
11,  updraft. Studies indicate that a balance between low-level streamwise      
11,  vorticity and sufficiently strong storm inflow results in helical flow     
11,  within the storm updraft. Consequently, storms forming in strongly helical 
11,  environments favor the persistent rotating updrafts characteristic of      
11,  supercell storms. Additionally, the greater convective scale organization  
11,  due to helical flow results in longer lived storm structures, also a       
11,  characteristic of supercell storms.
10,                      STORM ENVIRONMENT - continued
11,
14,INFLOW (direction/knots, AGL)
11,
11,* INFLOW contains mean values of the storm inflow (storm) and the streamwise 
11,  inflow (streamwise) for 0-500, 1000, 1500, 2000, and 3000 meters.
11,
11,* The mean storm inflow for a layer is calculated by subtracting the storm 
11,  motion vector from the layer mean wind vector. This represents the flow 
11,  experienced by a storm as it moves through the environment.
11,
11,* Mean streamwise inflow for a layer portrays the fraction of layer mean     
11,  inflow aligned with the layer mean horizontal vorticity. Streamwise inflow 
11,  can be used with total vorticity or total inflow can be used with          
11,  streamwise vorticity to better understand the components of SR Helicity.
11,
11,* The magnitude of the storm inflow and the amount of storm-relative         
11,  directional shear impose a strong influence on subsequent rotation         
11,  characteristics of the convection. However, no amount of directional shear 
11,  can compensate for insufficient inflow. Multicell storms favor environments
11,  with weak inflow (less than 20 kts), but supercell often require           
11,  significant inflow to generate rotating updrafts.
10,                      STORM ENVIRONMENT - continued
11,
14,HELICITY  (m/s)^2
11,
11,* HELICITY contains the positive (pos), negative (neg), total (tot), and     
11,  normalized (rel) storm-relative absolute helicity (SR Helicity) for
11,  0-1, 2, 3, 4, 5, and 6 km. 
11,
11,* Rel (normalized mean storm-relative helicity) denotes the cosine of the    
11,  angle between specified layer mean storm-relative wind vectors and the     
11,  corresponding layer horizontal vorticity vectors. Since it represents the  
11,  ratio of streamwise to horizontal (shear) vorticity, Rel can indicate the  
11,  degree to which the storm-relative environment is conducive to updraft     
11,  rotation. However, Rel fails to account for the magnitude of the flow      
11,  entering the storm, so it is a poor predictor of storm maximum vorticity   
11,  (and of storm rotation) when the inflow is weak (less than 20 kts).
11,
11,* SR Helicity reflects a summation of streamwise vorticity through the storm 
11,  inflow layer, and measures the rotation potential available to a storm     
11,  moving through the vertically sheared environment. As such, SR Helicity is 
11,  critically dependant on the ambient shear vorticity, on the storm motion,  
11,  and on the subsequent strength of the storm inflow.
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14,                            STORM ENVIRONMENT
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10,                      The THERMODYNAMIC DATA Screen
11,
14,THERMODYNAMIC DATA
11,
11,* THERMODYNAMIC DATA contains temperature (T), dew point (Td), dew point     
11,  depression (Tdd), mixing ratio (w), theta-e (TH-E), and relative humidity  
11,  (RH) for the surface, 850, 800, 700, 600, and 500 mb levels.
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14,LAYER AVERAGE DATA
11,
11,* LAYER AVERAGE DATA contains layer mean values of T, Td, Theta, TH-E,    
11,  Theta-w (TH-W), w, and RH for the sfc to 900, 850, 800, 750, 700, and
11,  650 mb layers.
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10,                   WIND LEVEL DATA/PRESSURE LEVEL DATA
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11,* WIND LEVEL DATA contains the ground-relative and storm-relative wind data  
11,  associated with the actual RAOB levels. PRESSURE LEVEL DATA contains       
11,  temperature, dew point, and wetbulb temperature data from the actual RAOB  
11,  levels.