1.Awsitr=791006 Skew T, Log P Diagram

Total Page:16

File Type:pdf, Size:1020Kb

1.Awsitr=791006 Skew T, Log P Diagram AWSITR=791006 .1. Revised THE USE OF SKEW T, LOG P DIAGRAM ANALYSIS AND FORECASTING DECEMBER 1979 Revised March 1990 (This June 1995 reprintingincludes allerrataand revisions to date, includinga minor change to the convective gust potentialforecast procedure on Page 5-41) . APPROVED FOR PUBLIC RELEASE; DISTRIBUTION IS UNLIMITED — AIR WEATHER SERVICE Scott Air Force Base, Illinois 62225-5008 Rovlsod March 1990 REVIEW AND APPROVAL STATEMENT . FX)R THE (-{)hl MANDFi R v 4 —- II Revkted March 1990 REPORT DOCUMENTATION PAGE 2. Report DJte: December 1979 (Revised March 1990) 3. Report Type : Technical Report 4. Title: I“he U.~eof /he Skew T, Log P Diagrom in Analvsis and Forecasting 7, Performing Organization Name and Address: }IQ AWS/XT, SCONAFB, IL 62225-5(X)X 8. Performing Organization Report Number: AWSnR-79/(X)6 (Revised) 11. Supplementary No[es: Reprinted in March 1990 m incorpx+tc the I’ollowing’ Novcmlx’r 1987 revision th:~l updates obsolete references and adds new stability indices and I[wmulas; AugusI IWM and March 1989 crra(a: and a March 1990 revision Lhal adds new stabili[y indices and log forecasting techniqu~$s Supcr$cdc$ AD-A 195862. 12, Dis(ribu[ion/Avtiilabiiity Slatement: Approved for public release: distribution is unlimi(ed. 13, Abstract: Describes the DoD Skew T, Log P diagram and provides instruclionq 011 il~ usc lnslruclton$ include how to plol data on the (iiagram and how to usc the dakr to (ieterminc unreported mc[~wr(ll{)gical clclncnls and a(mosphcric stabi lily, Also tells how to analym disco n[inu ities, stublc Iaycrs, ami cl Iluds, a~ wt’11 as how to (ISC [he plot(cd diagram to help Iorecust meteorological phcnonmna such us oircra~t icing an{! SC!crr corrvcclivc st{mns. Revised in November 1987 to add several new stabilily indices and provide instructions for plotting and wsing pressure allitu(lc curves. ‘1’hc March i9YU revision adds several new stabili(y indices and I’tnxasling uxhniqucs currently displwed on (he Satellite D8ta Handling System (SDHS), (he Aulornatcci Wet!lhcr Distrihulion Syslem (AWDS ), and microcomputer Skew T programs. 14, Subject Tcrrns: METF.OROL(W’I’,” WEAT}l ER, WEATHER FOREC’AS”I”l N(~, WI;4”l’til’.R ANAi. }’SIS. UPPER AIR, SOLINDING, atmcxphc’ric wmdmg, :Iuimphc’ric suihilit>, s[ahillly II I(IC’I. 111~’1~’(lrt)l{~~lc:iiwund Ing, n~c[c(m)loglcal anal >si.s,Skew “r. [ (Jg i’ diagrani 15: Number of Pages: 15~ 17. Sccurily Classtlictrhun ol Rt>jw)rt L’nciassi(icd IX. Sccurily CIassl(ication of thisPage: ( Inclasw!ic(i ][), Security C’lusslfication 0[ Atwuxl: Uncixsllicd 20, Limil~tion 01 Abstract: (11. Standard Form 298 .. Ill Revised March 1990 .- PREFACE This rcpm ([JrigitTiIlly issued (m I %plcmbcr IY52 as AWSM 105- [ 24) was converted (o an Air Wealher Scrvicc ‘lc~hnical Report (A WS[TR-79/(N)6) in Dcccmbcr 1‘J79. Surprisingly, lhcrc have been only minor chwrgcs in the lxrsic pr(~cdurcs for plotting, analyzing, and using [hc Skew T, Log P diagram over (he pas[ 35 years. The (WO rcccnt revisions (November 1987 wrd March 1990) arc primarily cmwerncd with ncw skrbilily indices. This rcprin[, which im orp(~ratcs al! r(cvisions and crra~:t (() {ia[c. was rwccssary [o replenish stock and fill outstanding orders for !his venerable document. Many (JI the chtmgc~ in (he 19X7 rcvlsl(m had to do wilt) updating ohsolctc rclcrcncc:s, but ins[ruc(i(ms l~)r plotting and using IIW pressure altitude curve were also a(klcd, as paragraph 3.7, A major change was the addi(ion (in Chap[cr 5) of several new sktbili(y indlccs, ahmg wilh lhcir descriptions and formulas. For Ihc Ia[(cr, AWS thanks Bill Henry of [he National Wca[hcr Scrvicc Training (’enter, whose pamphlet (’k .Wcw T, Log f’, Diu,grmn) provided mos[ ol [hc ma{crial. Tht. 1990 rcvisi(m Mhls scvcrai new slability indicts currently displayed on (he Satcllilc Datu Handling Syslcm (SDHS ), [hc Automa[cd Weather Diswihuiion Sys[crn (AWDS ), and micr(~omputcr Skew “r programs. For (hc microcnmpu[c’r in{iices, AWS/XTX used the vc>ry rcc(. n[ly puhlisbcd SLcw-/’ Profc.crion(ll, Version 2.3, 2 Novcmt)cr 1989. Thi~ revision also irrcludcs procedures [or dclcrmining a Fog S~~bili[y index, a Fog Point value, tind a Fog Thrcal value. This printing (March 1990) also incorporates August 1988 and March 1989 errata, Readers may note that many of the cquipmmrl rcfcrcnccs in Chaplcr 7 seem obsolete, These references (along with some of [hc equipment) arc being reviewed Ior possible updating in subscqucrrt revisions. Revleed Mnrch 1990 contents Page Chapter I-Introduction Organization of the Manual . , . 1-1 Reason for Choosing the Skew T, Log P Diagram . 1-1 Different Versions of the AWS Skew T, Log P Diagram . 1-2 Chapter 2-Description of tho Skew +7 Chart Isobars . ...2-1 Isotherms . ...2-1 Dry Adtabats, . ...2-1 Saturation Adiabats . 2-1 Saturation Mixing-Ratio Lines . 2-2 Thickness Scales . ...2-3 The 1000-mb Height Nomogram . 2-4 Standard Atmosphere Data. 2-5 Wind Scale . ...2-6 Contrail- Formation Curves . 2-6 Analysis Blocks . ...2-6 Chap/or 3-Plotting Sounding Data on tho Skew-l Chart General . ...3-1 Number of Soundings Plotted Per Chart . 3-1 Chotce of Color . ...3-1 Plotting Individual Elements . 3-1 Plotting Wind Data . ...3-2 Legend . ...3-2 Construction and Use of the Pressure Altitude Curve 3-3 Chapter 4-Determination of lJnroported Meteorological C)uantitios From Pi8ttod Soundings Introduction . ...4-1 Mixing Ratio . ...4-1 Saturation Mixing Ratio. 4-1 Relative Humidity . ...4-1 Vapor Pressure . .. o.. ...4-3 Saturation Vapor Pressure . 4-4 Page Comments on Temperature Parameters . 4-5 Potential Temperature . 4-5 Wet-Bulb Temperature . .. 4-5 . Wet-Bulb Potential Temperature . , . , . 4-5 Equivalent Temperature . 4-6 Equivalent Potential Temperature. , . 4-8 Virtual Temperature ...,. 4-9 Thickness of a Layer . 4-10 Height of the 1000- mb Surface . 4-11 Pressure Altitude . 411 Density Altitude, . 4-11 Convection Corfdensation ~evel . 4-12 Convection Temperature . 4-12 Lifting Condensation Level . 4-13 Mixing Condensation Level . 4-13 Level of Free Convection . 4-14 Positive and Negative Areas . 4-15 Equilibrium Level . 4-16 Energy Determinations on the Skew-T Chart . 4-19 Chapter 5–Determination of Stability The “Parcel” Theory as a Basis for Determining Stability and Instability . 5-1 General Comment on the Effect of the Assumptions in the Parcel Theory on the Utility of Parcel-Method Techniques . 5-2 The Parcel- Theory Assumptions Used in the AWS Skew- T Chart . 5-3 Identifying the Basic Types of Stability and Instability for Small Parcel Displacements in a Sounding Plotted on — the Skew- T Chart . 5-3 Description of Stability Criteria. 5-5 Discussion of Superadiabatic Lapse Rates . 5-6 Oscillation of a Parcel as a Function of Stability . 5-7 Note on Errors Caused by Use of the Observed-Tempera- ture Curve for the Virtual-Temperature Curve in Stability Determinations . 5-7 An Example of Stability Determinations on a Skew-T Chart . 5-9 Processes Which Change .i)~ Lapse Rate. , . 5-10 Non-Adiabatic Heating and Cooling Effects . 5-10 Instability from Surfa( Heatllug . 5-10 Stability from Surface Cooling . 5-13 Advection Effects . 5-13 Preliminary Remarks on the Effects of Vertical Motion . 5-15 Effects of Convergence and Divergence . 5-15 Cases Without Vertical Shrinking or Stretching . 5- lfj Cases With Conver~cr; (’e but Without Vertical Motion . 5-17 Cases With Divergence but Without V(rtical Motion . 5-17 The N()-Divergel)ce Case. 5- Ii’ In the Lower Atmosphere . 5-17 Inthe Upper Levels . 5- 17 HOVJ to Assess the Vertical-Motion Field In Practirc . 5- 18 Penetrative’ Conv~ction . “5- 20 ‘J i WAsed Mmrch 1990 Page Stability-Instability Criterta for Large Verticai Displacements . 5-20 Latent Instability . 5-21 Validity of Assumptions . 5-23 Procedure for Finding Whether Any Latent Instability Is Present . ..O 5-23 The Value of the Distinction Between Pseud* and Real- Latent Instability . 5-24 Utility of Latent-Instability Analysis in General . 5-25 Potential InstabUlty . 5-26 Effects of Lifting Potentially Unstable and Stable Layers . 5-28 Does the Whole Layer Become Unstable ? . 5-28 Superadtabatic Lapse Rates from Layer Lifting . , . 5-31 Effects of Divergence . 5-31 How Much Lift Is Needed for Release of Instability? . 5-31 Lifting’ of Potentially-Stable Layers . 5-31 Processes Which Change the Potential Instability . 5-31 Relation Between Potential and Latent Instability . 5-31 Slice Method . ;:;; The Stability Indexes ................................................................................. ......... The Showalkr Index ......................................................................................... 5’35 The Lifled Index ................................................................................................ 5-35 The Modified Likd Index ................................................................................. 5-36 The Fawbush-Miller Stability index .................................................................. 5-36 The Marlin Index ............................................................................................... 5-37 The Besl Lifted Index ........................................................................................ 5-37 The Model Lifkd in&x ..................................................................................... 5-38 The NGM LifmdIndex...................................................................................... 5-38 The “K”Index .................................................................................................... 5-38 The “KO”
Recommended publications
  • Thermodynamics
    Copyright© 2004, School of Meteorology, University of Oklahoma. Rev 04/04 Knowledge Expectations for METR 3213 Physical Meteorology I: Thermodynamics Purpose: This document describes the principal concepts, technical skills, and fundamental understanding that all students are expected to possess upon completing METR 3213, Physical Meteorology I: Thermodynamics. Individual instructors may deviate somewhat from the specific topics and order listed here. Pre-requisites: Grade of C or better in MATH 2443, PHYS 2524, METR 2024 (or 2413). Students should have a basic understanding of functions of several variables, partial derivatives, differentials of multivariate functions, line and surface integrals, the basics of state variables such as temperature, pressure, density, and volume, and basic energy concepts prior to starting this course. Goal of the Course: This course introduces the physical processes associated with atmospheric composition, basic radiation and energy concepts, the equation of state, the zeroth, first, and second law of thermodynamics, the thermodynamics of dry and moist atmospheres, thermodynamic diagrams, statics, and atmospheric stability. Topical Knowledge Expectations I. Basic Radiation Principles. • Understand the basic physical concepts of radiative transfer of energy, including radiation characteristics, quantities and units. • Understand the concepts of emission, absorption, and scattering of radiation. • For solar (short-wave) radiation, understand the definition of the albedo and know typical values for different surfaces. Understand the dominant causes of absorption and scattering of solar radiation in the atmosphere. • For long-wave radiation in the atmosphere, understand the important constituents (greenhouse gases) and processes affecting emission and absorption. • Be familiar and work problems using Wien’s Law, Stefan Boltzmann’s Law, and the Inverse Square Law.
    [Show full text]
  • Vertical Structure of the Atmosphere
    Chapter 5: Vertical structure of the atmosphere 5.1 Sounding of the atmosphere Fig.2.1 indicates that globally temperature decreases with altitude in the troposphere. However, already Fig.4.2 showed that locally the temperature can also stay constant with height (isothermal layer), or even increase (inversion layer). The actual stratification of the atmosphere is highly variable in space and time and is, thus, routinely probed by all national weather services. Generally, this probing consists of launching a radiosonde every 3 to 6 hours. Fig. 5.1: Photo sequence of the launching of a radiosonde on a ship and (on the right) the schematic structure of a radiosonde; La METEO de A à Z; Météo France ISBN/2.234.022096 The balloon is filled with hydrogen. Attached is a parachute to assure a soft landing, an aluminium foil to assure a high radar reflectivity and the actual sonde containing instruments for measuring pressure, temperature and humidity. For a description of the humidity sensor see chapter 3.4.1. Temperature, humidity and pressure are radiotransmitted to the station at the ground, while wind speed and wind direction are derived from telemetric data following the balloon by radar. The vertical profile of the atmosphere is then transferred on thermodynamic diagram papers. An eXample of such a representation can be found in Fig. 5.3. The diagram paper used here is a skew T –log p diagram paper which has a logarithmic aXis of pressure in the vertical and the isotherms are straight lines tilted 45° with respect to the horizontal. Other diagram papers are known also.
    [Show full text]
  • ESCI 241 – Meteorology Lesson 8 - Thermodynamic Diagrams Dr
    ESCI 241 – Meteorology Lesson 8 - Thermodynamic Diagrams Dr. DeCaria References: The Use of the Skew T, Log P Diagram in Analysis And Forecasting, AWS/TR-79/006, U.S. Air Force, Revised 1979 An Introduction to Theoretical Meteorology, Hess GENERAL Thermodynamic diagrams are used to display lines representing the major processes that air can undergo (adiabatic, isobaric, isothermal, pseudo- adiabatic). The simplest thermodynamic diagram would be to use pressure as the y-axis and temperature as the x-axis. The ideal thermodynamic diagram has three important properties The area enclosed by a cyclic process on the diagram is proportional to the work done in that process As many of the process lines as possible be straight (or nearly straight) A large angle (90 ideally) between adiabats and isotherms There are several different types of thermodynamic diagrams, all meeting the above criteria to a greater or lesser extent. They are the Stuve diagram, the emagram, the tephigram, and the skew-T/log p diagram The most commonly used diagram in the U.S. is the Skew-T/log p diagram. The Skew-T diagram is the diagram of choice among the National Weather Service and the military. The Stuve diagram is also sometimes used, though area on a Stuve diagram is not proportional to work. SKEW-T/LOG P DIAGRAM Uses natural log of pressure as the vertical coordinate Since pressure decreases exponentially with height, this means that the vertical coordinate roughly represents altitude. Isotherms, instead of being vertical, are slanted upward to the right. Adiabats are lines that are semi-straight, and slope upward to the left.
    [Show full text]
  • IMS4 Weather Studio
    IMS4 Weather Studio IMS4 Weather Studio is a unique tool for processing, analyzing and graphic presentation of the surface and upper air meteorological, radiation and climatological data. Processing, analyzing and presentation of data of various kinds Meteorological and Standalone application or integrated Supports standard Archive of various settings Pilot Briefing with IMS4 Message switching meteorological saved by individual users and data processing server formats The easy-to-use tool provides convenient way for objective • Topography analysis and displaying of complex data - real-time data • Actual or historical weather data from SYNOP and METAR distribution systems (GTS), SADIS, as well as data outputs from bulletins Numeric Weather Prediction models (NWPs). • NWP model output in GRIB format • Satellite and radar information IMS4 Weather Studio has an inestimable wide use in • SIGWX charts in BUFR format meteorological institutions, forecasting services, and crisis • Lightning locations centers, airports, at climatological research and dispersion • Flight Information Region (FIR) modeling and for many other users. Each layer allows customization by providing a wide choice of Layered maps setting options and the stored customized layer configurations The IMS4 Weather Studio allows easy creating, viewing and can be applicated easily over the maps. printing of the layered maps. The layers include among others: 1 IMS4 Weather Studio Visualization of thermodynamic diagram from local temp IMS4 Weather Studio - GRIB Model (station Prostějov, 1.5.2014 – 00.00, 12.00) Weather data Thermodynamic diagram Weather data can be displayed as numeric values at selected The IMS4 Weather Studio offers a tool to draw thermodynamic locations or grid points, or interpolated in the forms of color diagram.
    [Show full text]
  • 5 Atmospheric Stability
    Copyright © 2015 by Roland Stull. Practical Meteorology: An Algebra-based Survey of Atmospheric Science. 5 ATMOSPHERIC STABILITY Contents A sounding is the vertical profile of tempera- ture and other variables in the atmosphere over one Building a Thermo-diagram 119 geographic location. Stability refers to the ability Components 119 of the atmosphere to be turbulent, which you can Pseudoadiabatic Assumption 121 determine from soundings of temperature, humid- Complete Thermo Diagrams 121 ity, and wind. Turbulence and stability vary with Types Of Thermo Diagrams 122 time and place because of the corresponding varia- Emagram 122 tion of the soundings. Stüve & Pseudoadiabatic Diagrams 122 We notice the effects of stability by the wind Skew-T Log-P Diagram 122 gustiness, dispersion of smoke, refraction of light Tephigram 122 Theta-Height (θ-z) Diagrams 122 and sound, strength of thermal updrafts, size of clouds, and intensity of thunderstorms. More on the Skew-T 124 Thermodynamic diagrams have been devised Guide for Quick Identification of Thermo Diagrams 126 to help us plot soundings and determine stability. Thermo-diagram Applications 127 As you gain experience with these diagrams, you Thermodynamic State 128 will find that they become easier to use, and faster Processes 129 than solving the thermodynamic equations. In this An Air Parcel & Its Environment 134 chapter, we first discuss the different types of ther- Soundings 134 modynamic diagrams, and then use them to deter- Buoyant Force 135 mine stability and turbulence. Brunt-Väisälä Frequency 136 Flow Stability 138 Static Stability 138 Dynamic Stability 141 Existence of Turbulence 142 Building a Thermo-diagram Finding Tropopause Height and Mixed-layer Depth 143 Tropopause 143 Components Mixed-Layer 144 In the Water Vapor chapter you learned how to Review 145 compute isohumes and moist adiabats, and in Homework Exercises 145 the Thermodynamics chapter you learned to plot Broaden Knowledge & Comprehension 145 dry adiabats.
    [Show full text]
  • Thermodynamic Diagrams
    ESCI 341 – Atmospheric Thermodynamics Lesson 17 – Thermodynamic Diagrams References: Introduction to Theoretical Meteorology, S.L. Hess, 1959 Glossary of Meteorology, AMS, 2000 GENERAL Thermodynamic diagrams are used to graphically display the relation between two of the thermodynamic variables T, V, and p. Process lines represent specific thermodynamic processes on the diagram. Important process lines are Isotherms Isobars Adiabats Pseudoadiabats Isohumes A useful thermodynamic diagram should have the following general properties The area enclosed by a cyclic process should be proportional to the work done during the process. As many of the process lines as possible should be straight. The angle between the isotherms and adiabats should be as close to 90 as possible. CREATING A DIAGRAM WITH AREA PROPORTIONAL TO WORK We’ve previously used the p- diagram. Since work per unit mass is defined as dw pd the area on a p- diagram is proportional to work. The p- diagram is not very useful for meteorologists because The angle between isotherms and adiabats is very small Process lines aren’t very straight Volume is not a convenient thermodynamic variable for meteorology For meteorology it would be useful to have a diagram that uses T and p as the thermodynamic variables. However, we can’t just arbitrarily use T and p and hope that area will be proportional to work. We have to find a way of setting up the axes of our diagram so that area will be proportional to work. Let the variables for the axes be X and Y, and let X and Y be functions of the thermodynamic variables.
    [Show full text]
  • MSE3 Ch05 Stability
    chapter 5 Copyright © 2011, 2015 by Roland Stull. Meteorology for Scientists and Engineers, 3rd Ed. Stability contentS A sounding is the vertical profile of tem- perature and other variables in the atmo- Building a Thermo-diagram 119 sphere over one geographic location. Sta- Components 119 5 bility refers to the ability of the atmosphere to be Pseudoadiabatic Assumption 121 turbulent. Stability is determined by temperature, Complete Thermo Diagrams 121 humidity, and wind profiles. Turbulence and stabil- Types Of Thermo Diagrams 122 ity vary with time and place because of the corre- Emagram 122 sponding variation of the soundings. Stüve & Pseudoadiabatic Diagrams 122 We notice the effects of stability by the: wind Skew-T Log-P Diagram 122 gustiness, dispersion of smoke, refraction of light Tephigram 122 Theta-Height (θ-z) Diagrams 122 and sound, strength of thermal updrafts, size of clouds, and intensity of thunderstorms. More on the Skew-T 124 Thermodynamic diagrams have been de- Guide for Quick Identification of Thermo Diagrams 126 vised to help us plot soundings and determine sta- Thermo-diagram Applications 127 bility. They look complicated at first, but with a bit Thermodynamic State 128 of practice they can make thermodynamic analysis Processes 129 much easier than solving sets of coupled equations. Parcels vs. Environment 134 In this chapter, we first discuss the different types Soundings 134 of thermodynamic diagrams, and then use them to Buoyancy 135 determine stability and turbulence. Brunt-Väisälä Frequency 136 Flow Stability 138 Static Stability 138 Dynamic Stability 141 Turbulence Determination 142 building a thermo-diagram Finding Tropopause Height & Mixed-layer Depth 143 Tropopause 143 components Mixed-Layer 144 In previous chapters, we learned how to compute Summary 145 isohumes (the Moisture chapter), dry adiabats Threads 145 (the Heat chapter), and moist adiabats (the Mois- Exercises 145 ture chapter).
    [Show full text]
  • Student Study Guide Chapter 8
    Adiabatic Lapse Rates 8 and Atmospheric Stability Learning Goals After studying this chapter, students should be able to: 1. describe adiabatic processes as they apply to the atmosphere (p. 174); 2. apply thermodynamic diagrams to follow the change of state in rising or sinking air parcels, and to assess atmospheric stability (pp. 179–189); and 3. distinguish between the various atmospheric stability types, and describe their causes and conse- quences (pp. 189–203). Summary 1. An adiabatic process is a thermodynamic process in which temperature changes occur without the addition or removal of heat. Adiabatic processes are very common in the atmosphere; rising Weather and Climate, Second Edition © Oxford University Press Canada, 2017 air cools because it expands, and sinking air warms because it is compressed. The rate of change of temperature in unsaturated rising or sinking air parcels is known as the dry adiabatic lapse rate (DALR). This rate is equal to 10°C/km. When rising air parcels are saturated, they cool at a slower rate because of the release of latent heat. Unlike the DALR, the saturated adiabatic lapse rate (SALR) is not constant, but we often use 6°C/km as an average value. 2. Potential temperature is the temperature an air parcel would have if it were brought to a pressure of 100 kPa. Potential temperature remains constant for vertical motions. 3. The lifting condensation level (LCL) is the height at which an air parcel wising from the surface will begin to condense. The LCL depends on the surface temperature and dew-point temperature. 4.
    [Show full text]
  • 1.Awsitr=791006 Skew T, Log P Diagram
    AWSITR=791006 .1. Revised THE USE OF SKEW T, LOG P DIAGRAM ANALYSIS AND FORECASTING DECEMBER 1979 Re v i s ed Ma r ch 1990 ( Th i s June 1995 r ep r i n t i ngi nc l ude s a l l e r r a t a and r e v i s i ons t o da t e , i nc l ud i nga m i no r change t o t he conv e c t i v e gus t po t en t i a lf o r e c a s t p r oc edu r e on Page 5 - 41 ) . APPROVED FOR PUBLIC RELEASE; DISTRIBUTION IS UNLIMITED — AIR WEATHER SERVICE Scott Air Force Base, Illinois 62225-5008 Rovlsod March 1990 REVIEW AND APPROVAL STATEMENT . FX)R THE (-{)hl MANDFi R v 4 —- II Revkted March 1990 REPORT DOCUMENTATION PAGE 2. Report DJte: December 1979 (Revised March 1990) 3. Report Type : Technical Report 4. Title: I“he U.~eof /he Skew T, Log P Diagrom in Analvsis and Forecasting 7, Performing Organization Name and Address: }IQ AWS/XT, SCONAFB, IL 62225-5(X)X 8. Performing Organization Report Number: AWSnR-79/(X)6 (Revised) 11. Supplementary No[es: Reprinted in March 1990 m incorpx+tc the I’ollowing’ Novcmlx’r 1987 revision th:~l updates obsolete references and adds new stability indices and I[wmulas; AugusI IWM and March 1989 crra(a: and a March 1990 revision Lhal adds new stabili[y indices and log forecasting techniqu~$s Supcr$cdc$ AD-A 195862.
    [Show full text]
  • Sounding Analysis
    Operational Weather Analysis … www.wxonline.info Chapter 11 Sounding Analysis Introduction The term “sounding” is used in meteorology to describe a vertical plot of temperature, dew point temperature, and wind above a specific location. It provides a picture of how these parameters change as you rise into the atmosphere. These vertical data are used to determine atmospheric stability, precipitation type, and a glimpse of cloud location at one point in time. The primary source for these data is the radiosonde, an instrument package that is launched at numerous locations around the world at 00 UTC and 12 UTC. This coordinated launch provides a three-dimensional picture of the structure of the atmosphere twice a day. The actual launch time is one hour prior to nominal observation time due to the time it takes for the instrument to rise into the stratosphere. On a good day, the radiosonde will reach the 10 mb level. Another source of sounding data is satellite sounders. Due to their asynoptic nature, these data are usually integrated via data assimulation into computer forecast models. These soundings tend to be smoother than radiosonde profiles. Soundings are also available from computer forecast models. At most forecaster workstations you can click on a point on a map and get a forecast sounding for that location. This allows you to evaluate future soundings for precipitation type or stability. Radiosonde Data : A radiosonde is an instrument package that measures temperature, relative humidity and atmospheric pressure (RAOB). These data are transmitted back to the launch site by radio. Temperature, relative humidity and pressure can be used to calculate dew point temperature and the height of a pressure level, and a variety of other variables.
    [Show full text]
  • The Skew T Diagram, and Atmospheric Stability Table of Contents 1
    Spring 2011 ATSC 3032 – Weather Analysis and Forecasting: Skew T diagrams and Stability The skew T diagram, and atmospheric stability Table of contents 1. The aerological diagram ........................................................................................................ 4 i. Radiosondes ............................................................................................................................. 4 ii. Hydrostatic balance; the hypsometric equation ....................................................................... 4 iii. Aerological diagrams ............................................................................................................... 6 2. Skew T applications ............................................................................................................ 10 (i) The skew T diagram ............................................................................................................... 10 (ii) Determination of moisture parameters .................................................................................. 11 (iii) Lifting condensation level (LCL) ............................................................................................ 13 (iv) Potential temperature ............................................................................................................. 13 (v) Moist potential temperatures ................................................................................................. 17 (vi) Normand‟s rule ......................................................................................................................
    [Show full text]
  • MACROPHYSICAL PROPERTIES and a CLIMATOLOGY of ARCTIC COASTAL FOG in EAST GREENLAND GAËLLE FLORENCE GILSON Bachelor of Science
    MACROPHYSICAL PROPERTIES AND A CLIMATOLOGY OF ARCTIC COASTAL FOG IN EAST GREENLAND GAËLLE FLORENCE GILSON Bachelor of Science, Université catholique de Louvain, 2008 Master of Science, Université libre de Bruxelles, 2010 A Thesis Submitted to the School of Graduate Studies of the University of Lethbridge in Fulfilment of the Requirements for the Degree DOCTOR OF PHILOSOPHY Department of Geography University of Lethbridge LETHBRIDGE, ALBERTA, CANADA © Gaëlle Florence Gilson, 2018 MACROPHYSICAL PROPERTIES AND A CLIMATOLOGY OF ARCTIC COASTAL FOG IN EAST GREENLAND GAËLLE FLORENCE GILSON Date of Defence: January 26, 2018 Dr. H. Jiskoot Associate Professor Ph.D. Supervisor Dr. C. Hopkinson Professor Ph.D. Thesis Examination Committee Member Dr. M. Letts Professor Ph.D. Thesis Examination Committee Member Dr. J. J. Cassano Associate Professor Ph.D. Thesis Examination Committee Member University of Colorado at Boulder Dr. L. Flanagan Professor Ph.D. Internal External Examiner Department of Biological Sciences Dr. A. Bush Professor Ph.D. External Examiner University of Alberta Edmonton, Alberta Dr. S. Bubel Associate Professor Ph.D. Chair, Thesis Examination Committee DEDICATION This dissertation is dedicated to my grandparents Denise and André, age 91 and 97. iii ABSTRACT Arctic summer fog is a major transportation hazard and has implications for the cryospheric energy balance. In this thesis, the climatology and macrophysical properties of fog along the coast of East Greenland are explored, and local to mesoscale environmental conditions studied to explain regional differences. Using a combination of long-term synoptic weather observations and Integrated Global Radiosonde Archive data, novel automated methods were developed to classify liquid fog thermodynamic structure and calculate fog top elevation.
    [Show full text]