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UNCLASSIFIED F/G I/ ML

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MICROCOPY RESOLUTION TEST CHART

NATIONAL BUREAU OF STANDARDS 1% A

01IC fILECOBY

(0 ESMC-TR-87-04

PROBLEMS AND SUGGESTED SOLUTIONSRELATED TO DISPERSION FORECASTING

O UNDER SEA BREEZE CONDITIONSo

B. F. BoydT. L. WillongESMC/WE Staff MeteorologistPatrick Air Force Base, Florida 32925

5 May 1987

LECTE

Evaluation 1987 IApprovedfor Public Release;Distribution Unlim ited

Prepared forEASTERN TEST RANGERANGE SUPPORT OFFICEPATRICK AIR FORCE BASE, FLORIDA 32925

97J

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6a. NAME OF PERFORMING ORGANIZATION Sb. OFFICE SYMBOL 7a. NAME OF MONITORING ORGANIZATION

Office of Staff Meteorology (Ifapptiabe)ESMC /WER Eastern Test RangeEastern Space and Missile Cen er EtrA

6c. ADDRESS (City, State and ZIP Code) 7b. ADRESS (City, State and ZIP Code)

Patrick AFB FL 32925 Patrick AFB FL 32925

Be. NAME OF FUNDING/SPONSORING BSb. OFFICE SYMBOL 9. PROCUREMENT INSTRUMENT IDENTIFICATION NUMBER

ORGANIZATION Eastern Space (Ifappticable)

and Missile Center ESMC

Sc. ADDRESS (City. State and ZIP Code) 10. SOURCE OF FUNDING NOS.

PROGRAM PROJECT TASK WORK UNITPatrick AFB FL 32925 ELEMENT NO. NO. NO. NO.

11. TITLE (include Sezcurij/ty, lsiriatoaProblems and SuggesteaSolutions Related to Disp~lewion ForecastingJI'.O Ts810 AlL gRf(s*OndLitlons

T . - Ik1n n Ah _ , n ~13.. TYPE OF REPOIT 13b. TIME COVERED 14. DATE OF REPORT (Yr.. Mo., Day) 15. PAGE COUNT

Evaluation FROM 1987 TOJ1987 87-5-5 910. SUPPLEMENTARY NOTATION

17. COSATI CODES 18. SUBJECT TERMS (Continue on reverse if necessary and identify by block number)

FIELD GROUP SUB. GR. Sea Breeze, Disper-"ion, Range Operation, Meteorology

IS. ABSTRACT (Continue on reverse if neces.ary and identify by block number)

Problems in forecasting toxic effluent dispersion under sea breeze conditions at CapeCanaveral are examined. Land and sea breezes are fairly well understood in a general sense;however, in order to forecast dispersion and transport of toxic effluents or to assess theimpact of a major accident in a coastal region, smaller scale features of the sea or landbreeze must be considered. A case study is presented to demonstrate the problem. Importantsmall scale features associated with a land or sea breeze mdst be observed and measuredbefore they can be effectively modeled. Such measurmements must employ techniques thatyield observations with high spatial and temporal resolution. Techniques using SoundDetection And Ranging (SODAR) And Light Detection And Ranging (LIDAR) are proposed aspossible methods to provide high resolution measurements of the Cape Canaveral sea and landbreeze. ' ,, , r,; . r , "

20. DISTRIBUTION/AVAILABILITY OF ABSTRACT 21. ABSTRACT SECURITY CLASSIFICATION

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B. F. BOYD 305/494-5915 ESMC/WER

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PK)ULEMS AND SUGGESTED SOLUTIONSRELNfW1 0I DISPERSION FOREC ASTING UNDER

SEA UI(EEZE CONDITIONS

T. L. Wilfong and B. F. BoydOffice of the Staff MeteorologistEastern Space and Missile Center

Patrick Air forte 1ws, Florida 32925

AaSTRACT

problems in forecasting toxic effluent dispersion under sea breeze conditions at Cape Canaver4are examined. Land and sea breezes are fairly well understood in a general sense; however, in orderto forecast dispersion and transport of toxic effluents or to assess the impact of a major accidentin a coastal region, smaller scale features of the sea or land breeze must be considered A caestudy is presented to demonstrate the proble. Important small scale features associated with aland or sea breeze must be observed and measured before they can be effectively modeled. Suchmeasurements must employ techniques that yield observations with high spatial and temporal res-olution. Techniques using Sound Detection And Ranging (SODAR) and Light Detection And Ranging(LIDAR) are proposed as possible methods to provide high resolution measurements of the CapeCanaveral sea and land breeze.

INTROUCTION

Te Commander, Detachment 11, 2nd Weather Squadron, is the Staff Meteorolcgist to the omanderof the United States' Eastern Space and Missile Center (ESMC. One operational unit of ESMC is theEastern Test Range (ETvW. As a national range, the TR supports the National Aeronautics and SpaceAdministration (NASA), Army, Navy, Air Force, and foreign government space and missile programs.This support begins at Cape Canaveral and continues through the Caribbean and into the SouthAtlantic Ocean.

Detachment 11 personnel provide forecasts, observations, climatological studies, and oonsultantservices to a wide variety of range users, as illustrated by current programs supported (Table I)and nomabe.r of launches (Table II). iis unique mission, coupled with geographical location, haslead to the development of one of the betst meteorologically instrumented operational areas in theworld. An illustration of instrumentation at the ETR is the Weather Information Network DisplaySystem (WINDS). The WINDS consists of 16 permanent towers, 9 temporary locations, and other specialsites located within the Cape Canaveral Air Force Station (CCAFS) and the Kennedy Space Center(KSC). That network has been temporarily expanded to include another 26 sites, some of which areoff Federal property. Figure I shows the location of the towers with sensors mounted from 2 to 165meters (6 to 568 feet).

TABLE 1: Current ES4C Major Programs TABLE II: Annual ESNC Launch Support Summary

as of 30 Sep 86

Space Ballistic AF NASA NKVY AJW 7MAL

- Atlas Centaur - U. K. Polaris FY 86 6 4 45 9 64- Delta - Pershing I FY 81 3 8 21 6 38- Titan IV - Pershing II FY 82 3 13 28 8 52- Titan 34D - Poseidon FY 83 1 12 25 13 51- Ariane -Trident I FY 84 2 7 17 7 33- Space Shuttle - Advanced Trident FY 85 1 11 21 1 34

F86 6 .7. 18 _6 ;33Guided Missile

IRMTWAL .16 62 175 52 365- SHiAM

With the materials used in support of the unique mission of the ETR, dispersion is of someconcern. CQ4rVnt models used as fo~ecasting aids at the 4" have been discusaeo cocently, by Boydand Bowman, 1 Boyd and Overbeck, Taylor and Schuman, an~pnlehart otjl.16 Earlier reportsdealing with the problem at the hfR include Haugen and Taylor and Siler. 9

Diffusion modelingunder the best conditions presents a challenge. A omplete review of basic fffusion modeling, ascurrently practiced, was recently (1985) completed by Briggs and Binkowaki.v In their 209 plus

Approved for public release; distribution is unlimited

87 5 13 048

P"1941 report, supported by over 240I riet..rtqces, they limited their discussion tolbasicl atmospheric boundary-layer dittusion, leaving out the complications introduced by sourcebuoyancy, plum. deposition, chpinicil reactivity, and cxphez flows due to structures, large terrainfedtures, wdIE land-water boundaries". 'lb. purpose of this paper is to look at amu of those specifica

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Fiue2sshwthe sea and land breezes dnteasne-oupwrmoto ofE thsiroertenadoTiprsngari relace at th surrfe th coolrr

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When~~~~~~~~~Ln tharviinnag-caewnds ih h sea breeze develop s aalrcuatons tdin-

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upward ~ ~ ~ ~ ~ _________ MM notion of_______ th iFvrteln.Ti iigarisrpae ttesraewt olt

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Fig 3. Characteristics of a Lake Breeze Fig 4. Characteristics of a Land ares*oFrom Lyons et al (18) From Lyocns at a1 (16)

extent, both landward and seaward. It there is a large-scale wind blowing from land to sea, thesea breeze initially develops out at sea, advancing more slowly landward and reaching the coast muchlater in the afternoon like a cold front with its characteristic wind shift. A pictorialdescription of the known structural and dynamical, arameters defining sea (or lake) and lanbreezes (Fig. 3 and 4) was taken from Lyons t al.19

The sea breeze circulation system consists of a landxard current close to the earth's surfaceand a much weaker but deeper return flow above. The sea breeze (and associated land breeze) willvary with geographical location, season, time of day, and the synoptic scale weather pattern. Thetop of the landward current ranges from a few hundred mters near large lakes and middle latitudesea coasts to approximately two kilometers in the tropics. The landward penetration of khe seabreeze varies with the land-sea temperature contrasts and the prevailing synoptic situation. Underideal conditions the sea breeze is frequently observed as far inland as 36 to 71 ka from theseashore in middle latitudes. In tropical regions, the sea breeze sometimes reaches 106 to 266 kminland. maximum wind speeds are as high as a few tens of meters per second, while the verticalvelocities are about two orders of magnitude smaller. The daily maximum winds generally occurshortly after the temperature maximu.

LCAL PROBLEMS

The general structure of the sea breeze is well understood. Early studies by Hill 1 4 and Red2 6

investigated same features of the sea breeze in the Cape Canaveral area. Sea beeze mudels havesuccessfully reproduced broad effects of the sea breeze over southirn Flordia; ' ot er, thereis a distinct lack of observational data to validate and reinforce modeling efforts.. , Lack ofhigh resolution observations of sea breeze frontal slope, height, intensity, onset time, and speedof movement under various synoptic conditions seriously limits the modeling of toxic effluenttransport in a coastal environment. In tact, it remains to be demonstrated that current diffusionmodels can assess the complete Ampact of a major accident in a coastal environment in either a postevent or a prognostic manner. This is especially true in view of the recent reassessment ofexposure limits by the Surgeon General which resulted in lowering the acceptable limits.

There are a number of different parameters that must be forecast during a launch sequeno thatmay depend on sea breeze conditions. 'tiese include damage due to acoustic overpressures and disper-sion of possible toxic spi Is and rocket exhaust. With the advent of payloads containing radioisotopes, dispersion of the isotope debris in the event of vehicle destruction may also be nea-sary. As an example of an operational problem, consider the Space Shuttle launch scheduled for 1636EDT on 12 July 1985. As part of the launch sequence, a forecast of the rocket exhaust effluentdispersion ikrequired by four hours before launch time. The Rocket Exhaust Effluent DiffusionModel (REED) is used to forecast the dispersion of rocket effluent for Shuttle launches. Practic-ally speaking, the RKEDM provides reasonable estimates of concentration, dose and de ition, pro-vided the input meteorological parameters -- primaily temprature and wind profiles - are valid.There is no wind forecast capability in RU-4M itself, and the model assumes there is no horisontalvariation in the wind and temperature profiles.

Fig. 5: Surface Weather Map at 6806 Uii, Fig. 6: 500-4illiber Height Contours12 Jul 85 (From 22) . U s wi 12 Jul 85 (From 22)

Figures 5 and 6 show the surface and 5e millibar maps at 3 EDT,DT. A high pressure ridgedominated the region. Winds were southwesterly at less than 3.5 meters per second below 5000meters. With no synoptic chags expected, the forecast problem was the sea breeso . Figure 7 showsthe in deposition forecast made using winds actually observed at 1136 Bur using # rawinsmod andtower 6313 sensors. ?b provide a forecast toe launch time, the input wind profile was Subjectivelymodified to acoount foe the sea breeze etteet. Persistence was assumed above 975 nters. The RMoutput based on this forecast profile is shown in Fig. 8. By 1536 EDT a strong sea breeze had set

hCi PN:

Fig. 7: MM HM Gasvitational Deposition Fig. 8: RE CL Gravitational Deposition

Analysis Using Winds Observed at 1130 un Analysis Using Feorecast Winds Vaid at

in to about a kilmoter in height at the 14unch GPWKA NMO

site and winds aloft had become southeastrly. -- -- """Using winds actually observed at 1530 UM~r W104!" ]

9. This is only on example, but demonsatest¢ the Cimportanlce oft an acurate sea tbree/e forxe-*bt. , ' , -

Evolution of the s breze at C Cmnmverl

irregular. Further, the presence of the lcuJian

- and IM andn Rivers and the Indian River Laquo~n -present An alternating land/water terrain; thus,une would expect to see the effects ot ller---

scale feature. Figures li througjh 13 shlow the rig. 9t PI I HLrvitationl Depiixtionevolution of the lI&-W/soa breeze at four toower s - Analysis using Winds Observed at 1539 EDr'al I three silos roeth of th yort C."ver.AJ 1jjrq 12 Jul 85. FromS B%4 and homa (7)C~vral. lower 9V93 is neargestl th coias

. "Iw

gil3 is three miles inland; tower @403 is tour silos inland; and, 603 is eight miles inland. TheWINUS netwok provides data in five inute averages. 1b produce tha figures, data were gatheriedfrom the sensors at 16 motors (54 feet) and resol red into the east-west (U component) and north-houth (V omponent). Note that a north wind iz then repreented by a positive V, A a west wind isrepresenteld by a positive U. A seven pointr unning open (35 minute) was used to smoot the data.

With vry. light synoptic wind conditions, the tranition from the nighttime I"n beeze to thedaytime sea breeze can be taken as the point where the U component of the wind switches fromoffshore (+u) to onshore (-U). Times are di, playod in Eastern Standard Time (E.ST) rather thanDaylilght Savings Time in order to better represent true local (sun) time. by 1015 E;ST, the sea

-.--

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Fig. 17: 1ow WL3 r tind l t 16 Maitocs Fig. I I oer 0iL3 Gind at1 Meoton12 Jul 86 12 Jul 85

"ra MUMV IM &#O T

Fg 12 T 040 W a 16 m186

brez has' esalse near th coas at toe

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Fig. 12: Tower 1413 Winds at 16 Meters Fig. L3ll Tower 63 Winds at 16 Meters12 Jul 85 12 Jul 85breeze has established near the coast at tower '

003. At approximately 1110 it appears to havemoved three miles inland to tower 0303. Atapproximately 1120 it appears at tower 0803, butdoes not appear at tower 0403 until 1145. Loki geven further inland at tower 1108 which is 11nautical miles from the coastline, a sea breezecirculation appears at about 11655 (Fig. 14). It ,s I

'in these cases, as one would expect, maller scale t Ncirculations developed that affect the developnentof the large scale sea breeze. ibis effect c.an bemore dramatically seen by looking at unaphoLU. inthe horizontal plane.

Using a Barnes analysis technigqu, 3' 4

irrtfJ-uldrly sp ced data like that from the WINS Wwerscan be transferred to a regular grid system. ibiis -i 5 5technique was applied to the winds at 16 meters iMO.mum . res,from all available towers at 1630, 1169, ai.d 1130EST (Fig. 15-17). Wind patterns at 16 meters Fig.14: Tower 1198 Winds at 16 Meterschanged dramatically during that hour. At 1630 12 Jul 85EST one can see the sea breeze transition begin-ning along the coast and also along the banks of the Banana and Indian Rivers. By 1139 EST, theprimary sea breeze circulation appears well estakbished, and the effects of the secondary circu-lations can be prominently seen in the broader regions of the rivers. Several regions can be seenwhere convergence or divergence is ocurring. These are, of course, also regions of strong Upwardand downward motion respectively.

We have only looked at the near surface aspects of the land/sea breeze circulation in thisanalysis, but it does demonstrate the complexity of the toxic effluent transport problem in the CapeCanaveral area. Effluents are caught up in a complex circulation pattern that can carry then aloftand back down again. Effluents released near the coast before the onset of the sea breeze may becarried out to sea, only toreturn again as the circulation develops. The complete sea breezecirculation patterns - aid thus, the outcoe of a toxic release - cannot be completely describedwith noar surface data. Attempts to model such circulations. have met with good success in thegeneral sense; however, such circulations are highly depeident on local terrain conditions. Sitespecific characteristics must be modeled. Frinally, modeling efforts suffer from a lack of detailedobservations of the vertical and horLiontal btructure and time evolution of the land/sea breese.

Po1TlrlAL SOLUJIONSThe sea breeze is a complex phenomenon that presents a difficult three dimensional transportproblem under ideal circumtances. The problem is further complicated in the Cape Canaveral area byan irregular coastline and the presence of the Lanana and Indian rivers and the Indian River Lagoon.

In order to develop an adequate modl that wil I forecast the sea breese, detailed dbstvations arerequired of the sea breeze depth, structure, and behavior under varying synoptic conditions. Inorder to observe the evolution of the sea braze, aedsurest methods with high teoral aid spatialresolution inst be eloyed. Modern sounding techniues employin light aid sound provide two

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•Fig. 15: 16 MeterWinds at 1030 EST 12 Jul 85 Fig. 16; Same as Fig- 15 at 1190 ESTObtained by Harned

4 Analysis of tower dat.

possible observing systems. Such systein -ireanalogous to the familiar RADAR - , dio LJt,'LC-tion And Ranging -- but employ sound (SCuA) andILght (LIDAi) and have been bho t be ett. ctxve

tools in probing the atmosphere.2 ,2

a

Sound traveling in the atmosphere is scatteredby small scale density discontinuities -- *Lien- - •tially thermal turbulence. Operdting in a immuo-static mode, SDARs can project sound verticallyand use the returned signal to monitor the growth OP 01 - W., w-of the planetary boundary layer. Thermal turbu-lence generally exists throughout the atmos ere. ,At the top of the planetary boundary layer, strorj V E - -temperature gradients exist that result in paticulacly strong thermal turbulence. Similarly, atthe boundaries of a sea breeze front, strong te-perature gradients produce Utrejn yrbulence that

can be monitored by a SW)AL . , SOb thusemployed can detect the time evolution (it the W IV t~height of a land/sea breeze. By tilting beams to W o ,the north (or south) aid to the east (or west) andexamining the doppler shift of the bacitactteredsignals, profiles of the north-south dnd past-west m e d, O-wind components (V and U respectively) can bederived. These, of course, can be resolved into , ,Vhorizontal wind speed and direction. Similarly, 1,

the vertical wind component profiles (W) can bederived from a vertically looking beam. Power andsignal-to-noise ratio limit the SOmAIt to altitudesgenerally less than a kilmeterc. N"Woo U M

SWAM with wind profiling capabilities have Fig. 17s Same as Fig. 15 at l1i ESTbeen operated swccessfully in various locationsand conditions. Three have been deployed at Vandenberg AFS for over a year. Derived profilesindicate very well the evolution of the sea breeze there. In the ecuthecn part of the Great SaltLake Desert, 90DAM wme deployed to investigate detailed flow structure in the bouadary layer.

Dta were obtained on a sufficiently snall space 2Vand time scale to describe diurnal circulation 4 4

20 - d •

patterns in addition to more well defined disoon- 0

tinuities. For example, Fig. 18 depicts a time 6 J j

height wind profile that shows a cold frontalpassage on 16 December 1984. The near surfacefrontal boundary appears as a distinct narrow _ | .iitransition zone, whereas aloft the zone is more k k A

broad and diffuqe. .4 1-\

By contrast with SCOAR, a LIDAR system depends 4 (kk i b .

upon ambient aerosols to observe the structure ofthe boundary layer and determine winds. A LIDAR kuses a laser to transmit monochromatic light. -

Discontinuities in aerosols produce differential . k4backscattering of the incident laser light. m o ra I* go IS O Ns a Wbackscattered light is sensed by the LIDAR detec- m .. "" Im

tor and processed into a visual image. Whereas a

SODAR is inherently limited to a point nwasure- Fig. 18: SODAR Time Height Wind Profilement, a LIDAR can scan much like a [ADAIL By 16 Dec 1984. From Astling (2)scanning both in the horizontal and vertical (PPIand RHI ppans), a complete three dimensional picture of the boundary layer structure can bederived. 9 Figures 19 and 20 show HI scans in both a convective 'boundary layer a nra stablenocturnal layer. Wind profiles can be derived from LIDARs by tracking inhomogeneitiesV or usingthe Doppler shift of the backscattered light to measure the radial component of the wind.

1 7

77 3 4 -1 5 7 j

A 04__ .&.A

L ' lo~u[ " 1meeru J

Fig. 19: LIDAR Depiction of Clear Air CGrt- Fig. 26: LIDAR Depiction of Night Time O~n-vective Pluses. From E. Eloranta, University vective Plume Over Local Heat Source (Pond).of Wisconsin. / From E. Eloranta, University of Wisconsin.

The contrasting aerosol content of air ,asses in a cgastal area make LIDAR a natural tool forobserving a sea breeze. For example, Nakant and Sasano tracked the inland penetration of a seabreeze front and observed its structure in detail. It* observations were carried out over a regionof the Kanto Plain about 66 kim northeast of Tokyo, Japan. Figure 21 shows the position of the LIDARand the inland penetration of the sea breeze. Figure 22 shows a vertical cross section of the seabreeze front itself. The original figure showed measured aerosol concentration in terms of thevolume extinction coefficient crossection displayed by ten color slice levels. The figure isreproduced here to show the structure and slope of the front and the billows present.

SUMMARY

The general structure of a land/sea breeze is fairly q11 understood; however, numerical seabreezlmodels, and certainly diffusion modeling in coastal regions are still in an exploratorystage. Several numerical models have been developed that simulate a sea breeze; however, verifica-tion and application of these models have been hampered by a lack of detailed two and three dimen-sional measurements of the sea breeze wind structure, slope, speed of movemnt, etc. under varyingsynoptic conditions. The Cape Canaveral area presents unique challenges and opportunitips. Thecoastline is irregular. Alternating land/sea interfaces may give rise to secondary circulationsthat retard or enhance the primary land/sea breeze circulations. On the other hand, the area iswell instrumented. "e new tower network upgrade, when complete, will provide on of the largestosuo-scale netorks in the o ld and could provide measurements to study the near surface features

of the sea breeze. These measurements combined with those made with a network of S MDARs and a LIXWRcould provide the data sets needed for further model development and refinrent.

- ____ _ ___ ____A

/ 1500

L 500

5 10 14

Fig. 21: Penetration of the Sea Breeze in the MW (knKanto Plain on 15 Feb 84. Sites A-K supp] iedwind strip chart recordings. Arrows are wind Fig. 22: Graphical depictisa of a LIDAR scanvectors at 1700 Japan Standard Tin*. LIDAK showing the distribution of aerosol ooncentrameasurements were done in the region toundJed by tions in the sea breeze front in the Kanto Plainthe broken line. From NaKane and Sasano (20). on 15 Feb 84 at 1768 JST. Nakane and Sasano (20).

ACK MMOW 41

The authors would like to thank Edwin Eloranta at the University of Wisconsin for providingLIDAR photographs; Walt Lyons of RsCAN Corp for his helpful discussions; Rick Schumann of t24SCOCorp for preparing analysis fields; and Gry 'raylor of EISC Corp for providing the Barnes analysistechnique references.

I. ALgarwal, S. K. and S. Singal, (1980): A tudy of Atmospheric Structures Using SCDAR inRelation to Land and Sea Breezes, boundary Layer Meteor., 18, 361-371.

2. Astling, E. G., (1987): Remote Sensing of Vertical Profilers of Mesoscale Wind Discontinuitiesin the Boundary Layer, Preprints Sixth S)0 iwpoin Meteorological observations and Instrumentation,New Orleans, Amer. Meteor. Soc., 31-34.

3. Barnes, S. L., (1964): A Technique for Maximizing Details in Numerical Weather Map Analysis,J. Apipl. Meteor., 3, 396-469.

4. Barnes, S. L., (1973): Meso ale Objective map Analysis using Weighted Tim&-SeriesObservations, NSSL Tech. Memo, NSSL-62, 6

opp.

5. Bennet, R. C. and - R. List, (1975): LAke Breeze Detection With Acoustic Radar, Preprints 16thConference on Radar Meteorology, Houston, 1, Amer. meteor. Soc., 266-262.

6. Uubanan, C. H., J. R. ijorklund, dnd j. L'. kwtferty, (1985): oUser's Manual for the RevisedHEEDM (Rocket Exhaust Effluent Diffusion Model) Computer PrOgram for Launche at Kennedy Space Can-ter.* TH-85-157-03, H. E. Cramer Co., USAF Oitract F98606-83-C-0914,

7. Boyd, B. F., and C. R. Bowman, (1985): "buffusion odeling in Support of the Space Shuttle',presented at the Joint Afmy-Nvy-NASA-Air Force Safety and •Environmental Protection Sub itteeMeeting, Monterey, CA, 4-8 Nov 85.

8. Boyd, B. F. and C. R. Botan, (1986): Otrrdtional Use of Air Pollution models at the Space andMissile RdNe, Prerints Fifth Joint Conference on Applications of Air Pollution Meteorology,Chapel Hill, N. C., Amer. Meteor. Soc., 315-3lu.

9. Boyd, B. F. and K. B. Overbeck, (1987): Forecasting Atmospheric Sonic Propagation at the EasternTest Range (Paper AIAA-87-6012), AIM 25th AerospaCe Sciences Meting, RMo, NV.

10. Briggs, G. A. and F. S. Sinkowki, (1985): mesearch on Diffusion in Atmospheric BoundaryLayers: A Position Paper on Status and Needs, 131A1600/53-85/72, 227pp.

-- mmm mmmm mm 1 a m mm mmm mm~mm m -a

11. Chang, L. P., E. S. Talke, and R. L. Soni, (1982): Development of a Two Dimenbional Finite-Element PiL Model and Tw Preliminary Model Applications, Mon. Wea. Rev. 119, 2027-2037. 4.

12. Englehart, R. W., B. W. Bartram, H. Firtte~nberg, R. W. JubaCh, and F. R. Vaughn, (1987):OInnovative eteorology and Developnent in U. S. Space Radioisotope Power Safety RiskAssessments," the Fourth Symposium on Sj-Ace Nuclear Power Systems, Albequarque N. M.0 12-16 Jan-87.

13. Haugen, D. A. and J. H. Taylor, (1963): l1t. Ocean Breeze and Dry Gulch Diffusion Programs,Volume 11, Ak'CRL-83-791 (11), Air Force Caubridye Ppsearch Lab, Hansom Field, MA, loopp.

14. Hill, C. K., (1967): Study of the LAnd xOd Sea Breeze Regimes at Cape Kennedy, Florida, ftraMay 23 through September 1966. NEA 'AC brauich Mmo R-ALRO-YE-29-67, 12pp.

15. Hooper, W. P. and E. W. Eloranta, (1986): Lidar Measurements of Wind in the Planetary BoundaryLayer: The Method, Accuracy and Rezults from Joint Measurements with Radiosonde and Kytoon,J. Clim. Appl. Meteor., 25, 990-10o1.

16. Kunkel, K. E., E. W. Eloranta, and S. '. Shipley, (1977): Lidar bservations of the Convectiveboundary Layer, J. Appl. meteor., 16, 1306-1311.

i. Lawrence, T. R., B. F. Weber, M. J. Post, R. M., Hardesty, ind R. A. Richter, (1986):Comparison of Doppler Lidar, Rawrnonde, and 915-Mliz UHF Wind Profiler Measurements ofTto-osxair ic Winds, NO4A-TM-E.RL-WPL.- 10, 89pp.

18. Lyons, W. A., C. S. Keen, and J. A. Schuh, (1983): Modeling MesosCale Diffusion and TransportProcessets for Releases within CodStal Zones uring Land/Sea Breezes, NUPlD/CR-3542, 1 84pp.

19. Lyons, W. A. and R. A. Pielke, (1985): lvrecasting Sea Breeze 'Tunderstorms Using a MesoscaleNumerical Model, Final Report to NASA, Contract No. NAS10-11142.

20. Na an, H. E. and Y. Sdsano, (1986): Structure of a Sea-areeze Front Revealed by Scanning Lidarobservations, J. Meteor. Soc. Japan, 64, 707-196.

21. Ntt, W. D. and R. L. Coulter, (lvdti): Acoustic Remote Sounding, Probing the Atmosphericboundary LWyer, Amer. Meteor. Soc., Huston MA., 281-239.

22. NoAA: *Daily Weather Maps, Weekly Serit-L., July 8-14, 1985, National Meteorological Center,National Weather Service.

23. Peterson, F. L., N. 0. Jenson, and U. P. ienson, (1976): A esoscale Phenoenon Revealed by anAcoustic Sounder, J. Appl. Meteor., 15, b62-bu4.

24. Pielke, R. A., (1978): mesOcale meteuruj. ical modelinq, ACadeMic Press, 612pp.

25. Pielke, R. A., (1974): A 0"arison of 11 ce-65imensional and T1o-Dimensional NumericalPredictions of Sea Breezes, J. Atm. Sci.. 31 1577-1585.

26. Aeed, J. W., (1979): Cape Canaveral Sea Breezes, J. Appl. Meteor., 18, 231-235.

27. Rizzo, K. R., and W. A. Lyons, (1977): AcuuftiC Sounder Measurements of Summer Mixing Depths inCo4stal Environments. Preprintu Conterence Un APPI ications of Air Pollution Meteoroloqy, AMS, SaltLake City, 68-71.

28. Schwiesow, R. L. (1986): Lidar l4easureitunt of Boundary-Layer Variables, Probing the Atmospherictjoundary Layer, Amer. Meteo. Soc., boston, MA., 139-162.

29. Siler, R. K. (1989): A Diffusion Climatology for Cape .Canaveral, Florida, NASA TechnicalMemorandum 58224, 43pp.

30. Simpson, J. E., 0. A. Mansfield, J. N. ti LIord, (1977): Inland Penetration of See BreezeFronts, Quart. J. R. Met. Soc., 103, 47-76.

31. Taylor, G. E. and R. A. Schuman, (19U6): A [escription of the Meteorological and Range SafetySupport (MAiSS) System, r nts Fifth Joint Conference on Applications of Air PollutionMeteorology, Chapel Hill, N. C., Amer. Meteor. Soc., 133-136."

32. Wexler, R. (1946): Theuoy and Cbservations of Land and Sea Breezes, Bull. Amer. Meteor,. Soc.,27, 272-287.

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