Naval Research Laboratory OM copyWashington, DC 20375-5000

|N NRL Memorandum Report 63520)

Environmental Measurements in the McKinleyClimatic Laboratory Main Chamber,

May 2-10, 1988

G. M. FRICK AND W. A. HOPPEL

Atmospheric Physics Branch

Space Sciences Division

October 5, 1988

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Environmental Measurements in the McKinley Climatic Laboratory Main Chamber, May 2-10,1988

12 PERSONAL AUTHOR(S)

Frick, G.M. and Hoppel, W.A.13a TYPE OF REPORT 13b TIME COVERED 14 DATE OF REPORT (Year, Month, Day) 15 PAGE COUNT

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Environmental measurements were made in the ma' chamber of the McKinley Climatic Laboratory atEglin AFB, Florida, to help assess the performance of ARM DSU-19 target detectors. The measurementsrevealed that the depolarization of backscatter from a *lpieaser was significantly greater for an ice fog than

a wet fog.

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CONTENTS

I. IN T R O D U C T IO N ........................................................................................

II. T E S T S ............................................................................................................ 7

il . R E M A R K S ................................................................................................... ... 23

IV. ACKNOWLEDGEMENTS .................................................................................. 23

A P P E N D IX A ............................................................................................... ... 3 1

A P P E N D IX B ............................................................................................... ... 4 5

Accession For

NTIS GRA&IDTIC TABUnannounced 0Just ifloaton

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Av a-Y A oi

ENVIRONM-ENTAL MEASUREMENTS IN THE MCKINLEY CLLMATICLABORATORY MALN CHAMBER, MAY 2-10, 1988

I. INTRODUCTICN

A. Purpose

These measurnts were made in support of the evaluation of HARM DSU-19target detectors (TDs). The TDs illmninate a volume using an infrared laserdiode and lock at the backscattered signal. It is possible that certan'atmospheric conditions may cause backscatter such that fuzing will occur.measurement of the envirorment in terms of visibility, aerosol particledistribution and water or ice content define parameters whJich could incer theperformance of the TDs.

B. Facility and Instrumentation

The measurements were made in the main chamber of the YcKiiley liaticLaboratory, located on Eglin AFB, Florida. The chamber has a vcl,-re cfapproximately 3,000,000 cubic feet, and can be cooled to -65 degreesFarenheit. Rain was simuilated by arrays of nozzles situated approxLmatel'v 40feet above t-he chamber floor, which produced rain rates up to five inches perhour over an area approxi'ately 50 x 100 ft. Both wet and ice fogs erecreated by bringing in warm humid air through an air handler at the too of thechamber and mixing it with the cooled chamber air using a large wind rrac'i ne,two snow machine fans helped to distribute the fog thrcughout the cnarmer.

Rain rates were measured with a tipping bucket rain gauge, along withoccasional carparisors to a standard rain gauge. Rain droplets were sized bVimpaction on a powdered mesh which -as photographed for later evaluaticn. The-mist coponent of the rain (10

The saturation vapor pressures over water and ice are given by the Gzff-

Gratch fonmulas:

logl0 ew =-7.90298 [-TS- 1]- 5.02808 logl0 Ts ]

- 1.3816 x 0 [10 'll344(1-T/TS) - 1]

+ 8.1328 X 10- 3 [!0-3.49149(Ts/T - 1)_ 1 + log,, e

for water, and wO

log,0 e i = - 9.09718 (To/T - 1) - 3.56654 log,, (T /T)

+ 0.876793 (1 - T/To) + lcsl0 eio

for ice.

where ew = SVP (mb) over water

e.= SVP (mb) over ice

T = Absolute Temperature (0K)

To = 273.16 OK

Ts = 373.16 OK

ew SV= SV T (1013.25o mb for std. atn.)

eio= SVP @ To (6.1071 h = 0.0060273 std. atn.)

These fornulas are plotted in Fig. 1.

The mixing of two saturated air masses results Ln a maxi:rtmn vaporpressure given by:

'4 e e, TTI1 e I + "-2 e 'IT1 -2qTem.x= Mat -

where enix = vapor pressure of the mixture

e I = saturation vacor pressure at TI

e = saturation vapcr pressure at '2

T, = Temperature of the wan air

T2 = Temperature of the cold air

M, = Mass of the humid air at tert-rature T1 ( =ia + 1v

= Mass of the dry air at temperature T2 ( ="a

Thus if droplet for-mation is inhibited, the vapor pressure ofthe mixture will lie along a straight line connecting the saturationvapor pressures el and e2 obtained frcm Fig. 1.

qw __ C

3

Since the saturation vapor pressure curve is slightly concave, thiswill always produce a supersaturation. As fog droplets are fo-ed,the latent heat wanms the mixture and decreases the supersaturationwhich inhibits further growth. The final temperature and liquid watercontent (LWC) can be conputed by solving heat balance equations forthe two air masses, including the latent heat of the water vapor.Let

Mivi = Initial mass of water vapor

ivf = Final mass of water vapor

Cpa = Specific heat of dry airCpv Specific heat of water vapor

C pw = Specific heat of water

L Latent heat of vaporization of water

Q1= Cpa Mla(TI - Tf) + Cpv Mlvf(Tl - Tf) - L (Mlvi - Mlvf)

+ C (Mlvi - M1vf) (T1 - Tf)

Neglecting the second and fourth tens b ecause they are relatively small

Q1 = Cpa Mla (TI - Tf) - L (Mlvi - Mlvf)

and for the cold, dry air mass

2 = 2 Cpa (Tf - T2 )

now Q1- Q2 = 0, so

Balance the heat lost by the wacrer air to that gai-ned by the cooler

air.

C T- f +L(M, M. ) 'Cpa Mia (TI- Tf) + L (Cvi - i - M pa (Tf - T2 ) = 0 i)

The water mi-xing ratio, w, is the mass of the ,-ter vapor L4vided by

the mass of the dry air. Thus

W Mv 0.622 e 0.622 e

1a p-e p

e = Partial pressure of water vapor

p = Total pressure (= 1013 mb)

4

now adnIvi = 'la w(T1 ) and Mlvf M "la w(Tf) so that eq. (1) becomres

Mla { Cpa ( T1 - Tf ) - L C w(T!) - w(Tf) I } + M Cpa ( Tf T2 =0

now the change in mixing ratio, Aw = w(T!) - w(Tf)

-0.622i062 e (Tl) - e(Tf)

where ew(T) can be obtained ftrm the Goff-Gratch forula.

Let f = Ma and f= M) + , then1 Ma~ 2 M + f

f, {Ca(Tf - TI) + L 0 [ew(Tf) - e (Tl)]} + f2 Cp( Tf - T2) = 0pa f 1 1013 w11 2Ca2

Once f!, f2, T1 and T are set, since C L and e_.(T1) are kncw-r, T,22pal e( 1

can be deternined by a simple iterative process.

The LWC can be approximately dete-nined by the relaticn

3 3.53 x 105 wLWC (g/ = T ( 1 - 0.61 w

Fig. 2 shcws the predicted L:;;C and fin-al : e.-ratures Fcr mixtures Z-f10% warn saturated air at temperature T1 (given cn the abscissa), withcold dry air at the temperatures abeled on the c.rves. The solidlines give the final temperature, read cn the left hand side c thefigure, and the solid lines give the I:NC, read on the right. Fcrexample; 10% warn saturated air at 3C0 C mi:

N) m" CtD Lf

m C-

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mV C% tar%,

Ln Oli

We have set in I 1/E = 3.00 to be consistant with the foz-rula used

with the HSS visicmeter, and calculated a from

N N 2a--£ . = 27r £ n. r.i=l I i=l 1 I.

where n. is the concentration (m- 3 ) of particles with radius ri (M),

as obtained from the PYS instruments. The calculated visual range can then heccmpared to that obtained fr=m the FSS visicmeter. A plot of visibility andLC vs. concentration of monodisperse water droplets is presented Ln Fig. 3.The visibility is given by the solid lines (decreasing with particleconcentration) and the LWC is given by the dotted lines (LncreasLng withparticle concentration).

E. Polarization Measurents

An instrument to measure the polarization of backscattered light f=:m iceand wt fogs was specially constructed for these tests. The "str---ntconsists of a He-Ne laser which illuninates the fog with a polarized beam, anda receiver that looks at the backscattered laser light, splits it intocomponents with polarization parallel and perpendicular to the outgoing heam,and provides voltage outputs proportional to their intensities. TIhis ail.,calculation of the polarization of the backscattered light Ln tez s of theoutput voltages. Thus

% Polarization = Vo - VxVo - Vx

where Vo (Vx) is the voltage output proportional to the Lntensity of tack

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fall velocities and droplet size distribution from the podered mesh. Table 1gives a synopsis of the rain data, and plots of the visual range dur-ng therain tests are presented in Appendix A. The lack of a direct correlationbeteen rain rate and visibility is evident from Table ., this is because thedroplet size distribution is dependent upon the flow through the nozzles.Figure 7 shows two size distributions obtained from the CA P data for the rainrates of 1.1 in/hr (curve A) and 1.0 in/hr (curve B). Curve B has many Tcresmall droplets (these are responsible for the reduction in visibility) becausethe flow rate through the nozzles was greater, producing a higher degree ofatcmization. The rain rate for curve B is less than for curve A becau.se thesmaller droplets drift a considerable distance and distribute the ^-ter over amuch larger area.

Table 1.

TLE RAIN RATE VISUAL RANG(in/hr) (A)

5/2/88 small nozzles1246-1251 0.6 3001252-1254 1.0 1501301-1308 1.0 701311-1318 1.2 401322-1329 1.5 221332-1341 1.5 191349-1406 1.9 15

5/3/88

0821-0827 0.8 2100833-0843 1.1 1500851-0902 1.0 500904-0919 1.3 350921-0935 1.7 18

5/4/88 large nozzles

0908-0916 1.4 1250920-0935 2.5 550941-0948 2.9 400952-1007 4.4 301012-1034 4.3 161043-1050 1.4 101051-1100 2.1 60 (est.)1102-1107 2.8 351115-1125 3.5 251133-1143 5.0 12

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B. Ice Foq

The ice fog tests were conducted on May 6, upon our arival at the chamberthat morning Am observed the chamber was already foggy. This was purported tobe due to an opening of the large chamber door earlier that morning. Uponentering our shelter in the chamber at about 1245 we recorded the visualrange to be approximately 80 m and the temperature as -48 OC. The very lowterperature ensured that the particles were ice, as was visually confi-d bytheir glint in the laser beam. At about 1344, as the w-ana humid air wasbrought in, the region in front of the wind machine had the appearance of aheavy snowston. Snow built up on and fell from the ceiling trusses of thevicinity of the wind machine. Within five minutes the chamber %as filled witha heavy ice fog and frost formed on all available surfaces. At 1354 thisfirst ice fog yielded a minimum visibility of 23 meters before it began todissipate, during this time the chamber temperature rose to -43.2 0 C. A secondfog, created by injecting more wann humid air at 1429, produced a .-tz.visibility of 41 m and brought the chamber temperature up to -33.31C. Silveriodide was burned and more humid air was injected at 1448, this tire weobtained a minimum visibility of only 45 m. Plots of the recordedvisibilities are given in Figs. 8 and 9.

The most interesting data from this test is that from the polarizaticninstrument, unfortunately this instrument only obtains adequate backscatzerwhen the visibility is less than about 30 m. Thus the first ice fog was theonly one to yield polarization data. Fig. 10 shows the polarizat.in andvoltage outputs frm the instrument for the ti:7es shcw-n. The polarization isgiven by the histograms and the O's (X's) denote the output voltages frm theparallel (perpendicular) ccnmonent. Figure 10 is of particular interest, forit shows that t-he ice fog did not simply depolarize the laser beam, butrepolarized it in a direction perpendicular to original polarization. Webelieve this to be due to the scattering of the beam by ncn-sherca'!.(probably needle-iLke) ice crystals which could have a large armcunt ointernal reflection and a preferred orientation during their fall. The icecontent of these fogs, given in Figures 11-13, was computed frcm t he CAP ardCSAS data and ass-mes solid spherical particles. The maximum, ice content cf1.9 -"3/m3 achieved during the first ice fog corresccnds to a visibility of 23in. Figure 14 give the size distributions of ice crystals for the tires 1354,1400 and 1404. These show the peak particle size to be at r=4 in, but give noindication of any distinguishing characteristic that set curves A and C aoartfrom curve B, as revealed by the differences Ln the polarization data(specifically the Xs) of Fig. 10. Figure 15 shows the size distributiCs atthe tLmes of maximum ice content for the three ice fogs. C=r-e A corresoonIsto a visibility of 24 m and an ice content (IC) of 1.9 =,13 /m3 , curve S is forVR=41 m, IC=3.3 an3/m3 and curve C is for VR=45 m, :C=3.0 =_3/im 3 .

C. Wet Fogs

The wet fogs were produced in a manner identical to the ice fogs, excectthe initial chamber temperature was held close to freezing. On _ay 9 theinitial chamber was -10 0 C and e Lnjected saturated air at 130 C at a rate of

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50 lbs/s. The first injection started at 0943, lasted for 7 min. and produceda thin ice fog (VPz500m). A second injection started at 1002 and lasted for 9min., the chamber wamned to about -31C, no ice was observed and a VR of 20 mwas obtained. A third injection starting at 1035 and lasting 9 minutesyielded a VP :r_ 14 m, while the fourth injection (15 min.) starting at 1120,accompanied ;y the burning of newspaper to provide additional condensationnuclei, resul:ed in a 10 m VR. At 1302 a 6 min. injection produced a 'R of15m. On May 10 the initial chamber terperature was -60 C and Awe injectedsaturated air at 310C. The first injection (starting a 0810) lasted for 7min. during which newspapers %re burned and a VR of 9 m. was obtained. Asecond injection began at 0823, lasted for 6 min. and brought the VR dc,.n to aminim=m of 6m. Figure 16, curves A, B and C give size distributicns for thefog at tires when the visibility was 15, 20 and 25 rn respectively. Figure 17gives three size distributions, all of which correspond to a visibility of 10m.

In contrast to the ice fog, the wet fogs produced al-mst nodepolarization, as can be seen in Figs. 18-21. Bar charts of visibility,liquid water content and computed visibility can be found _n Aprpendix B.

III. REwARKS

There were a couple of instances when the HSS visicrreter indicated hichvalues for the visual range that did not correscond with visual observaticr.Due to the time constant incorporated into the instrurent it then raequiredseveral minutes to settle to the proper value. Times at -which t-he ESS data maybe erroneous are: 5/4 1052-1058, 5/6 1347-1348 and 1430-1432. The two ti-.eson 5/6 appeared to coincide with the cperaticn of the overhead door durz.chamber hunidification.

when the visibility was less than about 9 m there -,re too rany particlesfor the P.S CSAS to properly size and count. This results in ernecus L;.Csand computed VRs during these times. in addition, there are severalc-iousdiscontinuities in the !;C and ccrr~uted VR data w..itich are not chvsicall-,,possible; if values at these specific tites are re-quired, socothi-g using theneighboring data should be used to obtain representative values.

IV. AMCvIEDG ,=TS

The authors .,uld like to thank Dr. Hezann Gerber fcr .s exer-assistance on the design of the polarization i-nst_-rent.

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Appendix A.

The following neasurermnts of the visual range were obtained with the SSvisia'eter during the rain tests.

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The following are measurenents of the visual range, obtained with the FSSvisicneter, and liquid water contents and visual ranges calculated f-= thePMS aerosol spectrcneter data obtained during the fogs.

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11111TITI-I TrTrT]TrM FThJVVTITTn T=TTJTrTyrmTI

82 S).2

co

-S 2

~17I.-j