Iamap/Iapso Abstracts Volume 1

IAMAP/IAPSO MELBOURNE

JANUARY 1974

ABSTRACTS VOLUME 1

UAPRC MPR US CR SB 1 IAMAP/IAPSO COMBINED FIRST SPECIAL ASSEMBLIES MELBOURNE, JANUARY 1974. ABSTRACTS VOLUMES

LIST OF SYMPOSIA

VOLUME 1

IAMAP UAPRC Upper atmosphere, pollution, radiation and climate. MPR Meteorology of the polar regions.

US "• Meteorological sessions. CR Clouds and radiation. SB Surface biometeorology.

1 VOLUME 2 Joint IAMAP/IAPSO FR Frontiers sessions. I IAPSO PO Physical

Abe, T. PO-35 Bigg,E.K. UAPRC-1-6 Abhyankar,V.V.[C] US-IV-5 Bigg,E.K. US-III-1 Ackerman.M. UAPRC-6-6 Bigourd,C. CR-I-9 NA Adams,G.W. UAPRC-5-2 Birch,J.R.[C] UAPRC-3-5 Adem,J. AS-I-7 Black,P.G. US-VI-3 Ahearn,J.[C] OW-I-11 Black,P.G. AS-I-2 Alexandrov,A. S. MPR-II-4 Black,P.G. AS-IV-4 Allison,I. MPR-I-7 Blackman,D.R.[C] OW-I-2 Alyea,F.N.[C] UAPRC-11-2 Blake,D. UAPRC-14-1 Andrews,J.C. PO-6 Boer,G.J. UAPRC-9-6 Antonia,R.A. US-V-1 Bolle,H.-J.[C] UAPRC-3-4 Ardouin,B.[C] US-I-6 Bonmarin,P.[C] A3-IV-7 Arya,S.P. s. MPR-I-3 Bossolasco,M. US-II-8 Arya,S.P.S. GARP-I-2 Bourke,W.p. GARP-I1-1 Asano,S.[C] CR-I-5 Bourke,W.P. GARP-II-2 Astafurov,V.G.[C] US-II-4 Bowden,K•F. ED-2 Astapenko,P. MPR-II-7 Boyd Barker,D.[C] UAPRC-3-3 Bradley,E.F, GB-I-5 Brekhovskikh,L.M. OE-1 B Bretherton,F.P.[C JPO-37 Baines,P.G. OW-II-2 Braslau,N.[C] CR-II-3 NA Baker,D.J.[C] OW-III-6 Briggs,B.H. UAPRC-8-4 Baker,D.J. OE-14 Briscoe,M. OE-5 Bsng,N.D. OW-II-3 Britaev,A.S. UAPRC-5-3 Bang,N.D. OW-III-5 Britton,G.P. AS-I-9 Bangham,M.J.[C] UAPRC-3-5 Brook,R.R. as-i-2 Banner.M.L. OW-I-1 Brooks,J.N.[Cl UAPRC-3-3 Barabash,M.B.[C] UAPRC-7-6 BrooJis,J.N.[C1 UAPRC-3-6 Barbee,W.TC] OW-II-1 Brophy,R.G.[C] US-VI-6 Barber,R.T. OE-7 Brown,R.A. MPR-I-4 Barenblatt,G.I. SB-I-3 Brown,R.A. PO-2 Barker,A.A. DC-7 Brown,W.E. PO-31 Barker,D.B.[C] UAPRC-3-3 Bryan,K. AS-III-5 Barker,D.B.[CJ DAPRC-3-6 Bryazgin,N.N. MPR-I-5 Barnett,J.J. US-VII-1 Buat-Menard,P.L C1 AS-II-7 Barnett,T.P. AS-III-16 Buchwald,V.T. OVJ-III-14 Barrick,D.E. OW-I-8 Budd,W.F. MPR-I-6 Bean,B.R. GARP-1-5 Burkert,P. UAPRC-3-4 Belmont,A.D. UAPRC-9-3 Burkov.V.A. PO-18 Belyaev,V.S. PO-16 Burova,L.P.[Cj MPR-II-3 Belyaev,V.S. PO-17 Businger,J. AS-IV-1 NA Bennett,A.F. ED-15 Bye,J.A.T. PO-13 •'..* Bernhardt,K. US-V-5 Bykova,L.P.[C] SB-I-4 Bernstein,R. PO-12 Byutner,E.K. MPR-I-2 Berlyand,M.E. UAPRC-13-3 Berlyand,M.E. US-III-5 NA Bezvikonniy,K.[C] MPR-II-7 Bielitch,R.B.[C] US-IV-7 Dickson,R. R. AS-III-2 Dolganov,L.V. [C] MPR-II-5 Donaldson,C.du P .[C] UAPRC-12-2 c Donelan.M. OW-I-6 Cadle,R.D. UAPRC-2--1 DoneIan,M. AS-II-8 Carstens,J.C.[C] US-III-7 Donguy,J.R. PO-5 Carver,J.H. US-I1-9 Doos,B.R. FR-II-2 N Carver,J.H. US-VII-3 Doronin,Yu.P. MPR-I-8 K Castleman,A.W. UAPRC-1-4 Downey,W.K.[C] AS-III-4 Cattle,H. AS-IV-9 Dubov,A.S. SB-I-4 Chabert d'Hieres,G. OW-II-13 Durbin,P.A.[C] PO-38 Chacko,0.[C] US-IV-5 Dutsch,H.U. UAPRC-4-3 Chacko,0.[C] US-V-9 Dworski,J.G.[C3 OW-II-1 Chacko,0. SB-II-6 Chalikov,D.V.[C] AS-III-11 NA Chandra,S. US-V-3 E Chashechkin,J.D.[C] PO-36 Efimova,Ii.K.[C] US-II-6 Chayanova,E.A.[C] UAPRC-2-3 Elachi,C.[C] PO-31 Chesselet,R.[C] AS-II-7 Elena,A.[C] US-II-8 Christie,A.D, UAPRC-6-5 Elford,W.G. UAPSC-8-5 Church,J.A.[C] ED-5 Elford,W.G. US-III-3 Clark,J.H.E. UAPBC-10-3 Elliott,B. ED-3 Clarke,R.A. ow-iri-4 Elliott,J.A. PO-39 Clarke,R.H. AS-IV-8 Elliss,J.LC] CR-II-7 Clarke,R.H. GARP-I-1 Emmanue1,C.B.[C] GARP-I-5" Coantic,M. AS-IV-7 Evans,W.F.J. UAPRC-3-2 Cohen,A. US-IV-4 Eyre,W.S. PO-1 Cohen,A. UAPRC-2-2 Ezraty,R.[C] AS-IV-7 Colin,C. PO-4 Contiliano,R. IC] UAPRC-12-2 Coulman,C.E. DC-1 F Cowan,1. FR-III-2 NA Fabian,P.[C] UAPRC-5-5 Cox,S.K. CR-II-2 Fandry,C.B. PO-37 Craig,R.A. UAPRC-13-4 Fedorov,K.N.CC] OE-1 Cresswell,G.R. PO-4 2 Fedorov.V.V.CC] UAPRC-7-5 Csanady,G.?= PO-10 Fedorov,V.V.[CJ MPR-II-6 Cunnold,D.M. UAPRC-11-2 Feigelson,E.M. CR-II-1 Curley,S.[Cl OW-I-11 Filippov,V.V. US-V-8 Curtin,D.G.[CJ US-I-3 Firing,E. OW-lll—xO Fleming,J-W. fc 1 UAPJSC-3-5. Fleming,R.J. . GARP-II-6 t D Fofonoff,N.P.[C] 4. OE-«5 Dam el son, E. F. [C j TAPRC-2-1 Foken,T.tC] HSTIV-21 •' Danielsor.,". F. UAPRC-10-5 FoHiin»Ii.M- [C] " OE-I P'ir.iclson,':'.F. [C]UflPRC-14-3 Fomiii/L.M. FR-III-3 K Dartt,D.G. lC~i UAPRC-9-3 Foster,T.D. DC-17 = £ Oave.J.V. CR-IT-3 NA Fouqart,Y. CR-I-9 ...N US-V-9 Franceschini,G.A. CR-I-7 , Do,A.K.[C3 s Daaven,D.G.[C1 UAPRC-10-5 Frankignoul,C. OW-II-4 ^ Deland,R.«J. UAPRC-9-1 Frassetto,R PO-24 Do land,R.J. GARP-IV-3 Friedrich,H.LC] AS-III-121 Del Beato.R. DC- 6 Frisch,A.S. AS-IV-3 * Denisov,Y.M. US-III-4 Fritz,S. FR-I-1 N Denmead,O.T., SB-I-1 Fukuchi,N.[C] PO-35 Denton,R.A. DC- 10 Fukuoka,S. ED-11 , •' Fusey,F.X.[C] De schamps # P. Y. AS-I-1 AS-I~1 f, Desikan,V.[C] US-IV-5 Fymat,A.L. CR-I-3 Fymat,A.L. GARP-IV-4, Han,Y. C OW-III-7 Hansen,D.V. [Cl GARP-III-4 Harries,J.E. UAPRC-3-5 G Harris,R.D.[C] UAPRC-5-2 Gaigerov,E.S. UAPRC-7-5 Harwood,R.S. UAPRC-7-4 Gaigerov,S.S. MPR-II-6 Harwood,R.S. UAPRC-14-4 Garbalewski,C. UAPRC-2-4 Hasse, L. AS-IV-12 Galbally,I.E. US-VIi"-7 HasseJmann,K. FR-I-3 NA Gambo,K. AS-IV-10 Hayden,C.M.. [C] GARP-IV-2 Garratt,J.R.[C] US-VII-6 Heath,D.F. UAPRC-6-3 Garratt,J.R. SB-I-2 Heath,R.A.[Cl OW-III-2 Garrett,C. OW-II-5 Heath,R.A. ED-14 Gascard,J.[C] DC-15 Hempel,G.[C] OE-7 Gates,W.L. AS-III-7 IIenin,C.[C] PO-5 Gauntlett,D.J. GARP-II-5 Herman,G.F. UAPRC-7-2 Gavrilin,B.L. PO-20 Hess,G.D.[C] GARP-I-1 Gavrilova,L.A. MPR-II-5 Hesstvedt,E. UAPRC-12-5 Gaynor,J.E.[ci AS-IV-19 Hickey,B.M.FC] OW-III-6 Gelinas,R.J. UAPRC-LO-6 Hicks,B.B. AS-IV-2 Gentry,R.C.CC] US-VI-3 Hill,H.W. US-I-5 German,A.I.[C] UAPRC-2-3 Hilst,G.R. UAPRC-12-2 Gerstmann,W. US-V-4 Hind,A.D.[C] UAPRC-8-1 Gezentsvey,A.N.[C] PO-17 Hinwood,J.B. ED-4 Gibson,T.T. US-I-1 Hinwood,J.B.[C] ED-7 Gill,A.E. OW-III-18 Hirota,I. UA?RC-9-2 Gill,A.E. AS-1-5 Hitzfelder,S.J.[CJ CR-I-4 Gilchrist,A. AS-III-6 Holland,W. AS-III-12 Gilmer,R.O.[C] GARP-I-5 Hollinger,J.P. OW-I-14 Glazov,G.N. US-II-4 Honda,T.CCl OW-I-4 Godfrey,J.S. OW-III-8 Horton,B.H.[C] US-II-9 Goldberg,E.D.' FR-II-4 Horton,B.H.[C] US-VII-3 Goldman,A.[C] UAPRC-3-3 Howe,M.S.rc] ow-n-ir Goldman,A.TC] UAPRC-3-6 Hoy,R.D. CR-II-4 Goldstein,M.[C] US-VI-3 Hsu,E.Y.[C] AS-IV-20 Golitsyn,G.S.[C] SB-I-3 Hsuah,Y.LCl OW-III-11 Gonella,J. AS-II-4 Huddar,B.B. UAPRC-1-3 Gorelik,A.G. US-IV-7 Hud<3ar,B.B.[C] US-V-9 Graber,M. [C] UAPRC-2-2 Hunkins,K.L. OE-4 Grasni'jk,K.H. UAPRC-12-3 Hunt,B.G. UAPRC-10-2 Gras£>l,H. UAPRC-13-5 Hunt,B.G. UAPRC-11-1 Greaves,J.[CJ AS-1-2 Hupfer,P. AS-III-3 Gregory,J.B.[C] DAPRC-8-2 Hupfer,P. AS-IV-21 Gregory,J.B. UAPRC-8-3 Hurley,D.G. OW-II-7 Grijalva,N. PO-23 Grimshaw,R. OW-II-6 Gruza,G.V. US-II-1 1 Guterman,I.G. US-II-2 Ilyas,M.[C] US-II-9 Imberger,J. ED-6 Irish,J.IC1 OW-II-1 H Tshikawa,N.[C] MPR-I-9 Haberl,J.B. US-III-8 Ivanov,Yu.A.[C] OE-1 Hall,F,F. AS-IV-19 Ivanov,V.N. GARP-III-6 Hall,M. PO-27 Halikas.G. PO-11 I Halpern,D. AS-II-10 Hamilton,G.D.[C3 OW-III-9 Jaenicke,R. US-III-6 Hamilton,G.D. AS-II-6 Jarrige,F.LC] PO-4 Hamilton,P.[C] ED-2 Hamon,B.V. PO-43 Jayaweera,K.O.L. F. [C] MPR-II-8 Kuriyan,J.G. US-III-2 Jayaweera,K.O.L.F. CR-II-10 Kuznetsov,E.I.[C] PO-22 Jessen,W.[CD UAPRC-5-5 Johannessen,O. M. PO-26 Johnson,D.R. AS-III-14 Johnson,K.W. UAPRC-7-3 Laby,J.E. UAPRC-7-7 Johnson,K.W. UAPRC-10-4 Lacombe,H. FR-I-2 Jones,I.S.F. PO-28 Laconibe, H. AS-I-8 Jones,I.S.F. PO-29 LaevastUfT. OW-III-9 Jones,J.H. AS-1II-15 Laevastu,T.[C] AS-II-6 Joseph,C.P.[CJ UAPRC-1-3 Laevastu,!.[C] AS-IV-5 Joseph,C.P.[CJ US-V-9 Lajoie,F.A. US-VI-1, Junge,C. UAPRC-1-1 Lambert,G. US-I-6 Junge,C. FR-II-1 NA Larson,S. AS-IV-5 Lazrus,A.L.[C] UAPRC-2-1 Lecomte,P. [C] AS-I-1 K Leifer,R. UAPRC-1-5 Kagansky,A.S.[C J US-V-8 Levin,L.M.[C] DC-3 Kalachinsky,S.F.IC] US-IV-7 Lindzen,R.S.[C] UAPRC-14-1 Kalihinan,M.Ya.[C] UAPRC-7-5 Lleonart,G.I., OW-I-2 Kalihman,M.Ya.[Cl MPR-II-6 Lloyd,K.H. UAPRC-8-7 Kano,M.[C] UAPRC-7-8 Loewe,F. tiPR-I-1 Karabasheva,E. I. *• PO-21 Logvinov,K.T. UAPRC-7-6 Karimova,G.U.[C] MPR-II-4 London,J.[C] UAPRC-14-3 Karol,I.L. UAPRC-12-6 Longuet-Higgins ,M.£'.OW-I-3 Karol,I.L. UAPRC-13-1 Louis,J.-F. UAPRC-14-3 Kassner,J.L.[CJ US-III-8 Lovill,J.E. UAPRC-4-4 Kattawar,G.W.[C] CR-I-4 Lovill,J.E. CR-II-8 Kelkar,R.R.[C] CR-II-6 LowpC.H. UAPRC-8-1 Keller,J.L.[C] US-1-8 Lupini,R. PO-41 Kelly,G.A. GARP-IV-5 Lyubimtsev,M.K. [CJ PO-16 Kidson,J.W.[Cj UAPRC-9-6 Kidson,J.W. US-VI-8 Kilworth,P.C DC-18 M Kjelaas,A.G.[C] AS-IV-19 GARP-II-3 Klimova,E.I.[C] McAi'aney,B. J. US-I-7 McBean,G.A. AS-IV-6 Kollmeyer,R.C.[CJ ED-12 UAPRC-13-2 Kondo, J. MacCracken,M.C. AS-IV-13 McCue,R.[C] UAPRC-5-2 Koshelkov,Yu.P. LC] UAPRC-7-5 McEwan,A.D. OW-II-8 Koshelkov,Yu.P. UAPRC-9-4 McEwan,A.D. DC- 11 Koshlyakov,M.N.fC] OE-1 McGavin,R.E.[C] GARP-I-5 Kostko,O.K.[C] UAPRC-2-3 McIntyre,M.E. OW-II-il Kouznetzov,G.I. US-IV-2 McWilliams,J.C- OW-III-12 . Kraus,E.B. AS-II-2 Maier~Rein»er,E. PO-14 Kraus,E.B. AS-III-10 Malevd, v -M aladch,S^. AS-6 Kraus,E.B. GARP-I-6 Mailing ,3r,W.G.[C] US-VI-3 Kraus,H.[C] GARP-III-1 Manabe,S.CC] AS-III-5 Krauss,W. OW-II-9 Mangarella,P.A. AS-IV-20 Krekov,G.M.[CJ US-II-4 Mani,A.[Cj UAPRC-1-3 Krivilo,P.F.[C] US-V-8 Mani,A.fC] UAPRC-5-4 Krueger,A. J. UAPRC-6-2 Mani,A. US-IV-5 Kriigermeyer,L. GARP-I-3 Mani,A. Kruspe , G. AS-IV-18 Mani.A. CR-II-6 Kuettner,J. OE-6 NA Mani,A.[C] SB-I2-6 Kuettner,J. P. GAKP-III-1 Manins,P.C. Kulkarni,R.N. UAPRC-4-5 Manowitz,B.[Cl oc^ie Kulkarni,R.N. UAPRC-7-1 Manson,A-H. UAPRC-1-4 UAPRC-8-2

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Manson,A.H.rcj UAPRC-8-3 Novokrestchenova,A.S.[C]US-IV-7 Manton,M.J. DC-2 Noye,B.J. OW-III-13 Martell,E.A. UAPRC-2-6 Nysen,P.A.TCT PO-28 Martell,E.A. SB-I-6 Marunich,S.V.[C] SB-I-4 Mashkovi ch,S.A. GARP-II-4 o Mastenbrook,H.J. UAPRC-3-1 Oakey,N.S.[CJ PO-39 Mellor.G.L. PO-38 O'Brien,R.S.[C] US-VII-3 Menzhulin,G.V. SB-II-2 Ogawa,T.[C] UAPRC-12-4 Mestayer,P.[C] AS-IV-7 Ohkusu,M.fC] OW-I-4 Milford,S.N. ED-5 Ono,A.[C] UAPRC-1-6 Miller,M.J. DC-5 Ono,A.[Cl US-1II-1 Mintz,VT.CC] US-1-3 Ostapoff,F. AS-I-10 Mintz,Y.[C] 0W-1II-7 Osman,M.M. AS-III-17 Mishina.M.I. US-I-7 Ovcharenko,V.P. [CJ US-III-4 Mitsuta,Y. AS-IV-15 Ozmidov,R.V.[C] PO-16 Mitsuyasu,H. OW-I-4 Ozmidov,R.V. PO-17 Miyauchi,M.[C] UAPRC-7-8 Mizuno,S.[C] OW-I-4 Molinar,R.L. GARP-III-4 Moncrieff,M.W. DC-4 Pade,B.rC] PO-10 Monin,A.S.[C] PO-17 Paka,V.T.rC] PO-17 Monin,A.S.[C] AS-III-11 NA Paka,V.T.fC] PO-21 Mooers,C.N.K. OW-II-12 Palevich,L.G. [C] PO-22 Morelli,J. AS-II-7 Paltridge,G.W. CR-I-8 Morris,R.J. pq-34 Paltridgc,G.W.[CJ DC- 11 Morton,B. R. DC- 12 Panchev,S. US-VI-4 Moss.D.G.[C] UAPRC-3-5 Panin,G.f C] AS-IV-21 Miihleisen,R. AS-II-12 Panofsky,H.A. AS-IV-17 Munk.W.H.fC] OW-I-10 Paskausky,D.F. PO-7 Munk,W.[C] OW-II-5 Paskausky,D.F. ED-12 Munk,W.fCl OE-8 Paszynski,J. SB-II-3 Munkewitz,H.R.[C] UAPRC-1-4 Paterson,M.P. US-VII-8 Munn,R.E. FR-III-4 NA Patzert,W.C. AS-II-9 Murcray,D.G. UAPRC-3-3 Pearman,G.I. US-VII-6 Murcray,D.G. UAPRC-3-6 Pearman.G.I.fC] SB-I-2 Murcray,F.H.[C] UAPRC-3-3 Peri,G^[C] AS-IV-7 Murcray,F.H.[C] UAPRC-3-6 Peterson,J.T. US-VII-5 Murphy,D.L.[C] ED-12 Petrossiants,M.A. GARP-III-5 Myatch,L.T.[C] GARP-III-6 Petrossiants,M.A.[C] GARP-III-6 Mysak,L.A. OW-II-10 Petrov,L.S. [C] MPR-I-5 Mysak,L. A. OW-III-15 Phillips,N.A.[CJ UAPRC-11-2 Phillips,O.M.[C] OW-I-1 • N Phillpot,H.R. GARP-IV-6 AS-IV-10 Pisharoty,P.R. Nakamura,K.[ CJ OW-III-19 OE-11 NA Nakano,M. Pittock,A.B. UAPRC-6-1 Nalwalk.A.J.[C] ED-12 Pittock,A.B. OE-8 UAPRC-9-5 Namias,J. Plass,G.N. CR-I-4 Namias,J. 4 AS-III-1 Platt,C.M.R. UAPRC-9-3 CR-II-9 Nastrom,G.D.[C] Podz imek,J. US-III-7 Neal,A.B.£C] GARP-IV-6 Podzimek,J. FC] OE-3 US-III-8 Neal,V.T. Polian,G.[C] US-I-6 Needier,G.T. OW-III-2 Pollack,J.B. AS-IV-19 UAPRC-15-2 Neff ,W.D.[C] Pollard,R.T. OE-10 Neill,G.F.[C] UAPRC-3-5 Pollard,R.T. AS-II-11 AS-II-1 Neshyba,S.[C3 Pollock,T.J.[C] ED-4 Newell, R.E.[C] UAPRC-7-2 Popkov,A. US-II-4 Newell, R.E.[C] UAPRC-9-6 Portasov,V.S.[CJ UAPRC-2-3 Newell,R.E. FR-I-4 NA Price,P.G. US-I-4 Seaman,R.S.[C] GARP-II-5 Prinn,R.G.[Cj UAPRC-11-2 Sedunov,Y.S. US-IV-8 Prisenberg, S. [ C3 OW-II-1 Seiler,W. UAPRC-2-5 Pruchniewicz,P. G. UAPRC-5-5 Sekihara.K. UAPRC-7-8 Prumm,D AS-II-3 Selezneva,E.S.CC] US-III-5 NA Puri,K.K.N. GARP-II-2 Sen Gupta,R. PO-30 Pyle,J.A.[C] UAPRC-14-4 Shapiro,A.CC3 OW-I-12 Shapiro,A. OW-I-13 Sharaf El Din,Si.H.PO-25 Q Sharp,B.B. ED-10 Queck,H. CR-II-5 NA Sharp,D.B.[C] ED-10 Quiroz,R.S.[C] UAPRC-7-3 Shedlovsky,J.P.[C3UAPRC-2-1 Shimazaki,T. UAPRC-12-4 Shishkov, Yu.A. PO-19 IRV Simmons,A.J. UAPRC-10-1 Rabe,K.[C] AS-II-6 Simpson,R. W. AS-III-4 Rabus,D.[C] UAPRC-3-4 Sissons,N.V. US-VII-4 Radok,R. PO-8 (Smagorinsky,J. ) AS-III-5 Rahalkar,C.G. [Cl SB-II-6 Smith,W.L. GARP-IV-2 Rakipova,L. R. US-II-6 Solomon,H. PO-40 . Ramamonjiarisoa,A.[Cj AS-IV-7 Sonter,M.J. US-VI-5 Randhawa,J.S. US-VII-2 Soong,Y.S. OW-III-11 Rangarajan,S. - US-IV-1 Speranza,A.[C] PO-41 * Rangarajan,*" US-IV-6 Spencer,D. OE-12 Raschke,E. MPR-II-1 Spillane,K.T.[C] US-I-2 Raschke,E. CR-I-6 Sguires,P. CR-I-1 Rasmussier. ,H. ED-7 Sreedharan,C.R. UAPRC-5-4 Rattray,M. OW-II-1 Srinivasan, V.[Cj CR-II-6 Reid,R.O.[C3 ED-3 Stark,K.P. US-VI-2 Reid,R.O.[C] ED-13 Steedman,R.A. ED-16 Reiniger,R.F.[C] OW-III-4 Stefanov,S.R.[C] PO-36 Richards,J.M. DC- 13 Stewart,R.H. OW-I-10 Richter,K. OE-13 Stewart,R.W. FR-III-1 NA Rikiishi,K.C. OW-I-4 Stommel,H.M. FR-II-3 NA Robinson, A. R. OE-2 Stone,N.W.B.CC] UAPRC-3-5 Robinson,R.M.[C] OW-II-8 Strang,D.M. US-VI-6 Rokityan,V.E.[C] UAPRC-2- Street,R.L.CC3 AS-IV-20 Romanov,Yu.A. PO-19 Stubbs,T.J.[C] UAPRC-8-4 Roper,R.G. uAPRC-e-e Suberville,J.-L,. [C3OW-II-13 Rosen,J.A. UAPRC-1-I Suhara,T.[C] OW-I-4 Ross,D. PO-32 Sundararaman,N. [;C3UAPRC-4-6 '< Ross,J. SB-II-4 Sundararaman,N. SB-II-5 Rotschi,H.[Cj PO-4 Swann,N.R.[CD UAPRC-3-5 s T Saint-Guily,B. OW-III-16 Taft,B.A. OW-III-6 St. John,D.E.[C] SB-II-5 Takano,K. OW-III-7 Sanak,J.[CJ US-I-6 Takashima,T. US-IV-3 Sasamori,T. UAPRC-14-2 Tanaka,M.[C] CR-I-5 Schiff.H.I. UAPRC-4-1 NA Tang,C.L.[C3 OW-III-15 Schmidt,U.[C] UAPRC-2-5 Tang,W. US-V-7 Schmitz,W.[C] OE-2 Tarbeev,Y. GARP-III-2 Schneider,S. H. US-III-9 Tasai,F.[C3 ow-i-4 • Schooley,A.H. AS-I-4 Taylor,T.D.fC] UAPRC-12-1 : Schulze,R. UAPRC-6-4 Tennekes,H.£Cj AS-IV-17 Schuster,B.D. [ C3 UAPRC-2-1 Thompson,D.C. MPR-II-2 • Schwerdtfeger,P. SB-II-1 Thomson D.W.[CJ AS-IV-17 ;'

••'• '- '" . . '.1

> ; • *'\ Thomson,M.R. US-V-2 Webster,P.J.[C] SB-II-5 Thompson,N. AS-IV-16 Wegrzyn,J.E.[c] US-III-8 Thompson,R. OW-III-17 Wendler,G. MPR-I-9 Thompson,R. AS-IV-14 Wendler,G. MPR-II-8 Thompson,S.M. DC-9 Wendler,G.FCJ CR-II-10 Tiefenau,H.[C] UAPRC-5-5 Weston,K.J.[C] AS-IV-9 Tikhonov,A.P.[C] UAPRC-2-3 White,W.B. PO-3 Tiwari,V.S.[C] UAPRC-5-4 Whitehead,J.A. ED-8 Toba,Y. OW-I-5 Whitenaad,J.A. DC-19 Toba,Y. OE-9 Whittaker,R.E. ED-13 Toon,O.B.[C] UAPRC-15-2 Whitten,R.C. UAPRC-ll-5 Trenberth,K. E. AS-III-9 Widhopf,G.F. UAPRC-12-1 Trevison,A.[C] PO-41 Wilbrandt,P.[C] UAPRC-5-5 Trizna,D.B. OW-I-11 Williams,N.V. OW-III-20 Trokhan,A.M. PO-36 Williams,W.J.[C] UAPRC-3-3 Turco,R.P.[C] UAPRC-ll-5 Williams,W.J.IC] UAPRC-3-6 Turikov,U.G.£C J AS-III-11 NA Wood,I.R. ED-9 Turner,J.S.[C] OW-I-3 Woods,J.D. PO-9 Turner,J.S. DC- 8 Woolf,H.M.[C] GARP-IV-2 Twomey,S. CR-I-2 Wooster,W. S. AS-III-8 Woronko,S.F. UAPRC-15-1 Worthem,S.[c] AS-I-10 u Wright,J.W. OW-I-7 Uliana,E.A. OW-I-12 Wucknitz,J.TC] GARP-I-3 Unthank,E.L.[C] UAPRC-7-7 Wunsch,C.[C] OW-III-6 Wyrtki,K. OW-III-1

Valenzuela,G.R. PO-33 Vanhoutte,J.C.[C] AS-I-1 Yamada,S.[C] OW-III-19 Vastano,A.C.[CJ P0-11 Yamamoto,G. CR-I-5 Vastano,A.C.[C] ED-13 Yao,N. AS-II-11 Venka te swaren,S.V. [C3SB-II-5 Yaplee,B.S.[C] OW-I-12 Vijayakumar/R.[C] US-IV-1 Yaplee,B.S.[C ] OW-I-13 Villmann,Ch.J. US-II-7 Young,M.B.O.[C] AS-IV-20 Vincent,R.A.[C] UAPRC-8-4 Young,S.A. fC 1 CR-II-7 1 Vonder Haar,T. •/^nv,:-,.A. FC •.";-: 7 :-•; Vonder Haar,T.H. • GAM— II I- 3 Vuuir. , 'I. I . Voskresensky,A.l. MPR-II-3 Vorobjev,V.P. PO-22 Vreugdenhil,C.B. ED-1 z Vulfson,N.I. DC- 3 Zaichikov,B.P.\Z ] UAPRC-7-5 Vupputuri,R.K.R. UAPRC-11-3 Zaichikov,B.P.tc] MPR-II-6 Vupputuri,R.K.R. UAPRC-11-4 Zakharova,I.M. [~c] US-IV-8 Zakharov,V.M. UAPRC-2-3 Zerefos,C.S. US-II-5 w Zhmur,V.V. [Cl PO-20 Walczewski,J. US-II-3 Zilitinkevich,S.S. AS-III-11 NA Walton,J.J. UAPRC-11-6 Zillman,J.W. US-VI-7 ! Wark,D.Q. UAPRC-4-2 Zillman,J.W. AS-II-5 Wark,D.Q. GARP-IV-1 Zore-Armanda,M. AS-III-13 Warren,B.A. OW-III-3 Zuev, V.5.[c: US-II-4 Way.-.e.S.P. Z--sv,V.£. Webb .Z.T.. Weia-E.-r. \1— 2 '/-11 Webster,?.J. -APHC-4-0 Webster,P.J. US-I-3 Webster,P.J. US-I-8 UAPRC-l-1 SULFUR BUDGET OF THE STRATOSPHERIC AEROSOL LAYER UAPRC-1 C. Junge

Max-Planck-Institut fur Chemie (Otto-Hahn-lnstitut), Mainz, Federal Republic of Germany

Particles of the stratospheric aerosol layer consist to

a large degree of sulfate. On the basis of material budget con-

siderations It was concluded soon after detection of the layer

that upward transport Into the stratosphere of gaseous sulfur

constituents must be Involved which in turn are converted into

partfculate matter by oxidation. These particles are subsequently

removed again from the stratosphere by mixing and sedimentation

so that the sulfur budget of the stratosphere is balanced.

It is clear that any explanation of the formation and

preservation of the aerosol layer must take the stratospheric

,-t sulfur budget Into account whatever the details of the chemistry

Involved may be. In this paper the concept of gas diffusion is

tested by model calculations on the basis of the presently available

knowledge. It is demonstrated that this concept can simulate the

basic features of the aerosol layer fairly well if the oxidation rates

of the gaseous sulfur constituent, as for instance sulfur dioxide, -9 are sufficiently low, I.e. of the order of 10 sec. This result,

obtained exclusively by meteorological considerations and obser-

vations, is compared with laboratory measurements of reaction

rates. Some interesting conclusions can be drawn from these

considerations. UAPRC-l-2 THE PRESENT WORLDWIDE DISTRIBUTION OF STRATOSPHERE AEROSOLS

J. A. Rosen

University of Wyoming, Laramie, Wyoming, U.S.A.

The University of Wyoming under contract to DOT and

ONR has conducted a series of balloon soundings on a globai scale

to establish the present levels and trends of high-altitude aerosols. ,

The measurements were made as much as possible on a quasi

synoptic basis. The results have been reduced to diagrams showing

mixing ratio isopleths in the stratosphere. These diagrams suggest

the source and sink regions of high-altitude aerosols. j.;

; :*,: v.-'

-.: •..••• • t." •<•:

It' '•-• > UAPRC-l-3 THE STUDY OF THE ELECTRICAL CONDUCTIVITY OF AIR IN THE LOWER STRATOSPHERE AT POONA

B. B. Huddar, C. P. Joseph and A. Man!

India Meteorological Department, Poona and New Delhi, India

Regular soundings to measure the electrical conductivity of the air over Poona have been made since 1969, using balloon borne conductivity sondes developed and constructed in the Instrument Research Laboratories of the Meteorological Office at Poona.

The earlier soundings had shown a sharp decrease in conductivity above 19 km and this had been attributed to the presence of stratospheric dust at this height. Associated increases in electrical potential gradient had been also observed.

The present systematic soundings show that the variation of conductivity with height agrees with theoretical values in summer, but during the winter months it shows a sharp fall after about 18 km. The main cause for the observed variations in conductivity would appear to be the changes in aerosol content in the lower stratosphere caused by changes in the circulation patterns in the lower stratosphere. I I

">•* t-

J ^ £ J/-M'.'., I '•> ISOTOPE AND CONCENTRATION MEASUREMENTS OF STRATOSPHERIC SUL.FATE*

A. W. Castleman, Jr., H. R. Munkelwitz, B. Manowltz

Brookhaven National Laboratory, Upton, N. Y. , U.S.A.

An investigation of the trends In concentration and S "/S isotopic ratio of the sulfur component of stratospheric aerosols has been made in order to assess the significance of various possible sources, as we'! as establish the contribution from In situ gas-to- particle reactions. Concentration and Isotopic values were found to undergo regular cyclic changes following a few/ major explosive volcanic eruptions. However, after the volcanic-Induced pertur- 34 bations subsided, the S enrichment of stratospheric aerosols collected in both Hemispheres returned to a value of about 2. 6 /oo. These results show that the major perturbations to the low-level persistent aerosol layer result from a few explosive volcanic eruptions. Trends In S" enrichment of aerosols sampled at progressively later times following an eruption provide clear evidence thai the particles are continuously replenished by gas-to- particle reactions of the SO. initially Injected by the eruption cloud." The observed trends are consistent with a simple one-dimensional .... model which accounts for both transport and chemical reaction. The data suggest that, during periods of comparative volcanic quiesence, •' \ the primary input to the layer comes from a common equatorial spuHce, lj

*This work was performed under the auspices of the U.S. Atomic Energy Commission and was supported by the Environmental Protection Agency under an interagency agreement. r.

«'% \' » • UAPRC-l-5 THE MECHANISM OF FORMATION OF STRATOSPHERIC AEROSOLS

- < i'

+ <^J Robert Leifer

I New York University, New York, U.S.A.

j ( A model for the formation of stratospheric aerosols has been

1 , developed using laboratory data. Trace quantities of SOO, NH , O , £i 3 3 J - and H_O were irradiated for various periods of time and in different ' wavelength Intervals. Results of these experiments provided the | f' foil owing-Information: £;.'*'". - 1. The quantum yield of the homogeneous oxidation of SO, by f':-i'S- • • ' -10 I >; ..«» - O- Jn the first strong band is less than 1.0x10 ;•.'':>ri' 2. Formation and stability of acid embryos are highly dependent »;;", on the available water vapor concentration. j;.;*' 3« ' Experimental data for a H-SO^-H-O system Indicates that fjiV' concepts of equilibrium thermodynamics do not provide 1;^* "* ' realistic estimates of heteromolecular nucleation rates. V'T 4. SO, and NH_ dark reactions do not play a significant role p,*» In the formation of stratospheric aerosols. !.}'-*' Si. Trace orfianic materials may play a role in the formation of f ,j , . ' " condensation nuclei when radiation of wavelengths below ft* ...,,' • ' 2200A Is present. The chemical mechanism for the formation of stratospheric -If. aerosols as proposed previously by Friend and his co-workers has been j^ modified to include experimental data showing that coagulation of sulfuric *» acid embryos to some critical size is necessary before rapid growth by •ft* ' ,4, heteromolecular oxidation can occur. UAPRC-l-6 SIZE DISTRIBUTION AND NATURE OF STRATOSPHERIC AEROSOLS

E. K. Bigg and A. Ono

Division of Cloud Physics, CSIRO, Sydney, Australia

From 1968 to the present time particles have been collected from the stratosphere by a high velocity impactlon system carried on balloons. They are captured directly on to nitre-cellulose membranes coated with a thin layer of carbon or copper mounted on electron- microscope screens. The screens are arranged In a circle and rotate slowly beneatb. the impactor's nozzle after the equipment is first turned on at about 10 km, thus giving a continuous record as the altitude increases.

Chemical information Is obtained by reaction of the particles with thin films of reagents In the presence of suitable solvent vapours, as described by Bigg, Ono and Williams (1973).

A high proportion of the total number of particles consists largely of sulphuric acid with varying amounts of ammonium sulphate. However, reactions with barium chloride are slightly different from those with sulphuric acid or ammonium sulphate particles produced in the laboratory, and these differences may be due to additives not yet detected. Nitrate and chloride tests have not yet gfven positive results with stratospheric particles but some persulphate has been detected, using benzidine as a reagent in ethanol vapour, from particles collected near the base of the stratosphere.

The vertical dimensions of the particles are obtained by shadowing half of each electron-microscope screen with gold-palladium at an angle of tan 0. 5 with gold-palladium evaporated from a hot wire in a vacuum. Many particles are semi-liquid and flatten on impact. The assumption used for calculating volumes Fs that they form spherical caps whose height is given by shadow length. When ; no shadow is visible it is assumed that the particles have the maximum height that can occur for this condition. Particles with circular rings of satellite droplets are very common and pose a special problem. Fortunately many leave impact craters on carbon substrates allowing

••-:\ . f the diameter of the impacting sphere to be estimated. When this is not visible the equivalent sphere is estimated from comparison of t the diameter of the droplet ring with those of particles showing impact craters.

With these procedures all particles are converted to "equivalent spheres" and size distributions are formed such as those shown below (from a flight over Wyoming, U. S. A. on *21 March 1972).

(••••

':>?'

A. A A 001 003 0-1 0-3 1 3 31 0 6 0 6 ' CONCENTRATION OF FaRTlCLES WITH DIAMETERS »(! lcm"3 DIAMETER IM) S?ze distribution of particles Typical size distribution with altitude on one flight. of particles near 18 km altitude.

Particles are predominantly small, with modal diameters near 0. 1 urn. Those with diameters above 0. 5 um are more highly stratified and occur mainly between about 12 and 25 km.

Reference BJgg, E.K., Ono, A. and Williams, J. A., 1973. "Chemical tests for Individual submicron aerosol particles", Atmospheric Environment (in press). jl- , • UAPRC-2-1 \ RECENT STUDIES OF THE STRATOSPHERIC AEROSOL LAYER

UAPRC-2 R. D. Cadle, E.F. Danielsen, A. L. Lazrus, B. D. Schuster and J. P. Shedlovsky

The National Center for Atmospheric Research, Boulder, Colorado, U.S.A.

During the last few years, the National Center for Atmospheric Research (NCAR) has been investigating the composition, concentration, variation with season and location, and • meteorology of the stratospheric "aerosol layer". The present -v . c. contribution deals with our more recent, unpublished, findings. ' Junge and his co-workers, In the late 1950's and early 1960's, determined the concentrations of particles in the stratospheric aerosol layer by means of impactors. During recent years, determinations of the concentrations in that layer have been made by filters and indicated concentrations as much as sixty times those 1 obtained earlier. We have simultaneously flown both filters and » Impactors on WB 57F aircraft. Our initial, published results, although not conclusive, Indicated that the Impactors had, at most, about 20% of the collection efficiency of the filters for the stratospheric particles. We have now made more flights that confirmed these results with regard to total sulfate, but also suggest that the Impactors and filters collect ammonium sulfate, a minor constituent of the aerosol, with about equal efficiency.

•!* We have been determining the relationships between laser radar (lidar) signals and the concentrations of particles in the stratospheric aerosol layer determined by two techniques. Very good correlations have been found. Lidar equipment mounted in an aircraft has been flown from the equator to 85 N on one occasion. The results suggest a strong enhancement of the stratospheric aerosol layer in the north polar regions, possibly the result of *- Injections of particulate material from the recent eruption in Iceland. Flights on the 60th and 40th parallels also show this northern latitude enhancement.

Samples collected on filters flown on WB 57F aircraft have been analyzed for sulfate, ammonium, calcium, magnesium, sodium, chloride and bromide which are in paniculate form, and nitric acid vapor which is absorbed by the filters. The aircraft flights extend from 75 N to 51 S, and are flqwn four times annually at four to six altitudes between the tropopause and at about 65, 000 ft. Filter samples are also being collected by means of balloon fifghts at altitudes of 70, 80, and 90 thousand feet. The mixing ratios of all of the substances studied so far have had distributions that tend to parallel the tropopause height. These distributions are, thus, similar to isentroptc surfaces In the strosphere.

In order to understand the distribution of trace constituents in the stratosphere, it is necessary to understand the transport and diffusion processes involved. By means of the combined WB 57F data, data obtained with the NCAR Saberliner, and isentrop/c trajectories, and a meridional-vertical transport and diffusion model, we are attempting to describe the diffusion in the lower stratosphere from the small-scale gravity waves to tKe large-scale eddies. UAPRC-2-2 STRATOSPHERIC AEROSOL LIDAR MEASUREMENTS OVER JERUSALEM

A. Cohen and M. Graber

Department of Atmospheric Sciences, The Hebrew University of Jerusalem, Israel

The laser radar system, consisting of a ruby laser as the emitter, has been used used to map the aerosol layer centered at 20 km. Scattering measurements were made in two polarizations and changes as a function of time in the number density were detected.

The size distribution variations were observed by the analysis of the depolarization of the backscattered light.

The results were compared to those obtained in different sites over the whole globe and the height of the maximum concentrations vs. latitude and season were plotted.

Regular measurements of the stratospheric aerosol profile are being carried out in order to detect future concentration variations due to volcanic eruptions or other possible dust sources. The profile describes the altitude dependence of the aerosol concentrations between 1*0 - 30 km, by use of a multichannel analyzer.

rf*J

• 1- ?J UAPRC-2-3 THE DETERMINATION OF TROPOSPHERIC AND LOWER MESOSPHERIC DENSITY, TEMPERATURE AND AEROSOL PROFILE BY A METHOD OF TWO-FREQUENCY LASER SOUNDING

V. M. Zakharov, O.K. Kostko, V. S. Portasov, A.I. German, V.E. Rokltyan, E.A. Chayanova and A. P. Tlkhonov

U. S.S. R.

In the experiments a laser radar with the following parameters was used: ruby laser transmitter generating at 0. 6943 urn; neodymium laser transmitter generating at I. 06 um; both with a single * pulse energy of 0. 7 J and pulse-length of 25 ns. The receiving ,, antenna diameter was 0. 5 m, the viewing angle -1.5 mrad, and the interference filter half-width - 20 A; recording was carried out in the mode of a single""photon count.

To determine atmospheric transparency along the path up to the observed volume, the horizontal layer was viewed at different angles. Assuming horizontal atmospheric homogeneity it Is possible to determine an exponential attenuation term in the equation of laser location.

As far as the adequacy of the most frequently used apparatus, calibration by a scattering volume at about 30 km (so that Rayleigh scattering is assumed) may be considered doubtful, the following experiments were conducted. The total scattering coefficient profile for a ruby laser was determined in the processof calibration by the Rayleigh scattering at 30 km, as well as through laboratory calibration. j

The experiments indicated that within the limits of measurement errors both profiles practically coincide proving the fact lhat during our soundings (the Crimea, Autumn, 1972) atmospheric contamination at 30 km was negligible.

In a great number of experiments an increase of scattering ': was observed in the tropopause region and the zone of macreous clouds. { The data obtained agrees very well with other authors' results. Maximum ; Increase of a backscattered signal was observed at 20-22 km, for which * the ratio of total backscatterirjg to the Rayleigh backscatterfng was about 2. 2-2. 4. In some experiments secondary maxima were detected at «„ about 24 km. T- i f

£.A- *., •: Sounding at 1. 06 um was possible only up to 13 km, ;,i'v "> because of the low photomultfplier quantum efficiency. Assuming ' I C((i ' that backscattering Indicatrixes at 0. 7 um and 1. 06 pm for slight ' |* -,i= ' atmospheric turbidity are identical, we can discriminate between I C ' the signals for total and molecular scattering. Also made were '»'.'. •- the corresponding calculations which will be published in the future. ' i '• < It proved possible to estimate density profiles and atmospheric ] , . temperatures using two-frequency sounding data and to compare the i \:y»j .results ,w'*h radio-sounding data. The data obtained agree satis- ;, i:\ .factorlly with the results of measurements made by means of radiosondes.

1 •'•.-.• •

\:/ ' . UAPRC-2-4 ON THE INFLUENCE OF AIR-SEA INTERACTION ON THE DIFFUSION AND REMOVAL. OF AIRBORNE PARTICULATE MATTER

C. Garbalewski - i Maritime Department of Institute for Meteorology and Water Economy, Gdynia, Poland * -t ''»

The physical sea-salt nuclei characteristics greatly depending on aii—sea Interaction were measured in the period of 1970-1972 over the Baltic Sea, Particle size distribution and short term fluctuations'' ». of nuclei concentration were the basis of two different methods applied in the investigation of the physical sense of Index X in the distribution ^ law: n(h) 'v /f/.*3* • It 's shown, that X f°r sea-salt nuclei defines 'J«J in principle the ratio of nuclei "emigration" to "imtgration" processes' determined - the first by atmosphere self-cleaning and the second by

aerosol production and diffusion Intensity. Therefore X

where ^- particle concentration, 5^,- sea water salinity, . Jk dimensionless wind speed parameter determining the nuclei production ''•? rate and their diffusion intensity, -A self-cleaning constant for the, near sea surface air layer. Approximately the same values X found *-, from nuclei distribution analysis and from the investigation of hf/of' < \'' \ fluctuation versus time f confirms the theoretical assumption. In the ir V- first case the value X for oceanic and Baltic nuclei restricts 3, 17 «*''•••"'• . ..•' fM) and 3, 77 and in the second to 3, 06 and 3, 96 respectively. ^AcJcordlhgly^s to the found va.lues the mean residence time of aerosol at air-sea ' • sv •<: interface is 7" = 31 hours under local air circulation over the Baltic a i . and "?" = 25 hours under its advectlon from the Atlantic. 'V

H '•> •"•• j • X4 NEW ASPECTS ON THE ATMOSPHERIC CO- AND H.-CYCLES

i , W, Seiler and U. Schmidt

!', Max-Planck-instftut fur Chemie (Otto-Hahn-lnstitut), ^? Mainz, Federal Republ fc of Germany if,•;-.;•;•.• Since the detection of CO in the atmosphere in 1952 several

j ,;". Ideas about the CO-cycle In the atmosphere were published. In the

i'vv3 pearly sixties CO was thought to be produced only by man. At the

;/ i v present time it is assumed by several authors on the basis of isotoplc

f%- V' CO-data that CO Is mostly produced by natural processes, especially r.,'.;;:' >.. | ':"; C - by the photochemical reaction between CH. and OH. f:.;-X- h • ^i-;jty '•" In thjs paper the already published ideas about the CO-cycle

I *).: w'" De critically reviewed. New data about the latitudinal and hori- fl;} zontal dfstrFbution In the troposphere and lower stratosphere In both

\::?.i'£ hemispheres, data about the dissolved CO in seawater and rainwater By' '

!•• * •- • "

,*; 5.; ' . as well as field- and laboratory-experiments with marine and terre-

:'*~g ,. strlal micro-organisms will be used to present a more detailed jliJ/"' Information on the budget and cycle of carbon monoxide in the atmosphere.

%" ^Essential points such as the ratio of natural to anthropogenic CO- v> «•• . • •" - .;.; production in the troposphere, photochemical reactions in the lower .,i; ,, stratosphere involved In the CO-cycle and the latitudinal CO-distribution "V,v. V, ...

••'"'* between the hemispheres are discussed In detail.

'" New data about the H_-distrlbution in the troposphere and

«*'- the lower stratosphere are discussed. One of the most important

£'„ results Is the higher H2-mJxing ratio in the northern hemisphere.

:Tf> From budget considerations based on these data the anthropogenic

/• H_-productfon appears to be about 50% of the total H -production in sjy" the troposphere. Therefore, H seems to be a "pollutant" Jn the ?r.h' . * Qjj/f Jiatmosphene In contrast to former suggestions. UAPRC-2-6 HYDROGEN AND CARBON COMPOUNDS IN THE UPPER STRATOSPHERE AND LOWER MESOSPHERE

E. A. Martell

National Center for Atmospheric Research, Boulder, Colorado, U.S.A.

Large representative high altitude air samples were

collected using a rocketborne cryogenic air sampler, recovered

by parachute and transferred into stainless vessels for subsequent

laboratory analy ;is of minor constituents. Two successful rocket

sampling missions were carried out over White Sands, New Mexico,

~ 31°N: NASA Aerobee 4. 130 UA, September 4, 1968 and NASA

Aerobee 4. 235 0A, May 23, 1973.

In the 1968 sampling flight, liquid hydrogen was used as

cryogen and 9. 73 moles of air were collected between 44 and 62 km

altitude Results for hydrogen and carbon compounds, summarized

and discussed elsewhere (J) in volume parts per million, are:

+ CH«, , 0.25 - 0. 02; CO 2 , 308 - 3; and H2 , 0. 40 S 'So • The

water vapor mixing ratio was estimated to be -.2. 5x10 6 at the

stratopause and will reach a maximum of ~ 3. 0 x 1 0 6 in the lower

mesosphere if H2 and CH,, are completely oxidized.

The May 1973 flight utilized liquid neon as cryogen and

improved bakeout and transfer techniques. An 11.3 mole air sample

was recovered in the upper stratosphere between 40 and 50 km

altitude. Constituents in process of measurement include H 2 O,

H2 , CHk , CO2 , CO andN2O. These new results will be

presented together with a brief summary and discussion of the

vertical distribution of these gaseous constituents in the stratosphere

and lower mesosphere.

(1) E. A. Martell, "The Distribution of Minor Constituents in the Stratosphere and Lower Mesosphere", in Physics and Chemistry of Upper Atmospheres, B.M. McCormac, ed. , D. Reidel Publ. Co., Dordrecht-Holland, 1973. UAPRC-3-1

STRATOSPHERIC WATER VAPOR DISTRIBUTION AND VARIABILITY UAPRC-3

H. J. Mastenbrook

Naval Research Laboratory, Washington, D. C. , U.S.A.

A series of observations of the vertical distribution of

water vapor which began in 1964 now provides 10 years of data

for the study of water vapor distribution and variability in the

lower stratosphere. This data Is compared with other water

vapor measurements over the last decade. The recent observations

show that the trend of water vapor increased from 2 ppm to 3 ppm

mass mixing ratio which was observed in the first 6 years of data

does not continue beyond 1970. Factors which might account for

the 6 year trend of increase are considered.

. *3> UAPRC-3-2 ROCKET MEASUREMENTS OF WATER VAPOUR IN THE STRATOSPHERE

W. F. J. Evans

Atmospheric Environment Service, Toronto, Canada

A radiometer designed to measure water vapour by

long path length solar absorption was flown on a Black Brant V

rocket at the Churchill Research Range on May 16, 1973. The

integrated absorption in the 2. I/A. water vapour band was measured

as a function of altitude during the ascent leg of the flight when the

solar depression angle was 3 degrees. Preliminary analysis of

the absorption data has yielded a profile for the mixing ratio of

water vapour over the altitude range 20 to 35 km. These results

are compared with profiles predicted by photochemical models. UAPRC-3-3

DISTRIBUTION OF HNO AND HO IN THE STRATOSPHERE AS DETERMINED FROM ATMOSPHERIC EMISSION SPECTRA OBTAINED WITH BALLOON BORNE INSTRUMENTATION

David G. Murcray, Aaron Goldman, Frank H. Murcray, Walter J. W Iliams, James N. Brooks and D. Boyd Barkis

Denver Research Institute, University of Denver, Denver, Colorado, U.S.A.

A bailoon borne spectrometer system capable of measuring the absolute intensity and spectral distribution of the radiation emitted by the earth's atmosphere as a function of altitude has been flown on a number of occasions. For a number of these flights the instrumentation was set up to operate in the 10 pm to 12 urn wavelength region. At these wavelengths the major source of atmospheric emission at the altitudes between TO km and 30 km is HNO By noting the change in emission 3" with altitude and knowing the temperature versus altitude, it is possible to derive the HNO mixing ratio versus altitude profile from the emission data. Analysis of this sort have been performed on the data obtained during a number of flights. These data indicate that the HNO_ occurs in a layer with the peak mixing ratio occurring around 20 km. The mixing ratio is variable, however, enough daia have not been obtained to determine whether the variability is seasonal.

Several flights have also been made with the spectrometer set to scan the wavelength region from 17 um to 30 pm. The atmospheric co nd emission in this wavelength region is due to NO, HNO., 9 a HO.

Beyond 24pm the emission is due almost entirely to HOO rotational lines. Since the measurements are absolute, it is ag"ain possible to determine the water vapor mixing ratio profile from the data obtained with the instrument and the temperature versus altitude data obtained with concurrent radiosondes. The ^~>9O mixing ratio profiles obtained with the instrument on flights made from Holloman AFB, New Mexico show the typicalrginimum mixing ratio above the tropopause (mixing ratio ~ I, 0 x 10" g/g) with an indication of a layer close to 25 km r with a T x>\g - = of 5. 10 g/g. The m'x'n^ "atio 300 - e 1Z •"-. as oe:»-~ - = - -- the date i be g ien e 1>"~ tec r ques in detail. UAPRC-3-4 STRATOSPHERIC WATER VAPOUR AND METHANE PROFILES

P. Burkert, D. Rabus, and H.-J. Bolle

Meteorological Institute, University of Munich, Federal Republic of Germany

Concentration versus height profiles of stratospheric

water vapour and methane were obtained from balloon flight measure-

ments with an occultatlon technique. The instruments used were

two-channel interference filter radiometers operating in the 2. 7^

water vapour and 3. 3 ^«^methane absorption bands respectively.

These instruments were pointed against the sun with an accuracy

of 2 arc minutes. Typical values of water vapour concentration

are 1. 5 ppm at 16 km, and 9. 5 ppm at 30 km, values for methane

are 1. 4 ppm at 17 km and less than 0. 1 ppm above 26 km. The

accuracy of these numbers were estimated to be better than - 20%. I • •••;*; UAPRC-3-5 SUBMIL-LIMETRE WAVE OBSERVATIONS OF STRATOSPHERIC COMPOSITION

J. E. Harries, N. W. B. Stone, J. R. Birch, M. J. Bangham, N. R. Swann and G. F. Neill,

('• •••'

Division of Electrical Science

and

J.W. Fleming and D. G. Moss,

Division of Materials Applications

National Physical Laboratory Teddington, Middlesex, U.K.

As part of the United Kingdom research programme into the meteorological effects of stratospheric aircraft our group at the NPL has been engaged in observations of several minor constituents in the stratosphere.

The technique we are using is to measure the infrared emission from certain gases, at submill imetre wavelengths, where characteristic pure rotation line spectra occur. By monitoring emission rather than solar absorption we are free.Jo make measurements at all times of day or night at will. The submil I irnetrt' region has until recently, however, been relatively unexplored, and to make meaningful quantitative atmospheric measurements it has been essential to do a considerable amount of background study on the detailed pure rotation spectra of all the species of interest.

Our instrument i£ a high resolution Michelson interferometric spectrometer, capable of a resolution of 0, 03 cm over the range 10cm~ to 50 cm" . In this rangranqe H_OH-O,. O_, O_, HNO_, N^O and '2' 3' 3' NO, emissions can be identified.

The data which we have available at the time of writing (June 1973) have all been obtained from the U.K. prototype Concorde 002, while flying in various parts of the world. Measurements made in the Far East and Australia have already been reported, but more recent measurements over South Africa and over the Arctic are currently being processed, and will be communicated at the Conference. Latitude and day/night variations will be main study topic in these measurements.

Whereas our previous work has been aimed solely at deriving column densities, we anticipate that the more recent data may provide information on vertical mixing ratio distributions, as a result of the use of a stabilised infrared receiving system which can scan the horizon in elevation.

Further work is currently being organised aimed at high altitude balloon flights of our equipment. This experiment should be launched In the spring of 1974, but other balloon experiments, involving lower resolution interferometers, and radiometers, capable of measuring H_O, O_, and O , should have been launched before the Conference. UAPRC-3-6 VERTICAL DISTRIBUTION OF MINOR ATMOSPHERIC CONSTITUENTS AS DERIVED FROM BALLOON-BORNE MEASUREMENTS OF ATMOSPHERIC INFRARED SPECTRA

D. G. Murcray, A. Goldman, F. H. Murcray, D. B. Barker, J. N. Brooks and W. J. Williams

Physics Department, University of Denver, Denver, Colorado, U.S.A.

|7 ;. Mixing ratio versus altitude profiles of minor- atmospheric

| ' constituents have been derived from balloon-borne infrared

t r spectroscoplc measurements. The observational data were

i' obtained during balloon flights made with a solar spectrometer,

Si, " a spectral radiometer and a filter radiometer. The spectrometer "i * is used to measure atmospheric absorption using the sun as a source and the radiometers have been used to measure the atmospheric

emission at various altitudes. Spectral resolution is about 0. 3 cm

in the absorption studies and about 2 cm in the emission studies.

Vertical distributions have been determined for HO, NO, CO and UAPRC-4-2 MESO-SCALE VARIATIONS IN ATMOSPHERIC WATER VAPOR IN TROPICAL REGIONS DEDUCED FROM VTPR MEASUREMENTS

D. Q. Wark

National Oceanic and Atmospheric Administration, National Environmental Satel I ite Service, Washington, D. C. , U.S.A.

The Vertical Temperature Profile Radiometer (VTPR) on the NOAA-2 satellite measures the earth's radiance at 19 , where emission by the atmosphere arises from water vapor. In low-latitude regions the mean level from which the emitted radiation comes is between about 850 mb and 600 mb for very dry and very moist atmospheres respectively. Measurements in the Tropics are combined with other VTPR measurements to deduce the total precipi table water in areas 55 km x 55 km and 500 km x 600 km. Beyond the natural tendency to underestimate water vapor over areas partly filled by clouds, it is shown that in both resolution scales there is a large variability in water vapor content of otherwise similar areas. This is particularly true in totally clear areas, where total precipitable water may vary from less than 1. 0 cm up to 5. 0 cm. Examples are shown of regional water vapor distributions under different cloud conditions, particularly low clouds of stratiform and of strong convective configurations. A method of compensating for the unobserved portion of the atmosphere within and below clouds employs estimates of the heights and amounts of clouds and the variabilities of the cloud amounts. Water vapor measurements from these satellite data may be more useful than temperature profiles deduced from VTPR data at very low latitude. • 4 OZONE RESEARCH - PRESENT AND FUTURE

I UAPRC-4 :i H. U. Dutsch Laboratory for Atmospheric Physics, Zurich, Switzerland

It is the rapid development during the past ten years of an ; increasingly complex photochemistry in the stratosphere grouped J.\ around ozone as a central substance which provoked renewed strong | ' interest of different groups of atmospheric physicists in the triatomic JT" oxygen modification. There are presently three groups of chemically f,••• active trace substances known to be in close interrelation with odd f; oxygen (and with each other), namely odd hydrogen (H, OH, HO ),

t:: odd nitrogen (also called NO ; NO and NO.) and carbon compounds belonging to the oxydation chain originating from CH.. While the first two groups evidently contribute to odd oxygen destruction the third has been claimed to possibly reproduce such particles. As known for some time there is also an interaction with sulphur compounds which are at stratospheric levels oxidized to sulphates. For i,'•,:'<. the odd oxygen budget they are apparently of less importance because • no catalytic cycle seems to be involved in this process.

(;-;:.-. While odd oxygen is formed in the stratosphere by direct !.;• photochemical action from a permanent (fully mixed) atmospheric >•>•' constituent the members of the other three groups are produced from i'i relatively stable compounds (H-O, N«O, CH ) of variable concentration, ;? originating at the ground (two of them as product of biological processes), U which are transported upward into the stratosphere where NO and *' ^^A have a sink. Except in the upper stratosphere where a con- p" siderable part of odd hydrogen is formed by direct photodissociation IX of water vapour the active substances are produced by action of [; excited O-atoms, or also by derivatives of such processes (CH + OH). •o.-. These excited O-atoms are photodissociation products of ozone which t> is thus the dominating substance of the system.

I'. ? Undoubtedly the ozone problem has been strongly complicated by the described development; the number of pertinent reactions has been increased from four in the classical theory to over 50, whereby for many of them the reaction (or dissociation) rates are very poorly known. In addition to ozone a number of other trace constituents belonging to this photochemical system have long relaxation times and are thus effectively redistributed by the general circulation. On the other hand the whole trace constituent chemistry of the stratosphere is now merging into one integrated system and if a number of other substances can be effectively measured a much better check on the theory will become possible by comparing its results with the observations than it was the case up to now.

The interrelation of the ozone photochemistry with a large number of trace substances also means that the ozone layer may be altered by human interference. The possibility of its reduction by the exhaust of a future SST-fleet is therefore being intensively studied at present which has lead to rapid progress in the field; a complete solution of the question will, however, undoubtedly need many more years.

The complex interaction problem between photochemistry and transport processes concerning various substances can hardly be solved otherwise than by insertion of the photochemical equations into numerical (three-dimensional) general circulation models; however, studies with two-dimensional models may nevertheless be very useful in experimenting with the photochemistry.

Although theoretical studies dominate the ozone research at present, care must be taken in order to guarantee comparable progress on the observational side. Not only is it important that the concentration and distribution of as many as possible of the minor trace substances are measured, also the observational program with respect to ozone itself must be further intensified in order to provide a more reliable picture of the three-dimensional distribution of ozone and its change with season and (last but not least) of yeai—to-year differences. So far an interesting correlation is indicated between the quasi biennial variation of the tropical stratospheric circulation' and the ozone content in the maximum layer over mid-latitudes in the winter-spring season.

The observational knowledge is strongly needed for. testing ; the results to be obtained by modelling and it will also be of importance in connection with the coming problem to be tackled in the field of ozone ; research, namely the study of the feedback system ozone (photochemistry and radiation) - dynamics - transport processes, which dominates stratospheric circulation. While the dynamics of the present general j circulation models used in the above-mentioned photochemical experi- mentation is based on a cl imatological ozone distribution, the ozone data determining the radiation field must in the feedback studies be produced by the model itself. Only this procedure can lead to the,. ! full understanding of stratospheric processes which is needed among other things in studies of climatic change. } UAPRC-4-4

THE GLOBAL DISTRIBUTION OF TOTAL OZONE AS DETERMINED BY SATELLITE

• *

.•/«•>• ' James E. Lovill

f Lawrence Livermore Laboratory, University of California, 'I Livermore, California, U.S.A.

1 • , M The paucity of total ozone measuring stations over vast regions of both the Northern and Southern Hemispheres has greatly

(1' hindered any complete understanding of the role stratospheric ozone plays in the general circulation processes of the atmosphere. This paper will study the satellite measured total ozone distribution over 1 t" both hemispheres. The results of this study are complementary to t'j -the numerical models that have been developed at the Lawrence | Livermore Laboratory. These models have been developed to 'I study (1) the general circulation characteristics of the atmosphere, * . (2) the effect of man-made perturbations in the atmosphere, f. (3) photochemical and transport problems.

; -' A comparison of time-longitude stratospheric radiance ' i. values at 60 S with values of the total ozone indicated that low (high)

I t radiance values corresponded \/ery closely with low (high) ozone s , variations. The speed at which these ozone waves progress east- | ward is greater in the winter hemisphere. The speed of eastward | * progression decreases as one approaches the lower latitudes in the I "^ winter hemisphere. These waves will be discussed in relation to (1) global dispersion patterns that are produced by longitudinal asymmetries and (2) stratospheric modeling of ozone heating rates.

• The average latitudinal distribution of ozone is described, both temporally and spatially, during the autumn and winter in the Southern Hemisphere. The lowest mean total ozone value for the globe is observed at 6 S.

Maps are presented that describe the distribution of i total ozone for the Northern and Southern Hemisphere. Closely spaced total ozone isolines appear to reveal a rather strong jet stream west of South America at approximately 35 S.

Both the Northern and Southern Hemispheres appear to provide 'anchoring' mechanisms for total ozone ridges. The most 11 predominant ridges are also associated with the 'tightest' ozone gradients. In the Northern Hemisphere these locations are primarily Eastern North America, Central Europe and Eastern Asia. In the Southern Hemisphere ridges are evident over the East Indian Ocean, the Central Pacific Ocean and the Eastern Atlantic. The i-idges correlate closely with upper atmosphere height contours. The ridge pattern is easier to delineate In the Southern Hemisphere winter than in the Northern Hemisphere summer.

Observations of total ozone by satellite on a global-scale can prove to be quite useful fn the determination of the effects of man-made perturbations. By monitoring ozone variations over regions of suspected nitrogen oxide (NO) production, additional data will be made available as to the extent that NO will reduce ozone. UAPRC-4-5

*• OZONE TREND AND HAZE SCATTERING

R. N. Kulkarni

CSIRO, Division of Atmospheric Physics, , Aspendale, Australia t

It is known that total ozone in the atmosphere at a number of places in the world has increased (up to about 10% at some places) in the period 1960 to 1969. In Australia, Darwin showed an increase of 6. 0% from 1966 to 1970, and Brisbane an increase of about 5.7% from 1960 to 1969. At Aspendale and Macquarie Island although ozone was increasing in the last decade the increase was not statistically significant.

Since these observations are done with the Dobson Spectrophotometers and the equation used in calculating the j," ozone amount involves a differential scattering term which could i introduce a gradual error in the calculated ozone amount by a I •• gradual changing haze character, it was thought desirable to •'.. investigate this problem. |x. - x. ) values which represent [ the large particle scattering were used for investigating the effect of changing haze character on the calculation of ozone and its trend.

* It has been obser.ved that at Darwin and Brisbane (x. - x» ) decreases from 1960 to 1970 implying that the smaller , size particles are increasing in number in relation to larger size particles. It Is estimated that about 53% of the observed change

in x»n value at Brisbana is possibly due to changing haze pattern.

Variations of (x. - x. ) at these stations in Australia are discussed along with other observations on atmospheric turbidity at Volcanic eruptions, etc. UAPRC-4-6 THE UPPER TROPOSPHERIC CIRCULATION AND THE STRATOSPHERIC OZONE DISTRIBUTION IN THE SOUTHERN HEMISPHERE

P. J. Webster UnivefJity of Washington, Seattle, USA and

N. Sundararaman Cal ifornia State University, Northridge, USA

Using information from the recent "EOL.EL" balloon- satellite experiment, which provided a relatively dense collection of upper tropospheric wind, temperature, and pressure data over the Southern Hemisphere for the period, August 1971 to July 1972, an ozone climatotogy of the Southern Hemisphere is approached. The results of the study are presented in three parts:

(i) Using the "EOLE" data, a climatology of the upper tropospheric motions of the Southern Hemisphere is presented for the period in question with particular emphasis on the space and time scales of the various measured and derived quantities and the distributions compared with those of the Northern Hemisphere.

(ii) A study of the existing ozone network indicates that longitudinal variations exist in the Southern Hemisphere as they do in the Northern Hemisphere. The longitudinal variations of the upper tropospheric flow allow an understanding of this ozone distribution. The results of this correlative study and the ozone climatology from the relatively dense upper tropospheric data available for the "EOl_E" period are presented with specific synoptic case studies,

(iii) The ozone distribution is compared with that of the Northern Hemisphere and the similarities and differences discussed with particular emphasis on total ozone amount. Finally, a new global ozone budget is presented. UAPRC-5-1

LABORATORY STUDIES OF OZCNE PHOTOCHEMISTRY AND THEIR RELEVANCE ^O AT»/CS»-ER1C P-OTOC-EVISTPV

UAPRC-5

R. P. V/a."

er, we cor: ce~ = :o- .. ris/.ris/.ss oo- •-

r photoiys's >.c'cete :r£t e»c!e-c a:c'c =-c ~' ec- a' \* :^t' •* z~:~<: '.s

can be formed. The wavelength dependences of the various processes

are examined. Secondary processes involving the excited species,

such as reaction, quenching and energy transfer, are then discussed

in relation to their possible importance under atmospheric conditions.

Reactions of excited atomic oxygen (in, for example, D or S states)

with H^O or hydrocarbons can be a source of OH radicals. Recent

laboratory work which is ^©levant to the possibility that HO chains

play some part in controlling atmospheric ozone concentrations will

be reviewed and we then go on to discuss the reactions of the oxides

of nitrogen with ozone, and to evaluate the potential importance of

NO chains in the atmosphere. We fina'!\ coiisivir- tf,< :'n>ii,-,ii,»|.,

of the laboratory studies for the chemistry of a troposphere or

stratosphere which contains man-made contaminants. UAPRC-5-2 MESOSPHERIC NITRIC OXIDE DISSOCIATION AND IONIZATION IN THE 1O27-I33?A REGION

G. W. Adams, Space Environment Laboratory, NOAA Environmental Research Laboratories, Boulder, Colorado, U.S.A.

and

R. D. Harris and R. McCue, Center for- Research and Aeronomy, Utah State University, Logan, Utah, U.S.A.

Detailed calculations of mesospheric nitric oxide

dissociation and ionization between the O_ and NO fonization

c limits (1027. 5-1337. 5A) show that the contributions by Lyor

{1215. 7A) and by the rest of the wavelength region are comparable. A discussion of the band-averaging techniques used to handle the complex structure of the O_ and NO cross-sections

In this region will be given, and the resulting dissociation and ionization profiles presented. UAPRC-5-3 THE NON-PHOTOCHEMICAL PROCESSES OF OZONE FORMATION AND DESTRUCTION IN THE LOWER ATMOSPHERE

A. S. Britaev

Central Aerological Observatory, DoUjoprudm , U. S. S. R.

Comparatively well-studied photochemical ozone sources are situated in the upper stratosphere and mesosphere. Non- photochemical sources and sinks are acting in the lower layers. They

f' derive from the ionization processes (atmospheric electricity, snow-

•» storm electrification, cosmic rays), from the processes of gas

I ,.' solvation by aerosols, hydrometeors, water surface and soil, as

I.',. well as from chemical interaction of air ingredients with the surface, f' air pollutants and with the biosphere.

The capacity of these sources has been investigated by

measuring the ozone distribution with the help of very effective

current integrator analyzers. In particular we have studied the

influence of hydrometeors, humidity, ambient temperature and the

character of the underlying surface on the efficiency of the ozone

sources in Moscow. The ozone concentration is..likely to fall almost

to the zero in the presence of droplet fogs, drizzle, fine rains. As

the shower droplets are being warmed in the vicinity of the ground,

the ozone concentration grows. The capacity of this source is 11 -2 - 1 estimated to be about 1. 9* 1 0 MO • cm • sec £•* TV tower in Moscow have proved the highly stratified structure of The nocturnal ozone measurements from the 500-meter the lower ozonosphere with the smallest concentrations occ irring « TV tower i f'-~ at about the level of the temperature inversion. Ejji- The fallout of melting snow induced growth of ozone con- q{ . centration at the ground level at the rate of 1, 2 MO /m per hour,

I • while at the inversion point (50 meters above) the ozone concentration

*':.• remained constant. k The investigation of terrestrial ozone sinks and sources

claims the necessity of gradient ozone measurements with a time

resolution as short as 5 minutes and with an accuracy of 1/jg/m .

UAPRC-5-4 . OZONE MEASUREMENTS IN INDIA

C. R. Sreedharan, V. S. Tiwari and A. Mani

Meteorological Office, Poona ar.d Delhi, India

The measurement of ozone concentration at the earth's surface and in the atmosphere is of importance both in the study of the dynamics of the lowest layers of the atmosphere and in the study of air pollution near the ground. Using an experimental technique for the continuous measurement of ozone near the ground, with an electrochemical sensor developed in the Instrument Research Laboratories of the India Meteorological Department at Poona, continuous measurements of surface ozone concentration have been made at Poona (18 N) since 1969 and at Delhi (28 N) and Trtvandrum (8 N) since 1972. Regular fortnightly soundings with ozonesondes have also besn made at these three stations roughly along the 75 E meridian since 1971, using a Brewer bubbler type sonde with a non- reacting glass and teflon pump.

In the equatorial atmosphere represented by Trivandrum and Poona tropospheric ozone shows significant seasonal variations, but the basic pattern of the vertical distribution in the stratosphere remains practically unchanged throughout the year. In the higher latitudes represented by Delhi marked day to day variations are observed in the stratosphere associated with western disturbances and jet streams. r There is a marked diurnal variation in surface ozone concentration which clearly follows the diurnal variation of temperature. The diurnal variation is a maximum during the dry hot premonsoon months and a minimum during the monsoon. The surface ozone concentration also shows a pronounced seasonal variation, with a minimum during the monsoon months and a maximum during the pre- monsoon hot weather months. A secondary maximum in ozone concentration occurs in the forenoon during the winter months, associated with the breakdown of the temperature inversion that occurs near the ground. Sharp variations in surface ozone are observed in association with temperature inversions and air currents, with surface ozone changes being far more pronounced than those in any meteorological parameter.

An examination of the surface ozone data at the three stations shows a marked latitudinal variation in surface ozone concentration, with higher values occurring at higher latitudes.

From continuous measurements of the surface ozone, with three electrochemical sensors exposed simultaneously at three levels, 0, 15 and 35 metres above ground, using the rate of decay andRegener's profile methods the ozone flux near the ground and the coefficient of eddy diffusivity have been calculated. UAPRC-5-5 A STUDY OF TRO;JOSPHERIC OZONE AND EXCHANGE PROCESSES FROM WORLDWIDE SURFACE AND AIRCRAFT OBSERVATIONS

P. G. Pruchniewicz, H. Tiefenau, P. Fabian, P. Wilbrandt, W. Jessen

Max-Planck-lnstitut fur Aeronomie, D-3411 Lindau/Her2, Germany

Continuous registration of near-surface ozone has been

obtained during 1970-1973 from 15 stations operating in a meridional

chain between Troms/zf/Norway and Hermanus/South Africa. For

the same period 32 meridional profiles of the upper tropospheric

ozone concentration were recorded aboard commercial airliners

between Europe and South Africa.

The features of large-scale and seasonal variation of

tropospheric ozone are discussed in connection with the stratospheric ozone circulation, the stratospheric-tropospheric exchange,- the inter-hemispheric mass flux and destruction near the earth's surface.

For the northern hemisphere, the meridional distribution yields three bells of higher ozone intrusion at about 30 N, at between 40 - 45 N and at about 60 N.

A north-south hemisphere asymmetry in the tropospheric ozone content and its seasonal variatfon is apparent. These features will be discussed in detail in connection with the inter- hemispheric mass flux. UAPRC-6-1

OZONE CLIMATOLOGY, TRENDS AND THE MONITORING PROBLEM

UAPRC-6

A. B. Pittock

CSIRO Division of Atmospheric Physics, Aspendale, Victoria, Australia

Results from the first eijht years of the ozone sounding programme at Aspendale, Victoria, are presented and discussed in relation to data from the total ozone network and corresponding data from the northern hemisphere.

Mean annual cycles of the vertical distribution of ozone and its variability are presented, and its dependence on the strength of the meridional circulation is illustrated. Significant differences between the mean distributions at Aspendale and at corresponding latitudes in the northern hemisphere are found at most levels, with Aspendale having generally lower amounts. Possible reasons for these differences are discussed.

Trend analyses reveal a highly significant increase in ozone concentration between 1965 and 1973 at and above the 12 mb level, with a less certain decrease at and below the 25 mb level down to the 700 mb level. These trends are discussed in relation to circulation changes and other possible causes.

Finally, the limitations of trend analyses based on local and global monitoring data are discussed in relation to problems of natural and possible anthropogenic variations in climate. UAPRC-6-2 BEHAVIOR Or- ATMOSPHERIC OZONE DETERMINED FROM NIMBUS SATELLITE BACKSCATTER ULTRAVIOLET DATA

AH in J. Krueger

Goddard Space Flight Center, Greenbelt, Maryland, U.S.A.

The Backscatter Ultraviolet (BUV) instrument on the Nimbus 4 satellite is yielding a great quantity of information on the spatial and temporal variations of the high level ozone distribution and the total ozone amount. The latitudinal characteristics of the vertical ozone distributions are consis tent with our earlier limited knowledge from rocket soundings and the total ozone variations agree with results from the network of Dobson spectrophotometers. However, the uniform sampling density and wide geographic coverage of the satellite system are resulting in a substantial global data base for the time period 1970 through 1973. Furthermore, the satellite observations are revealing seasonal and geographic variations which were not anticipated.

Seasonal changes have been found at all levels up to the 0. 5 mbar level, the limiting altitude for the technique. Above 4 mbar, where photochemical equilibrium might be expected, the highest ozone mixing ratios are found at middle and high latitudes in the winter and spring seasons with values 2 to 4 times the summer values. At lower altitudes, the highest mixing ratios are found in the tropics at the 8 to 10 mbar levels.

Longitudinal effects are found below 4 mbar, particularly at the higher latitudes in the winter season. UAPRC-6-3 RECENT ADVANCES IN SATELLITE OBSERVATIONS OF SOLAR VARIABILITY AND GLOBAL ATMOSPHERIC OZONE

Donald F. Heath

Laboratory for Meteorology and Earth Sciences, Goddard Space Flight Center, Greenbelt, Maryland, U.S.A.

The sun has been under daily surveillance in the ultra-

violet since the launch of Nimbus 3 in April 1969. With the launch

of Nimbus 4 in April 1974 ultraviolet measurements of the solar

Irradiance by the Monitor of Ultraviolet Solar Energy (MUSE)

experiment and the atmospheric radiance and solar irradiance by the Backscatter Ultraviolet (BUV) experiment have provided concurrent observations of solar variability in the ultraviolet and global distribution of atmospheric ozone. Daily zonal means of ozone are compared with solar and geomagnetic phenomena. The long lived ultraviolet active regions on the sun which tend to be separated by 180 in solar longitude have been observed to be associated with the central meridian passage of solar magnetic sector boundaries which may be significant in evaluation of reported correlations between the solar magnetic sector structure and atmospheric circulation. UAPRC-6-4 THE INCREASE OF BfOLOGICALLY EFFECTIVE ULTRAVIOLET RADIATION DUE TO DECREASING OZONE CONCENTRATION

Rudolf Schulze

Meteorologisches Observatorium, Hamburg, Federai Republic of Germany

Diminuation of ozone concentration by stratospheric aircraft

exhaust would increase the uv radiation in the biosphere. In order to

estimate this effect, firstly the geographic distribution of the biologically

effective uv radiation (b. e. uv) was computed for several constant values

of total ozone content of the atmosphere. The b. e. uv radiation in the

equatorial zone, in the middle latitudes, and in the polar zone fs pro-

portional to about 10:4: 1.

When the ozone content is decreased by 10%, the increase

of b. e. uv amounts to 18% in the equatorial zone, to 19% fn the mfddle

latitudes, and to 22% in the polar zones.

Secondly, the actual global ozone distribution, depending

on geographic latitude and time of the year, was used to compute the present b. e. uv radiation climate. The actual b. e. uv on the southern hemisphere turns out to be higher than on the northern hemisphere, corresponding to the skin cancer frequencies observed on the respective hemispheres.

Thirdly, the increase of uv spectral irradiances due to decreasing ozone content was computed. For the wavelength 300 nm, the date of the equinoxes, and an ozone content decreasing from 3 mm to 2. 5 mm s. t. p. , the spectral irradiance increases by 90% in the equatorial zone, by 150% in the middle latitudes, and by 450% in

70 deg latitude. UAPRC-6-5 THE USE OF BUV SATELLITE OBSERVATIONS TO STUDY OZONE DEPLETION PROCESSES

v r "f A. D. Christie

}.>•* Atmospheric Environment Service, •'' J.t Toronto, Canada .'' -I1

• * *

f: Variations in the global distribution of atmospheric

\.'.L\ ozone, over a period during which a small megaton nuclear

J. weapon was detonated In tropical latitudes, have been studied

| ' using consistent observations from Instrumentation on the . .:/"

"*'•*

%\ Nimbus 3 satellite. Little change in ozone is observed, and

the results are used to speculate on the importance of S. S. T.

generated nitrogen oxides on ozone depletion.

I UAPRC-6-6 NEW INFORMATION FROM HIGH RESOLUTION STRATOSPHERIC SPECTRA

M. Ackerman

Institut d'aeronomie spattale de Belgique, Bruxelles, Belgium

Solar "spectra taken in 1973 on board balloon gondolas and aircraft have yielded information on NO, NO,, and H_O abundance in the stratosphere. The results will be discussed. I UAPRC-7-1 . I NIGHTGLOW AND DYNAMICS OF THE UPPER ATMOSPHERE -v * •f UAPRC-7 R. N. Kulkarni

CSIRO, Division of Atmospheric Physics, Aspcndale, Australia

A number of authors have remarked on the possibility of using airglow observations on "X5577 for understanding to some extent the dynamics of the lower thermosphere and upper mesosphere. Since the emission is from neutral oxygen atoms, it can be said that the observed motions of the isophotes are related to those of the neutral atmosphere.

The ground based nightsky observations on X 5577 made at Deniliquin, Australia (35° 32'^ 145° 02*E) at various angies in the N-S and E-W planes, combined with the existing data from Adelaide (34° 56'S, 138 35'E) and other places in the middle latitudes of the Southern Hemisphere are used to construct a in tne comprehensive picture of the seasonal variation of Icc77 middle latitudes of the Southern Hemisphere. It is interesting to note that the dissipation of turbulent energy and the diurnal wind energy have similar seasonal variations to that of I for the middle latitudes of the Southern Hemisphere. 5577

The year to year variation in the meafl values of 1 5577 are similar and opposite to the variation of total ozone in the atmosphere which is believed to be the result of the variation in the circulation of the lower stratosphere.

The short term and diurnal variations of I are presented and discussed in terms of atmospheric motion.

'•'rs UAPRC-7-2 VERTICAL MOTION IN THE MIDDLE AND UPPER STRATOSPHERE

Gerald F. Herman and Reginald E. Newell

Department of Meteorology, Massachusetts Institute of Technology, Cambridge, Massachusetts, U.S.A.

Data from the Nimbus IV Selective Chopper Radiometer for nine days in February, 1972 are used to reconstruct the global temperature distribution to 55 km. Well-developed slow-moving waves in the Northern Hemisphere show evidence of maximum amplitudes in the lower troposphere, and fn the lower and upper stratosphere. Typical amplitudes are or. the order of 35 K at 50 N. Amplitudes in the Southern Hemisphere are substantially smaller, and data for the Northern Hemisphere summer are used to estimate the extent to which this difference is due to seasonal changes in the tropospheric circulation.

The variation of phase with height indicates the vertical propagation of energy. The longitudinal temperature structure of the stratosphere is considered to be maintained by a vertical motion field which is forced from below, and we calculate the magnitude of this vertical r^otion from the first law of thermodynamics and calculations of radiative heating. The longitudinal temperature variation produced by the vertical motion Is limited by radiative damping, and estimates are made of the destruction of eddy available potential energy.

Vertical transport is less in the Southern Hemisphere, associated with the smaller amplitude thermal waves. Longitudinal variation of temperature in the tropics is on the order of 3 K and this is also indicative of the variation in the field of vertical motion.

For several of the days it was possible to compare the satellite temperatures with those obtained from the rocket network. Although the agreement is good in general, large systematic differences do occur. f " UAPRC-7-3 \ . \< ; ' A STUDY OF THE SOUTHERN HEMISPHERE STRATOSPHERIC I CIRCULATION REVERSAL USING SATELLITE RADIANCE INFORMATION

Keith W. Johnson and Roderick S. Quiroz

Upper Air Branch, NMC, NOAA, Hillcrest Heights, Maryland, U.S.A.

} ,'j The character and development of mid-winter thermal I ' patterns as well as the final spring warming and circulation reversal | in the Southern Hemisphere stratosphere have been difficult to study * . due to the scarcity of data above 30 mb. The Vertical Temperature Profile Radiometer (VTPR) on board the NOAA II satellite provides radiance information which is processed to supply temperature - • information, together with available rawinsonde data, is routinely analyzed by NESS, using a program developed by one of the authors. In this study we discuss the utility of this information in tracing the development of thermal patterns up to 30 km.

t. In addition, the Infra-red Temperature Profile Radio- meter (ITPR), and the Selective Chopper Radiometer (SCR) on the Nimbus V satellite provide radiance observations which are processed by'NESS in special cases to provide mandatory level temperature information for analyses up to 1 mb. The use of this information in studying development of thermal patterns at upper stratospheric levels is discussed.

Techniques have-also been developed for using satellite radiation measurements directly to infer the structure and circulation of the upper stratosphere in the Northern Hemisphere. The applicability of these techniques to the Southern Hemisphere is discussed and a brief review is made of winter and spring warming in the . Antarctic deduced with the aid of the satellite data.

t. * UAPRC-7-4 TEMPERATURE WAVES IN THE SOUTHERN HEMISPHERE STRATOSPHERE OBSERVED BY THE SELECTIVE CHOPPER RADIOMETER ON NIMBUS IV

R. S. Harwood

Department of Atmospheric Physics, Oxford University, U.K.

The paper describes the temperature field in the

southern hemisphere from 100-1 mb during August-October

1971 as revealed by the Selective Chopper Radiometer on the

Nimbus IV spacecraft with particular emphasis on the behaviour

and structure of zonal wavenumbers 1, 2 and 3. For a period

of 54 days, wavenumber two existed as a travelling wave

throughout the height range moving with a phase speed of IS

degrees longitude per day. UAPRC-7-5 VARIATION OF TEMPERATURE AND WIND REGIME IN THE UPPER ATMOSPHERE OVER THE ANTARCTIC

S. S. Gaigerov, V.V. Fedorov, M. Ya. Kalihman, Yu. P. Koshelkov, B. P. Zaichikov

Central Aerological Observatory, Leningrad, U. S. S. R.

' Meteorological rocket data obtained in the polar regions reveal large temperature and wind variability in the winter mesosphere. The maximal range of temperature fluctuations amounts to about 40 - 80 C in 7 to 10 days in the mesosphere. Temperature fluctuations gradualiy diminish In the stratosphere toward a minimum in the lower stratosphere. Warmings (and coolings) in the upper atmosphere precede those in the lower layers. Warm and cold pools can be seen overlying each other. Rocket observations at the Molodezhnaya station point out that the intensification of the westerly flow in the upper and middle mesosphere is usually accompanied by a warming while during the decrease of westerly winds as well as the growth of meridional wind components and development of easterly flow cooling of the upper atmosphere has been recorded.

i UAPRC-7-6 ON THE CHARACTER OF TEMPERATURE AND WIND VARIATIONS IN THE STRATOSPHERE OF THE EXTRATROPICAL LATITUDES

K. T. Logvinov and M. B. Barabash

Central Aerological Observatory, Leningrad, U. S. S. R.

Significant data of measurements on the rocket sounding network were collected during the past 15 years. Their analysis permitted the study of the distribution of the meteorological element fields in the stratosphere.

The study of the data of some rocket stations reveals sharp interseasonal variations of temperature and wind components In the stratosphere of the extratropical latitudes.

The analysis of monthly averaged values of temperature and wind components for the network measurements of 1961-1968 has shown that the main temperature and wind variations in the stratosphere took place with about a one-year period. At the same time, the semi-annual and two-year periods were revealed In the changes of these parameters. These periods are strongly marked in the variations of the wind components. ,

The greatest positive declinations of the zonal wind components with semi-annual period take place in spring and autumn months, and the greatest negative - in winter anc summer months. The semi-annual period of the meridional wind component Is displaced one half period relative to the zonal component. The maximum declinations of the meridional component coincide with the minimum declinations of the zona\ component and vice versa.

In the upper stratosphere the values of the amplitude of oscillation of the zonal and meridional wind components reach 30-35m/j and 8-10m/sec, respectively.

It is supposed that the changes of the wind components wfth the semi-annual period are seasonal variations of the meridional motior in the stratosphere, the maximum of which coincides with solstice, and minimum - with eau/nox.

Also, variations In the wind and temperature regimes In the- stratosphere with a two-year period are established. f V :.;;?•'/f ' • UAPRC-7-7

h:flt-?'< SOME SOUTHERN HEMISPHERIC MEASUREMENTS OF i-^-J ?' STRATOSPHERIC WINDS AND THEIR VARIABILITY

t *,,J' Jean E. Laby and E. L. Unthank ': .*••: .i. • vi'1;; Physics (R. A. A. F. ) Department, University of Melbourne, •;•-;' Melbourne, Australia

Radar tracked balloon flights were made daily during each of four sampling periods per year, 1967 - 1971 inclusive, atLaverton {3B°S, 145°E), Coffs Harbour (30°S, 1 53°E) and Longreach (24 S, 144 E). Each sampling period was of about », 12 to 14 days duration. From these launchings, wind data were obtained from the surface to 130, 000 ft. (40 km). Analysis of the zonal and meridional wind components so obtained have \-' V. •• yielded an 'average' annual distribution of wind speed versus f height and their variabilities at these three stations.

The dally sampling in the 30 to 45 km region has revealed many examples of large day-to-day variations in both {••if f zonal and meridional winds. Changes at the rate of 20 knots per day-over several days have been measured at all stations during the winter months whilst examples of much higher rates have been recorded at Laverton. Ill ff:;'. During the currency of these measurements several |'^X periods of stratospheric easterlies were observed at Laverton S disturbing the normal winter westerly flow, whilst in ? 969, the il turn around from winter westerlies to summer easterlies was £ : adjudged to be anomalous. These occurrences have been shown Sf to correlate highly with stratospheric warmings in the higher f latitudes. ! t An attempt was made to evaluate the usefulness of the I rocket winds obtained above 35 km at Woomera (31 S, 136 E) in planning research balloon flights elsewhere in Australia. Dai loon launchings were made at Longreach, Coffs Harbour and Laverton to measure stratospheric winds at the same time as rocket firings from Woomera. Results suggested that, on this scale of distances, the spatial variation of winds above 35 km is considerable even at the same latitude. UAPRC-7-8 ON THE STRATOSPHERIC RADIATION CLIMATE AS OBSERVED BY OZONE SONDE, RADIOMETER SONDE AND DEW-POINT HYGROMETER DURING FOUR YEARS FROM 1969 TO 1972 IN JAPAN

K. Sekihara, M. Kano and M. Miyauchl

Meteorological Research Institute, Tokyo, Japan

Owing to many efforts of Japan Meteorological Agency

Staffs various meteorological elements of the upper atmosphere

have been measured reliably and accumulated recently. Of these,

ozone amount, downward flux of radiation and water vapor mixing

ratio above the level of 10 km that were taken at the same date

have been selected and plotted as one set of curves. And in

addition by use of air temperature that were also measured routinely

the consistent theoretical downward radiation fluxes were calculated

in several cases in order to compare with measured ones and also

to seek the effect of additional radiation other than due to water

vapor and ozone-.

On the basis of statistical averages of different period

of time the recent trend of stratospheric radiation climate near Japan

is discussed. * ;-«' UAPRC-8-1 '" "'ft: DAYTIME WINDS IN THE LOWER THERMOSPHERE

UAPRC 8

C. H. Low and A. D. Hind

Australian Defence Scientific Service, Department of Supply, Adelaide, South Austral ia

Lower thermospheric winds have been measured in the altitude range 100 to 220 km, using chemical tracers in the dusk to dawn period, for over ten years in different parts of the world. Daytime wind measurements have been made in limited altitude ranges by ionised meteor trail drifts and ionised irregularity drifts.

A number of groups have worked on measuring daytime winds using lithium as a tracer and a narrow pass band photometer as detector, in place of photographic recording used at twilight and at night. The group at W. R. E. have now demonstrated that such a system works and have made measurements on a number of daytime trails.

A brief description of the Upper Atmosphere Research Group's Daylight Lithium Detector is given.

The results obtained so far are presented and compared with those obtained at twilight and at night. UAPRC-S-2

GRAVITY WAVE COMPONENTS OF WINDS IN THE UPPER MESOSPHERE AND LOWER THERMOSPHERE

A. H. Manson and J, B. Gregory

Institute of Space & Atmospheric Studies, University of Saskatchewan, Saskatoon, Saskatchewan, Canada

Progress in the techniques of measurements and analysis of radio-wave partial reflection drifts now permits the determination of departures from mean wind profiles on time and space scales appropriate to gravity wave motions. The main features of this work, and results of observations during

1972-1973 near Saskatoon, Canada, are discussed. UAPRC-8-3

t1., • '.!• COMPOSITE ROCKET & RADIO WAVE WINDS TO 100 KN/ MEASURED DURING 1969-1973 IN WESTERN CANADA

J. B. Gregory and A. H. Manson

institute of Space £> Atmospheric Studies, University of Saskatchewan, Saskatoon, Saskatchewan, Canada

S .'• A series of measurements of winds, 65 to 100 km has i been made at Saskatoon, Canada (52N, 110W) for the years t 1969-1973 by the partial reflection drifts technique. These f radio-wave winds are incorporated with rocket winds from

I' ; Primrose Lake (54N, 110W) as a tirre cross-section.

The main features of the wind profiles are in accord

;:'...' with current models of global winds. Significant departures

;•• " from the models exists in respect to velocities; measured magnitudes

being lower; and to inter-annual variations.

•'•-• The boundary between the eastward flow in the winter

;!•"• mesosphere, and the westward flow of the lower thermosphere,

-;'.'.;. is shown to progress downwards during the winter polar cyclone;

•V;' but in a manner which varies from winter to winter.^ The flow at

'i.» altitudes above 80 km shows evidence of inherent perturbations;

;t but is also perturbed from lower altitudes. Examples are given

\ of anticyclonic systems in mid-winter which persist from the

V surface to £ 1 00 km. UAPRC-8-4

UPPER ATMOSPHERE WINDS BY RADIO TECHNIQUES

B. H. Briggs, T. J. Stubbs, and R. A. Vincent

University of Adelaide, Adelaide, Australia

Reflections of radio waves from weak irregularities of ionization in the D region of the ionosphere can be observed over the height range 60 - 100 km. Observations of the fading of these waves made at spaced aerials can be used to obtain the horizontal motion of the atmosphere in this height interval.

In the present paper observations made at Adelaide and at Woomera (South Australia) by this technique are reported. The results show clear evidence of prevailing winds, strong tidal components (with the diurnal tide predominant), and also evidence for shorter period velocity fluctuations. Comparisons wfth drifts of meteor trails made at Adelaide show good agreement. Comparisons with winds observed at Woomera by various rocket techniques, including drifts of luminous vapour trails, have aiso been made. Although this aspect of the work is at an early stage of development, encouraging evidence of agreement has already been found.

It is concluded that the radio wave sounding technique provides c valuable and relatively inexpensive method for obtaining continuous observations of horizontal atmospheric winds, tides, and wave phenomena in the height range 60 - TOO km. Its use on a world-wide basis should be encouraged. 'PRC-8-5

A 6-YEAR SYNOPTJC STUDY OF WINDS BETWEEN 80 AND 100 KM, FROM METEOR TRAIL DRIFTS

W. G. El ford and S. A. Young

Department of Physics, University of Adelaide, Adelaide, Austral ia

Prevailing and tidal winds are determined from

regular meteor drift observations carried out at Adelaide,

South Australia, during the period 1966-1972.

Monthly averages of zonal and meridional winds over

the height range 75 - 105 km are presented in the form of isotachs

for six successive years. The zonal winds are predominantly

eastward with the intrusion of a westward flow above 95 km

during winter and spring. The meridional flow is directed

away from the pole during summer and toward the pole during

winter.

The 24 hour and 12 hour tidal winds show marked

variation with height and season but the annual behaviour is very

similar from year to year.

Calculations of the mear seasonal transient eddy

momentum flux have been carried out using daily measurements of the prevailing components of the wind. Results averaged over the six years are presented. UAPRC-8-6 THE DYNAMICS OF THE TURBOPAUSE

R. G. Roper

Georgia Institute of Technology, Atlanta, U.S.A.

The history of upper atmosphere physics has been characterized by an original assumption of static conditions, with a gradual modification towards dynamic modeling and an eventual meteorology of the region as more data becomes available. While, for most, meteorology "finishes" at 30 km altitude, high altitude balloons and meteorological rocket networks have pushed "conventional" meteorology into the stratosphere and mesosphere, and remote sensing techniques such as meteor wind radar have established the existence of a. synoptic meteorology, to 100 km altitude. The last few years have seen an extension of dynamic meteorology into the thermosphere as a necessary adjunct to realistic aeronomy. In particular, the establishment of relationships between the dynamics of the turbopause region and aeronomic measurements requires considerable meteorological input.

Even though both the altitude and the Intensity of mixing at the turbopause have been investigated for over a decade, there is as yet no accepted model which adequately incorporates diurnal and seasonal, let alone possible solar cycle variations. Dawn/dusk pairs of rocket released vapor trails evidence considerable variability in both mixing intensity below the turbopause, and turbopause altitude. The turbulent intensity in the meteor region (80-100 km), as measured by the radio meteor wind technique, shows marked seasonal, as well as diurnal and possible solar cycle variations. Radio measurements of the height variations of sporadic E layers have been related to turbopause altitude, as have measurements of atmospheric constituents by rocket borne mass spectrometers in the lower thermosphere, and attempts have been made to correlate turbopause altitude with exospheric density.

The turbulent intensity below 100 km maximizes In the early morning in the summer, and in the late afternoon in the winter, and varies seasonally, being greater in winter than in summer, with some years exhibiting equinoxfal maxima. The observed annual-variation in turbulent intensity below 100 km is out of phase with the turbopause altitude variation required to explain, for example, the thermospherlc helium distribution. In the southern hemisphere, correlation with the amplitude of the diurnal tidal wind has been found. As yet, the relationship between turbulent intensity below 100 km, and the height of the turbopause, has not been conclusively established.

In this paper, the current knowledge of turbopause dynamics is reviewed, with emphasis being placed on those models based on direct measurement, and related to the meteorology of this altitude region. A tentative global model of turbopause altitude and intensity is proposed. UAPRC-8-7 INVESTIGATIONS INTO THE NATURE OF THE TURBOPAUSE

K.H. Lloyd

Australian Defence Scientific Service, Department of Supply, Adelaide, South Australia

The structure of vapour releases into the upper

atmosphere from rockets, usually show an abrupt transition from

a turbulent to-a laminar form, at about 105 km altitude.

The problems in giving a criterion for this sudden cessation of turbulence at this altitude, known as the turbopause, are discussed, and a model for the turbopause, developed in analogy with the oceanic thermocline, is described.

Data are presented, showing vapour trails in which the transition region does, and does not, exist, and reasons for the different observations are discussed. UAPRC-9-1 TRAVELING PLANETARY-SCALE WAVES H* UAPRC-9 R. J. Del and

Department of Meteorology and Oceanography, Polytechnic Institute of New York, Brooklyn, N. Y. , U.S.A.

Observations of traveling atmospheric Rossby waves of largest scale, using conventional isobaric analyses, satellite infrared radiance (SIRS) data, and various kinds of ionospheric measurements, are briefly described and compared. The vertical and horizontal structure of these waves, extending from sea-level to at least 100 km, and from middle southern to middle and higher northern latitudes, is described. The results of spectral analysis, of both amplitude and phase, of the traveling waves are shown, demonstrating their remarkable coherence and small phase shifts over the entire vertical extent of the analyzed data and from equatorial to high middle latitudes. Differences in average behavior in the northern and southern hemispheres are described, and also the manner in which they extend at times from one hemisphere to the other, as demonstrated by Madden and Julian. The relationship between the vertical structure of the waves and their phase velocity with respect to the earth is described. Evidence of upward propagation of transient, that is non-sinusoidal, disturbances of planetary scale is also presented.

Estimates of the vertical energy flux associated with the traveling waves are made, based on the approximate (quasi-stationary) theory of Eliassen and Palm, the applicability of which is justified by considering the waves as stationary in an atmosphere moving at a speed equal to the difference of the wave speed and the average speed of the zonal wind. The results show that the structure of the traveling waves in the northern hemisphere is consistent with baroclinic conversion of energy from the mean flow to the traveling waves. UAPRC-9-2 PLANETARY WAVES IN THE SUMMER STRATOSPHERE AND MESOSPHERE

Isamu Hirota

Meteorological Research Institute, Tokyo, Japan

Planetary variations of temperature and wind fields in the upper stratosphere and lower mesosphere were analyzed by the use of meteorological rocket observations for the summer season of the Northern Hemisphere.

Frorr the vertical time-sections of temperature and winds at Cape Kennedy (28N, 81W), Barking Sands (22N, 160W) and other rocket stations in subtropics, it is found that the oscillation of these quantities with a period of 10 to 15 days is predominant above 30 km. To describe the nature of wind and temperature oscillations quantitatively, a power spectral analysis Is made for the rocket data during the period July through September In 1969 and 1970.

Further analyses indicate that the oscillation as revealed by the time series analysis for individual observation stations is a reflection of the horizontal movement of planetary waves embedded in the summer mesosphere easterlies. The east-west wavenumber is estimated as 2 or 3, and the vertical wavelength is close to 15 km. The wave amplitude increases with Increasing height In the stratosphere, but the wave energy density decreases with height indicating that the wave Is an evanescent mode.

The existence of planetary-scale wave disturbances in the summer stratosphere is also confirmed from the analysis of recently available meteorological satellite observations such as NIMBUS-SIRS and JTOS-VTPR.

Finally discussions are extended to the relationship between the winter and summer hemispheric circulations from a viewpoint of the planetary wave dynamics. J: '-.:.> UAPRC-9-3 r SUGGESTED CAUSES OF LATITUDINAL ASYMMETRIES OF PERIODIC i ,„ . VARIATIONS OF THE STRATOSPHERIC ZONAL WIND

A. D. Belmont, D. G. Dartt and G. D. Nastrom

Research Division, Control Data Corporation, Minneapolis, Minnesota, U.S.A.

Latitude-time sections of zonal winds from 20 to 60 km,

from 80 N to 80 S, 1961-1971, show interesting distributions with

latitude of the amplitude of their periodic variations. The minimum

in annual variation occurs slightly north of the equator, possibly

due to the eccentricity of the earth's orbit. The tropical semi-

annual wave has a maximum belt which coincides well with that of

the geomagnetic equator. Along 15 W it is at 8 S; at 170 E it o*

is 8 N. The recently found polar semiannual wave-may also be

consistent with magnetic variations. A terannual wave, found in

the analysis of single station data, was here reduced to the noise

level by the smoothing of interpolation on the latitude-time sections.

Its source is apparently the squarish shape of the annual insolation

absorption function at high latitudes. UAPRC-9-4

STRUCTURE OF THE STRATOSPHERE AND MESOSPHERE IN THE SOUTHERN HEMISPHERE

Yu. P. Koshelkov

U. S. S.R.

Rocket observations at Molode^hnaya (68 S, 46 E)

have shown that the upper Antarctic stratosphere (30 - 50 km)

is markedly warmer than that of the Arctic beginning with mid-

winter and especially in spring. In summer the temperature

difference between hemispheres lowers in magnitude, while

remaining up to the height of 40 - 45 km. in autumn and early

winter the upper Antarctic stratosphere, as well as the lower

stratosphere, is colder than that of the Arctic.

The lower mesosphere (50 to 60 km) over the Antarctic

is likely to be colder than over the Arctic all the year round. No

definite temperature differences between the two hemispheres have

been found in the upper mesosphere (65 - 80 km).

Mean pressure and density values in the stratosphere

and mesosphere of the southern hemisphere are considerably lower

than in the northern hemisphere. Negative deviations from the

latter amount to 25 to 40 percent in late winter. Maximum

deviations above 40 km have been observed in mid-winter, the magnitude being comparable with that of the lower stratospheric

layers. Pressure and density differences between hemispheres are retained up to the mesopause level in the winter period. In summer pressure and density values in the upper stratosphere and mesosphere are comparable in the two polar regions. » #> . UAPRC-9-5 * I GLOBAL INTERACTIONS IN STRATOSPHERE AND TROPOSPHERE I A. B. Pittock

CSIRO Division of Atmospheric Physics, Aspendale, Victoria, Australia

6 Significant correlations have been found between year-to- & year mean latitudes of the surface high pressure belt, l_, over Eastern ft Australia and atmospheric parameters such as total ozone, winds and V temperatures at various levels in the troposphere and stratosphere, **' and rainfall. These correlations extend from the tropics to the pole, I* and from Cape Town in the west to Chatham Island in the east. They | are thought to be representative of the mean meridional behaviour of % the Southern Hemisphere, and account for more than 50 percent of the s total yeai—to-year variance in various meteorological quantities at | many stations.

In addition, the pressure difference Papeete minus Darwin, which is a measure of the strength of the Walker circulation, and referred to here as ASOI {abbreviated Southern oscillation index after Troup), is found to be significantly correlated with total ozone, upper air temperatures, and rainfall over wide areas extending from Japan in the north to Amundsen-Scott in the south.

L & ASO! are not significantly correlated with each other in the southern spring (when the above relationships are most in evidence). It Is suggested that L is an indicator of the strength of the mean meridional Hadley circulation (via the mechanism governing the onset of baroclinic instability) which largely determines the magnitude of the mean meridional transport of heat, momentum and ozone to higher latitudes. ASOI on the other hand, indicates the degree of asymmetry between the eastern and western hemispheres. Between them, i_ and ASOI account for the major part of the total year-to-year variance of many meteorological elements over a major part of the Southern Hemisphere. It is suggested that the patterns of correlation with L and ASOI probably correspond to the first two characteristic patterns of climatic variability in the Southern Hemisphere, and that it should be possible to identify and quantify appropriate forcing functions and feedback processes so as to produce a mode! of climatic variability which may have prognostic value. - -1 ') - 4 b'iNUPTIC STUDY OF CRITICAL LAYER PHENOMENA UURING STRATOSPHERIC WARMINGS

Keith W. Johnson

Upper Air Branch, NMC, NOAA, iillcrest Hoiqhts, Maryland, U.S.A.

c. ..inj U' the stratospheric model proposed by "1 i p.jjsiblc initiating mechanism for a strato- •i '- the development of a critical layer in Ihe "•?. Oi«Jdri:;on has shown that critical layer 't,'r,\/t . ,)(.)' in

• '. study it is shown that only a small I \ (. 'i ity generation can be attributed ! I i irijor part of potential vorticity c ;•.' critical layer absorption and in turn '•rii'i 'ii of potential vorticity generation is 'K.I it of the stratospheric warming.

• i• viriz.jtion techniques in a critical .p'- is discussed and such techniques are ihi'- lor tl'>' stratosphere. 4 •?''*' .' UAPRC-10-5 ?* SEASONALLY-ZONALLY AVERAGED TRANSPORT AND DIFFUSION . MODEL DERIVED FROM ISENTROPIC TRAJECTORIES AND POTENTIAL VORTICITY

"A, ' i- Edwin F. Danielsen and Dennis G. Deaven

.; National Center for Atmospheric Research, i Boulder, Colorado, U.S.A.

When the continuity equation of a conservative substance or quantity is averaged both zonal I y and temporally to produce a suitable equation for a meridional-vertical transport and diffusion model, the flux divergence is decomposed to products of mean values and correlations between products of deviations from the mean values. For a seasonal model based on observations there are approximately 180 realizations of the air parcels, separated by the 12 hours between observations but related to each other by the 12-hour trajectories of the parcels. The irreversible mixing each parcel undergoes in 12 hours is generally negligible compared to the "mathematical" mixing produced by averaging each of the separate realizations; therefore to a first approximation we may derive the mean and eddy fluxes from isentropic trajectories and the principal of conservation of potential vorticity. The model discussed in this paper is derived from isentropic analyses and isentropic trajectories and potential vorticity analyses based on solutions of the balance equation. Each analysis is objectively determined by computer j algorithms from the National Meteorological Center's constant f pressure analyses over the Northern Hemisphere. Results for one | season are discussed including the flux terms themselves and the "t suitability of approximating these fluxes by a diffusion tensor times I the mean gradient of the conservative quantity. UAPRC-10-6

DIURNAL KINETIC MODELING

Robert J. Gelinas

Lawrence Livermore Laboratory, University of California, Livermore, California, U.S.A.

To date there has been little or no rigorous inclusion of diurnal variations of trace species in theoretical dynamic-klneti models of the stratosphere. This is undoubtedly due to rather severe difficulties that arise with numerical integration methods when applied to differential equations with time-varying reaction rate coefficients. In order to view the underlying difficulties in their rrfbst elemental form this paper reduces the treatment of diurnal variations to a strictly time dependent, or kinetic, viewpoint. To further clarify the basic physical and numerical problems, only purely absorbing atmospheres are considered. Reaction sets of increasing complexity (starting from the Chapman reactions) are considered for various altitudes, latitudes, and time spans. LLL versions of the Gear method are used to integre the reaction sets. The numerical difficulties encountered by high accuracy ordinary differential equation (ODE) solvers in connectk with time-varying reaction coefficients are described and strategi to delay (but not necessarily to correct) integration abortions are indicated. The reliability of these strategies is also considered. Finally, solutions for the various reaction sets and selected conditions are presented and compared to conventional kinetic treatments that employ constant, or seasonally varying, photodissociation rates. Sensitivities to uncertainties in microscopic absorption and quantum yield data and to solar flux uncertainties are presented. UAPRC-11-1 SOME POSSIBLE PHOTOCHEMICAL IMPLICATIONS OF A VERY DRY STRATOSPHERE OBTAINED WITH A GENERAL CIRCULATION MODEL UAPRC-II

B. G. Hunt

Commonwealth Meteorology Research Centre, Melbourne, Australia

An 18 vertical level hemispheric, stereographic projection,

general circulation model incorporating the hydrologic cycle has been

runout for annual mean conditions. Although realistic water vapor

concentrations were obtained in the troposphere and the vicinity of

the tropopause, very much drier conditions than observed were derived

in the model stratosphere. Several explanations are possible for this

discrepancy. They include the omission from the model of transport of water vapor into the stratosphere by cumulus cloud, errors produced in the model at low latitudes by the equatorial^wall, etc.

Of particular interest are the suggestions in the literature that oxidation of methane could act as a source of stratospheric water vapor.

This aspect will be discussed in more detail as well as other photochemical consequences of this problem. UAPRC-H-2 A GENERAL CIRCULATION MODEL OF STRATOSPHERIC OZOf

D.M. Cunnold, F. N. Alyea, N.A. Phillips, and R. G. Prlnn

Department of Meteorology, Massachusetts Institute of Technology, Cambridge, Massachusetts, U.S.A.

A multi-level global circulation model of the stratosphere which fully contains the physics of the interaction between ozone and the dynamics is being developed. It Is being used to simulate the transport of ozone in the stratosphere and to predict the changes in the global ozone distribution resulting from the NO injected by supe sonic transports.

The residence time of ozone in the lower stratosphere is several years and strong seasonal variations in the ozone and the ' dynamic budgets of the stratosphere exist; thus, the model must be capable of simulating several annual cycles. Furthermore, It Is desirable that several simulations be made to include various combinations of poorly known parameters (such as the austausch coefficient used to represent those vertical motions neglected in our model, and the source rate of NO from supersonic transports). Therefore, since we are interested in the stratosphere where smalle scale structure appears to be of secondary importance, a limited representation of the dynamics is utilized. The quasl-geostrophlc approximation is assumed and the horizontal variation of the depende variables - vortfcity, temperature, vertical velocity, and ozone mix ratio - is represented by 79 spherical harmonics. In the vertical direction 26 pressure surfaces (equally spaced In log p) between the ground and approximately 70 km are used giving a height resolution of approximately 3 km. The treatment of ozone photochemistry Is similarly limited and Includes only the Chapman reactions plus three reactions Involving NO .

The predictions of the model relating to the unperturbed stratosphere are being compared against observations of the ozone " distribution and mass and energy fluxes in the stratosphere. Initial predictions of the effect of supersonic transports on the ozone distribution will also be presented.

*This research is sponsored by the Atomic Energy Commission and the Department of Transportation under contract number AT (11-1)! 2249. I ' . UAPRC-11-3 SEASONAL AND LATITUDINAL VARIATIONS OF NO AND ; IN THE STRATOSPHERE

R. Krishna-Rao Vupputuri

Atmospheric Environment Service, Toronto, Canada

T b The seasonal and latitudinal behaviour of N-O and NO ... j> • * *

• M' In the stratosphere is investigated based on their currently known

f natural sojrces and sinks. This is done using a two dimensional

ft model which permits both horizontal and vertical transport processes

I to be Incorporated along with the photochemical processes. ,jjip The results show that the parameterized transports, •• namely the large scale eddy effects and the mean meridional motions f which affect the photochemical production and loss processes through If redistribution play a significant role in the maintenance of the absolute | concentrations of N_O and NO in all regions (both in summer and .. winter) except in the summer upper stratosphere. The vertical distributions of NO indicates, the mixing ratio Increases in the x

stratosphere from its lower boundary value (3 parts per billion) by

a factor of 6 In summer and 4 in winter on the average. In the

meridional direction the NO mixing ratio varies by a factor of x

2 with higher values occurring near the summer pole.

The lower boundary condition Influences the NO

concentration in the lower stratosphere but It has negligible

effect in the middle and upper stratosphere. UAPRC-11-4 THE ROLE OF STRATOSPHERIC POLLUTANT GASES (HO, NO ) IN THE OZONE BALANCE AND IT'S IMPLICATION FOR THE SEASONAL CLIMATE OF THE STRATOSPHERE

R. Krishna-Rao Vupputuri Atmospheric Environment Service, Toronto, Canada

A steady state zonal I y averaged model of the stratosphere wh incorporates the interactions between radiative-photochemical effects ar transport processes is used to investigate the pollutant effects of water vapour and nitrogen oxides on ozone, temperature structure and the mea circulation of the stratosphere in different seasons. Based on recent advances in the ozone photochemistry of the stratosphere the previous oxygen-hydrogen-nitrogen photochemical scheme is modified to include the reactions and the reaction rates that are generally accepted in the current literature.

The results of the numerical experiment consist of two parts. In the first part the meridional distribution of ozone mixing ration, temperature and the mean circulation are calculated under the combined influence of radiative-photochemical-transport processes using the back ground concentration of HO and NO that are considered to be typical o an uncontaminated atmosphere. In fhe second part of the experiment the sensitivity analysis is performed on ozone and heat balance of the stratc sphere by arbitrarily Increasing the initial background values of HO an NO by 50%.

Based on the results of the first experiment it is found that t\r nitrogen oxides contribute to substantial decrease of ozone and conseque the temperature throughout the stratosphere. Associated with the chan< in the ozone and heat balance, significant changes are also shown to be occurring in the zonal wind systems and in the vertical component of the mean meridional motion. The effects of water vapour on the other hand are considered significant only in the upper stratosphere where they cor tribute to substantial ozone reduction and temperature.

The sensitivity analysis shows that 50% increase in the water vapour mixing ration has little effect on ozone and temperature structure: in the lower stratosphere (less than 1% ozone reduction and less than ; . 03% reduction in temperature) although the ozone and temperature chan1 are considerably more significant in the upper stratosphere. In the cas where nitrogen oxides are increased by 50% the changes In ozone and : temperature are substantial throughout the stratosphere. In the lower stratosphere the ozone mixing ratio and temperature are reduced by i 15 to 30% and 0. 3 to 0.7% respectively. ]

The implications of ozone reduction on biologically effective < radiation (around 3050 A) reaching the ground are discussed. .•.-••.. UAPRC-11-5 fHE EFFECT OF SST EMISSION ON THE EARTH'S OZONE LAYER

R. C. Whitten, Space Science Division, NASA Ames Research Center, Moffett Field, California, U.S.A. and

R. P. Turco, R and D Associates, Santa Monica, California, U.S.A.

We have constructed a one-dimensional model of the minor A. constituents in the earth's stratosphere. Both chemical reactions and vertical transport by eddy diffusion have been included in the model. The coupled set of mass and momentum equations have been solved using a "semi-implicit" method (I.e. implicit in loss and transport terms, explicit in production terms). A technique based on atom conservation among the various species has been developed in order to insure accuracy. Boundary conditions are of considerable importance t and we have been careful to enforce conditions which yield experimental results near the lower boundary (10 km). Sensitivity tests have been applied in cases where the choice of the lower boundary condition for a given species is uncertain. Computations have been carried out for a simulated period of two years; the results are in good agreement with observations reported to date. The cases in which disagreement occurs will be discussed.

We have also carried out computations for a predicted 1990 fleet of SST's flying in a corridor from New York Jo London. The reduction in ozone columr. density due to water vapor deposition is completely negligible (less than 0. 1 percent), but column density reductions of ozone due to reaction with nitrogen oxides ranges from 2 to 11 percent, depending upon assumptions made about meridional spreading.

The computations discussed above are for a mean solar zenith angle only. We have recently extended the model to include diurnal variations. Preliminary results indicate that the effect of inclusion of the diurnal cycle on the daytime minor constituent concentration profiles, including the porturbod ones, is nut iin

Finally, we mention that changes in the osone balance <. an substantially influence atmospheric circulation. Although we do not compute such changes, our model results have direct application in this area. UAPRC-1 1-6

DISPERSION OF SST EXHAUST PLUMES IN THE STRATOSPHERE

John J. Wai ton

Lawrence Llvermore Laboratory, University of California, Livermore, California, U.S.A.

The dispersion of the exhaust plume left by a supersonic

transport is governed by turbulence on the scale of this plume. For

this reason, and because of the low level of turbulence in the stratosphere, relatively high concentrations of reactive materials may remain for extended periods of time. The effect of this phenomenon ; on the chemistry associated with a single plume has been studied using two coupled transport and chemistry models. !n the first model transport is parameterized in a one box kinetics calucation.

In the second model transport due to diffusion and advectlon in a two-dimensional frame can be treated explicitly. In addition to studies of a single plume, estimates have been made of the total buildup of material within a specified flight corridor. UAPRC- 1 2- I

DISPERSION OF SST EFFLUENTS IN THE STRATOSPHERE UAPRC- I 2

George F. Widhopf and Thomas D. Taylor

The Aerospace Corporation, Los Angeles, California, U.S.A.

The present paper will describe a numerical model for calculating dispersion of trace species in the atmosphere with direct application to the determination of the effect of SST pollutants on the natural stratosphere. Due to the fact that the state-of-the-art numerical global circulation modeling has not progressed to the stage of adequately predicting local atmospheric quantities and considering the insurmountable computer problems of a general three-dimensional model for the spatial scales of interest in this region, a phenomenological two-dimensional, 2onally averaged model of the atmosphere similar to that of Reed and German has been formulated.

Specifically, for the time scales of this problem, the effect of the pollutant trace chemistry on the hydrodynamic description of the atmosphere has been neglected and only their effect on the transient spatial distribution of the interesting atmospheric species is considered. Thus, the description of the natural atmosphere is prescribed (i.e., local thermoflynamic state, advec'ive and turbulent transport) and used to determine the transient spatial distribution of the important trace species considering multicomponent finite rate chemistry.

The complete paper will describe in detail the numerical models developed to predict both the "natural" and perturbed atmosphere. Specifically, the dispersion of the SST wake and the effective change in the flight corridor trace species concentrations will be presented together with the predicted global source rates which are to be supplied to the global modelers.

Reference: (1) Reed, Richard J. and German, Kenneth E. , "A Contribution to the Problem of Stratospheric Diffusion by Large Scale Mixing, " Monthly Weather Review, Vol. 93, No. 5, May 1965, pp. 313-321. UAPRC-12-2 SOME ANALYSES OF THE CHEMISTRY AND DIFFUSION OF SST EXHAUST MATERIALS DURING PHASE Ml OF THE WAKE PERIOD*

Glenn R. Hi 1st, Coleman duP. Donaldson, Ross ContIllano

Aeronautical Research Associates of Princeton, Inc. , Princeton, New Jersey, U.S.A.

The impetus for A. R. A. P. 's contributions to the DOT/CIAF analyses may be traced to the recognition that, in the generally stably stratified lower stratosphere, SST exhaust plumes could sperd a significant length of time in relatively high concentrations. There is a very real possibility that during a significant part of their residence time in the lower stratosphere SST exhaust materials behave quite differently than had been proposed In the earlier studies of their potential environmental impact. The studies reported here have attempted to test the bases of these earlier analyses and, where these have been found to be inadequate or erroneous, to develop more exact methods for the CfAP evaluations.

The results of these studies to date may be summarized as follows:

1. A detailed examination of the chemical depletion of ozone (O_) by the so-called NO catalytic cycle during the time SST exhausts are confined to above-background concentrations (the Phase III wake period in CIAP parlance) shows that the combination of relatively slow diffusive mixing and rapid chemical reactions serve to minimize the effect of SST exhausts on O_ depletion. While the SST-produced NO is substantially above background concentrations, it appears diffusive mixing of NO and O, is simply too slow to produce the O, depletions originally proposed.

2. The time required to dilute the SST exhaust plume may be a significant fraction of the total time these materials are resident in the lower stratosphere. If this is_ the case, then prior estimates of the environmental impacts of these materials must be revised significantly downward. ^

The combination of these conclusions must be tempered by a clear recognition of the uncertaintres of present knowledge and demonstrable facts which plague any analysis of this kind. However,

*Work sponsored by Contract NAS1-11873 it is evident that prior evaluations have uniformly adopted a conservative set of assumptions, in the sense that they lead to estimations of the maximum effect SST operations could have on the stratospheric environment. In the face of ignorance and uncertainty, this is, perhaps, a "safe" course to follow. A much more rational course, however, is to remove the ignorance and minimize the uncertainties, so that we might evaluate these effects confidently.

UAPRC-12-3 EXPERIMENTAL STUDY ON THE EFFECT OF SUPERSONIC FLIGHTS UPON THE VERTICAL DISTRIBUTION OF OZONE

K. H. Grasnick

Meteorological Service of the GDR, Meteorological Main Observatory, Potsdam, German Democratic Republic

Ozone sonde ascents with an eiectro-chemical ozone

sonde have at several occasions shown an anomallv sh.irp divi'i'asi1

of the ozone partial pressure between 16 and 22 km. This decrease'

occurred when at the same time there was supersonic air traffic in

that height region. To find out whether the ozone decrease is

caused by photochemical reactions with the aircraft exhaust gases

(NO compounds) or by a direct pollution of the ozone sonde,

systematic investigations are being made at present. For these

investigations optical ground-based ozone measuring instruments

are also included. In this paper the author reports on the results

so far obtained. UAPRC-12-4 THEORETICAL MODELS OF MINOR CONSTITUENTS' DISTRIBUTE IN THE STRATOSPHERE AND THE IMPACTS OF THE SST EXHAUST GASES

Tatsuo Shimazaki and Toshihiro Ogawa

Environmental Research Laboratories, National Oceanic and Atmospheric Administration, Boulder, Colorado, U.S.A.

Comprehensive theoretical models are being developed for the distributions of the densities of minor neutral constituents in the stratosphere, including the effects of photolyses and chemical reactions important to the ozone density and the dynamical effects by eddy diffusion and meridional circulation. Which chemical reactions are most important in reducing the stratospheric ozone density depends upon the adopted chemical reaction scheme and reaction coefficients, but regardless of what reactions caused It, if such ozone loss occurs in the dynamics dominated regions, the net loss of the ozone density is much reduced; the transports of ozone from its source regions tend to compensate partially what was lost by chemical reactions. Thus, the overall effects of the SST exhaust gases on the ozone density may greatly be reduced, if they are emitted in the lower stratosphere, where the dynamical effects are dominated over the chemical effects. In the source regions, where the chemistry is dominated, the ozone density is well maintained at the magnitude of photochemical equillbrlur which should not be affected by the SST exhaust gases, unless the exhaust gases are emitted right into the source regions or they are transported into that region to a large extent. These effects are discussed in some detail based on the results of our model calculations UAPRC-12-5 SPATIAL DISTRIBUTION OF MINOR CONSTITUENTS IN THE TROPOSPHERE AND STRATOSPHERE, STUDIED IN PHOTOCHEMICAL MODELS WITH TRANSPORT

Eigil Hesstvedt

Institute of Geophysics, University of Oslo, Blindern, Norway

A two-dimensional photochemical model with a

parameterized transport is presented. Distributions of minor

constituents are computed. In particular nitrogen oxides are studied and the effect of pollutants emitted from high-flying aircraft

is evaluated. In the troposphere one-dimensional models are computed for different latitudes and seasons. In particular the distribution of OH is studied and its effect on other constituents, such as CO is discussed. UAPRC-12-6 NUMERICAL MODEL OF THE GLOBAL OZONE TRANSPORT IN THE STRATOSPHERE

I. L. Karol

Institute of Experimental Meteorology, Obninsk, Kaluga Region, U. S. S. R.

The numerical model of the global zonally averaged

atmospheric transport by the macroturbulent diffusion and

meridional circulation up to 25 km level, which has been (1) elaborated on previously , Js extended to the 35-40 km level

using the published wind data for the middle stratosphere. The

zonally averaged monthly mean ozone concentration distributions

in the stratosphere are calculated taking Into account the photo-

chemistry of atomic oxygen and ozone and their reactions with the

nitrogen and hydrogen oxides. The different reaction rates and

concentration distributions of these oxides are considered.

The comparison of calculated ozone concentration and

published ozone data allows us to estimate global concentration

distributions of nitrogen oxides and photochemical reaction rates.

It makes possible also the determination of relative roles of photochemistry and stratospheric motions in the formation of the ozone global content distribution.

(1) See Karol, I. L. "Radioactive Isotopes and global transport in the atmosphere11. Gldrometeoizdat, Leningrad, 1972. UAPRC-13-1 PLANETARY DISTRIBUTIONS OF Pb - 210 AND Po - 210 CONTENT IN THE LOWER STRATOSPHERE AND THEIR USE FOR THE ESTIMATION OF TRANSPORT PARAMETERS

UAPRC-13 I.L. Karol Institute of Experimental Meteorology, Obninsk, Kaluga Region, U. S. S. R.

H The published results of aircraft measurements of radio- 'h 210 210 Sf active isotope Pb and Po concentration in the stratosphere "% over the western hemisphere up to 20 km level in 1967-1971 are f systematized and analyzed. The study of their seasonal and k latitudinal variations at different levels makes it possible to • i f estimate the effective "age" of stratospheric aerosols and to find out that tropospheric air enters into the lower stratosphere mainly in summer in the northern temperate and tropical latitudes. The interannual variation of stratosphere-troposphere exchange intensity in the northern hemisphere is considered as based on the "age" of stratospheric aerosols. This exchange intensity variation leads to the variation of stratospheric sulphate aerosol content according to the measurements in the northern temperate latitudes in 1960-1971. presentedTh foer methomeand seasona of estimatiol parametern is suggestes of verticad andl resulttranspors aret in the nonortherr n temperate latitudes based on the mentioned Pb and 210

aerosol transporc in the oiver s trato^p.^e -«?, AP O- -VI.-- ->ee.i elaborated on previously (see Karol, I.L. "Radioactive isotopes and global transport ]^, the atr~osp' e' e" . G ' c%o"re--t'i'- z-;it, .'/iV 1972). UAPRC-13-2 CLIMATE STUDIES USING A ZONAL ATMOSPHERIC MODEL

Michael C. MacCracken

Lawrence Livermore Laboratory, University of Cal ifornia, Livermore, California, U.S.A.

The second generation zonal atmospheric model ZAM2 is being developed and applied to studies of the potential climatic impact of stratospheric injection of trace species by high altitude aircraft. The^jnodel is a two-dimensional general circulation model using a 5 latitude grid at nine pressure levels extending into the stratosphere. The effect of. terms lost by zonal averaging is simulated by introduction of an eddy transport mechanism In which the eddy diffusion coefficient is a function of internal model variables. ZAM2 strives to model the thermodynamics and hydrology of a moist atmosphere under the Influence of solar and long wave radiation, and includes precipitation, cloudiness, convection and surface interactions. The planetary surface is represented as fractionally divided at each latitude band between open ocean, sea ice, and land which may have mountains of various heights. A surface energy balance is maintained allowing heat storage in the land, the build-up and decay of snow cover, and the growth and met tin of sea ice. The model uses a fifteen minute time step and may be run for several years without severe penalties in computation time.

Model validation includes comparison with climatic data and other modeling efforts as well as sensitivity studies of various of the modeled processes. Application of this model to the Climatic Impact Assessment Program involves studying the effects of injection of aerosols, reduction in stratospheric ozone heating, and possible perturbations resulting from water vapor injection. Preliminary results of some of these studies are discussed. '"if, UAPRC-13-3

ON THE ESTIMATION OF GLOBAL AIR POLLUTION AND ITS TENDENCY

M. E. Berlyand

Main Geophysical Observatory, Leningrad, U. S. S. R.

The analysis of available observational material allows one to establish some regularities of the macro-scale pollutant distribution in the atmosphere. One of the main peculiarities of this distribution is that air pollution in cities and industrial centers is rather substantial, and the concentration of pollutants decreases rapidly with increasing distance from them.

For the estimation of global air pollution tendency, which is necessary, for example, to investigate meteorological regime and climate changes, it seems efficient to determine total pollution concentration in a vertical air column. Such an integrated aerosol concentration's characteristic can be obtained using solar radiation data from the actinometric observational network. Atmospheric turbidity was estimated for a long time by either direct of scattered solar radiation flows. These flows are usually analysed by formulae containing only one parameter for radiation attenuation and permit no distinction between the influences of anthropogenic and natural factors. It seems more promising to take direct and scattered radiation into account simultaneously. For this purpose a theoretical model of atmospheric radiation transfer is developed, allowing the estimation of the two components of optical thickness resulting from radiation scattering and absorption. It became possible to make some conclusions on the tendency of the two components over the last ten years, using observational data from the USSR actinometric network.

There are considerable future possibilities in global air pollution determination connected with the organization of WMO regional stations for pollutant concentration measurement. Special attention when developing such a network should be paid to the measurements of integrated air pollution characteristics, simultaneous observations at regional stations and neighbouring cities to estimate local effects, and developing methods of analysis of observational data. UAPRC-13-4

INTERACTION OF RADIATION AND ATMOSPHERIC CIRCULATIONS

Richard A. Craig

Florida State University, Tallahasee, Florida, U.S.A.

According to simple considerations based on the radiative

relaxation time for temperature perturbations, radiation is not apt to

play an important role for transient phenomena in the troposphere with

periods less than 10 days. In the stratosphere and mesosphere, as

the fraction of thermally-active molecules (COO) remains constant and

the mean free path of the radiation Increases upward, damping by

infrared radiation becomes Increasingly important for disturbances of

shorter period.

There are two important complications that we do not

adequately understand. In the troposphere, clouds significantly

alter both the solar and terrestrial radiation fields and their positions

are affected by the circulation. This gives rise to the possibility of

feed-back mechanisms that may be Important on shorter time scales In

certain situations. In the upper atmosphere certain temperature-

dependent chemical reactions affect the formation of ozone and

therefore the absorption of solar radiation. Quantitative studies of

this effect are hampered by current uncertainties about the rate coefficients and abundances of trace constituents.

Incorporation of radiative effects in various models are reviewed in the light of these considerations. |

Hartmut Grass I

Institut fur Meteorologie, University Mainz, Germany

In 1973 four different types of absorption in the window region could be separated from own sky emission measurements with the use of statistical evaluation. The three continuum - like absorption types listed following their importance in mid- latitudes are: the so-called e-type absorption depending on water vapor pressure besides water vapor mass, the absorption by aerosol particles and the absorption by wings of distant strong water vapor lines, formerly regarded as the main source of continuum absorption in the window region from 8-13 micrometer. The fourth absorption is due to lines of water vapor and carbon dioxide within the window.

These absorption coefficients were incorporated in cooling rate calculations showing the great influence of the so- called e-type absorption in tropical regions on cooiing rates and on surface temperatures derived from satellite data. The differences between calculated and measured profiles of cooling>rates could be considerably reduced in the lower troposphere introducing the new absorption coefficients. Until now it is not clear whether the e-type absorption is due to self-broadening of water vapor lines or to a more complex molecule including at least one water vapor molecule. UAPRC-U-1 I THE EFFECT OF SIMPLIFIED PHOTOCHEMICAL. | '^MODELS ON CALCULATED EQUILIBRIA AND COOLING RATES t JN THE STRATOSPHERE AND MESOSPHERE UAPROI4 Donna Blake, Department of Meteorology, Florida State University, Tallahassee, Florida, U.S.A.

and

RichardS. Lindzen, Division of Engineering & Applied Physics, Cambridge, Massachusetts, U.S.A.

A scheme is developed which utilizes simplified models for the ozone photochemistry and the heating and cooling processes in the region 22-80 km. The scheme, which is suitable for incorporation into dynamical models of this region, jointly determines temperature and composition. Nitrogen and hydrogen reactions can be included in addition to pure oxygen reactions.

It is shown that joint radiative-photochemical equilibrium calculations of temperature and composition should be valid for the mean state of the atmosphere between 35 and 65 km. Since many parameters are uncertain in this height range, a wide variety of mixing ratios, cooling rates and reaction rates are used. The equilibrium calculations indicate that hydrogen reactions significantly alter the ozone and temperature distributions above 40 km while nitrogen reactions are important below 50 km. Comparisons of equilibrium distributions of ozone and temperature with those observed indicate that at the stratopause the water vapor mixing ratio is 6 8 1-5 x 10~ and the (NO + NO2) mixing ratio is 3-10 x 10~ . The latter is about 3 x 10 at 35 km. Obviously these values for the mixing ratios depend on the reaction rates and cooling rate coefficients used. However, the scheme is so simple that the effect of any new rate can be readily found.

The scheme is also used to calculate the relaxation of perturbations from joint radiative-photochemical equilibrium. For all cases studied, the inclusion of the temperature dependent photochemistry reduces the thermal relaxation time scale above 30 km from that found for purely radiative cooling. The time scale for the latter is 10 days at 35 km and 5 days at 50 km. When the photochemistry is included the thermal relaxation time scale is 3-7 days at 35 km and 1. 5-2.5 days at 50 km. This reduced time scale increases the dissipation for waves traveling in the stratosphere.

J UAPRC- 1 4- THE EFFECT OF RADIATIVE EQUILIBRIUM ON THE STRATOSPHERIC HADLEY CIRCULATION

Takashi Sasamori

National Center for Atmospheric Research*, Boulder, Colorado, U.S.A.

Based on numerical simulation of the atmospheric general ;, circulation conducted at the National Center for Atmospheric Research, (f together with the observed circulation in the stratosphere, the dynamicah similarity of the circulations of the stratosphere and troposphere is j discussed in terms of the internal and external parameters of the \ atmosphere. The Hadley circulation in the low latitudes and the I zonal circulation in the high latitudes are essential features common {; to both the stratosphere and troposphere. The difference In the .] latitudinal span of the Hadley cell in the individual regions is shown ^ to be primarily due to the different vertical static stabilities. Since 4 the vertical static stability of the stratosphere is maintained by a ij condition of radiative equilibrium, radiative processes are Important fi where the stratospheric jet stream has its maximum intensity. •;

*The National Center for Atmospheric Research is sponsored by the National Science Foundation. ,f UAPRC-14-3

THE INTERACTION OF RADIATION AND THE J MERIDIONAL CIRCULATION IN THE STRATOSPHERE

Jean-Francois Louis, National Center for Atmospheric Research and Department of Astro-Geophysics, University of Colorado, Boulder, Colorado, U.S.A.

Julius London, Department of Astro-Geophysics, University of Colorado, Boulder, Colorado, U.S.A.

Edwin F. Danielson, National Center for Atmospheric Research*, Boulder, Colorado, U. S. A.

A two-dimensional, seasonal model of the stratosphere is developed based on initial assumed temperature field and subsequent mutual adjustment of the temperature and zonal wind fields through the thermal wind relation for a spherical earth. Both fields are in good agreement with observations.

This model atmosphere is used to compute the cooling rate due to the IS band of carbon dioxide and the BO^band of water vapor. These cooling rates are then combined with the cooling rate of the 9.6*t- band of ozone (Kuhn and London; Kennedy) and the heating rate due to the absorption of solar radiation by O and O (Park), in order to estimate the radiation budget in the stratosphere.

The net heating rate obtained is then introduced as a forcing term Into the thermodynamic equation which is solved together with the continuity equation to compute the meridional circulation in the stratosphere. The weekly high altitude ESSA charts were used to estimate the horizontal eddy heat flux above the regions documented by Newell. The vertical eddy heat flux was neglected.

At the solstice the circulation in the stratosphere is dominated by a large mean meridional cell which transports tracers from the summer to the winter hemisphere at high altitude (above 35 km). Another, weaker cell is also apparent in the summer hemisphere in the lower stratosphere. At the equinox, the circulation is much weaker, and more symmetrical.

*The National Center for Atmospheric Research is sponsored by the National Science Foundation. UAPRC-14-4 A TIME DEPENDENT TWO-DIMENSIONAL MODEL. OF THE ATMOSPHERE BELOW 80 KM

R. S. Harwood and J. A. Pyle

Department of Atmospheric Physics, Oxford University, U.K.

The purpose of the model is the study of the interaction of dynamics, photochemistry and radiation In the stratosphere and mesosphere. The dependent variables are zonal means of the relevant meteorological quantities, held as functions of time, latitude and height (-log pressure) with a resolution of 10 degrees latitude and 0. 5 pressure scale height.

Eddy fluxes of heat and matter are treated by large-scale diffusion coefficients. This treatment is not applicable to the momentum flux; accordingly a novel technique suggested by Green (1970) is used in which the momentum flux divergence is obtained indirectly from the fluxes of heat and potential vorticity for which diffusion coefficients are more satisfactory.

Radiative coolings due to CO. and O, emission are computed from simplified expressions which are essentially cooling- to-space approximations with emissivitfes obtained by curve-fitting against the results of more elaborate treatments. Absorption of solar radiation by ozone is obtained from tabulations of absorption against ozone amount traversed. Radiation and latent heat release in the troposphere are specified climatologicalfy.

The photochemistry currently modelled is the classical ozone scheme but work is In progress on the inclusion of reactions involving nitrogen and hydrogen compounds. This will allow the investigation of possible stratospheric pollution problems.

Reference Green, J. S. A. 1970. Transfer properties of the large scale eddies and the general circulation of the atmosphere. Quart. J. R. Met. Soc. 96, pp. 157-185. •.;•.-•;.• UAPRC-15-1

.DETAILED AND PARAMETERIZED MODELS OF LONG-WAVE RADIATIVE TRANSFER IN THE TROPOSPHERE, STRATOSPHERE .••;* AND MESOSPHERE UAPRC-15

S. F. Woronko

Atmospheric Environment Service, Toronto, Canada

A program to compute atmospheric infrared fluxes and heating rates has been developed. Absorption by water vapour, carbon dioxide, and ozone is calculated by numerical integrations ofVoigt line profiles using statistical band model formulations. This technique allows the height integration to be performed before (he frequency integration, with the advantage that non-homogeneous paths can be treated more accurately than with scaling approximations. This advantage Is Important in the calculation of ozone heating rates especially. Clouds and aerosols are treated as continuum absorbers.

The above model has been used to derive an efficient parameterized model. This parameterization takes into account the statistically dominant features of the absorber (vertical) profiles in the atmosphere. The fluxes and cooling rates are calculated from the temperatures and from the coefficients of the empirical orthogonal expansions of the profiles. The method is most efficient when used with profiles that have a lower information content, such as those derived from satellite observations. UAPRC-15-2 A STUDY OF THE EFFECT OF STRATOSPHERIC AEROSOLS PRODUCED BY SST EMISSIONS ON THE ALBEDO AND CLIMATE OF THE EARTH

James B, Pollack, Space Science Division, NASA Ames Research Centre, Moffett Field, California, U.S.A.

and

Owen B. Toon, Laboratory for Planetary Studies, Cornell University, Ithaca, New York, U.S.A.

SSTs will contribute to the aerosol content of the stratosphere, principally through the conversion of sulfur gases to the sulfuric acid particles. Using recently derived optical constants for sulfuric acid, we have applied a combination of Mie scattering theory and a modified two-stream approximation to calculate the change in the overall albedo of the Earth and the Stratospheric heating rate as a function of the change In the optical depth of the stratospheric sulfate layer. We have also estimated the effect of these aerosols at thermal wavelengths by computing their optical depth as a function of wavelength." Because of the small size of the aerosols, their principal effect on the heat balance of the Earth is to cause a change of the Earth's albedo.

We have also made a first order estimate of the change in the Earth's surface temperature implied by the above albedo variations by using a non-gray radiative-convective model. This model allows for variations in the optical depth of tropospherlc clouds, but does not include feedback effects arising from changes in the extend of the polar ice deposits.

The above changes in the Earth's albedo may significantly influence the atmospheric circulation. Though we have not included these effects at this stage of our calculations, they can directly be applied to this area. MPR-E-1 ;; THE OIURNAL WIND VARIATION ABOVE THE INNER PARTS OF ICE SHEETS MPR-I

F. Loew?

University of Melbourne, Melbourne, Australia

In the interior of the big ice sheets of Greenland and Antarctica the prevailing downhill wind has in summer frequently the highest speed near midday. From the stronger development of the cold air layer near the surface during the night a nightly wind maximum might be expected as is actually found near the border of the ice sheet. But in the interior the slope is small, the surface wind is weak and can be speeded up by a stronger wind in the free atmosphere above the ground layer if this upper wind has a sufficiently strong component in the direction of the surface wind. Owing to the big diurnal variation of temperature in the ground layer the stability near the ground is diminished during the midday hours. This leads to a more effective speeding up around midday and results in a wind maximum at that time of the day. Several of the stations in the inner parts of ice sheets have indeed an appropriate relation of upper and slope wind.

Sometimes the wind maximum near midday can be explained by the combination of the upper geostrophic wind and the "thermal wind" caused by the inclined cold air layer near the ground. The latter varies in strength with the diurnal change In the size of the temperature inversion, and if certain relations exist between the upper wind vector and the strength and direction of the thermal wind during day and night, a midday maximum of the geostrophic surface wind and hence of the actual wind near the surface can result. An expression is derived for the necessary relation between the upper geostrophic wind and the thermal wind. MPR-I-2 THE INTERACTION BETWEEN TURBULENT FLUX AND THE SURFACE COVERED WITH MOVING OBSTACLES

h., K. By utner

U. S. S. R.

In a large number of experiments performed in recent years on the relation butween heat exchange coefficients and resistance in tubes covered with roughnesses of various sizes and shapes it was "establ ished that the ratio between these coefficients is not unity but is a decreasing function of the Reynolds number of the roughness. This fact is also corroborated by measurements under natural conditions. Its physical explanation is that the heat exchange process is mainly connected with the forces of tangent friction against the surface. The transfer of surface impulse at the expense of the horizontal component of normal pressure force has no analog in the processes of heat-mass transfer. A simplified model of the interaction between turbulent air flow and surface covered with moving obstacles is suggested in the paper. The boundary conditions at the surface include the presence of tangent friction forces and the adjacent visco-buffer layer, the thickness of which depends on the aerodynamic properties of obstacles and the density of their arrangement. An additional turbulization of air flow caused by the presence of obstacles leads to the change of heat resistance in the near-surface layer. The dependence of heat resistance value on the height, form, and velocity of motion of the obstacles has been studied. Estimates of the value of the ratio between coefficients of heat exchange and of resistance have been obtained for different sea surface conditions. In order to extend these estimates to storm conditions, further ^ studies on the sea surface structure are necessary during storms. However, under storm conditions heat and moisture exchange with * spray, thoroughly studied in the works by R. S. Bortkovsky, seems to be a prevailing process. MPR-I-3 CONTRIBUTION OF FORM DRAG ON PRESSURE RIDGES TO THE AIR STRESS ON ARCTIC ICE MPR-I

S. P. S. Arya

Department of Atmospheric Sciences, University of Washington, Seattle, Washington, U.S.A.

The wind force on a large floe of pack ice consists of skin friction drag on much of the level surface and form drag on hummocks and pressure ridges. The latter has been ignored in air stress determinations to date. It is argued that the profile and eddy correlation techniques of measuring stress have only local validity and cannot take into account the form drag on large scale topographical features. A more suitable method of determining the wind stress over large time and space scales is the so-called geostroF^ic drag method. A basic difficulty in applying this method to the Arctic pack ice, however, is that there is at present no practical way of measuring the large scale surface roughness characterizing all the topographical features.

An expression is derived for the form drag per unit area in terms of certain key parameters of the pressure ridge statistics and a suitable drag coefficient. Using the available field and laboratory measurements of these parameters, an estimate is made of the ratio of the form drag per unit area to the fractional stress. It depends on the intensity of pressure ridging, and on the meteorological conditions in the surface layer. The results show that the form drag on pressure ridges is generally greater than the skin friction drag on tho level ice surface, especially in stably stratified conditions.

Finally, some recommendations are made for better determination of the wind stress. The most uncertain parameter in the present calculations is the form drag coefficient which depends on the ridge profile. Many more observations of actual profiles are required to determine an average shape for each class of pressure ridges. Then, geometrically similar models should be tested in simulated wind tunnel flows for the purpose of determining their drag coefficients. MPR-I-4 AIR STRESS ACQUISITION AND EVALUATION OVER THE ARCTIC OCEAN

R. A. Brown

Arctic Ice Dynamics Joint Experinent, University of Washington, Seattle, U.S.A.

The AIDJEX Project is investigating the dynamics of ice motion on the Arctic Ocean. A good parameterization of air stress is essential to this analysis. Toward this goal, AIDJEX obtained one month's meteorological data on the ice in 1972. The evaluation of this data, plus other similar data, is used to determine the plan for data acquisition and evaluation in the forthcoming year- long AIDJEX Field Study. MPR-I-5

SNOW TRANSPORT AND WINTER PRECIPITATION f IN THE POLAR REGIONS N. N. Brynzgin and L.S. Petrov

The Arctic and Antarctic Research Institute, Leningrad, U. S. S. R.

In the polar regions precipitation mainly in solid form i occurs almost all year round. The techniques of precipitation measurements are known to be insufficiently accurate, and quantitative data obtained are unreliable. Some countries have stopped the publication of the data on precipitation amounts as they are considered to be erroneous (for example, Denmark from the Greenland area, Japan and Australia from Antarctica).

All precipitation gauges being used at present show large errors which should be taken into account in the estimation of real precipitation amount. Tretyakov's precipitation gauge used at the Soviet Arctic and Antarctic stations has four sources of errors due to: (1) wetting of the receiver walls, (2) evaporation from the gauge, (3) precipitation loss due to the wind action (in absence of snow drifting), (4) accumulation of snow lifted from the ground in the gauge while snow drifting. The values of the former two errors have been accurately estimated and used for correction of precipitation data, obtained by gauges. The latter have required special studies of snow transport and precipitation at various levels to be made in the Arctic and Antarctic.

The error due to the wind action with the wind speed being less than 8 m/sec (no snow drifting) has been determined from the data on precipitation measurements made at 1, 2 and 10 m levels. The value of the reference precipitation intensity has been analitically determined by the ratio of the soiid precipitation measurements at three levels to the wind speed. The ratio of the reference value to the precipitation intensity measured at the gauge level at any wind speed is a correction coefficient for the loss due to the wind action.

The data on snow transport intensity measured by the snow gauge of "Cyclone" type at 1, 2 and 6 m levels have been used to establish the dependence of snow particle concentration in snow drifting and snow drifting with snow fall on the wind speed and height. These dependences are approximated by the empirical formulae:

C = 5.9.10"1** U2'"9 : C = 2.8.10"3 • U2'15 ; Mw «r u • urn *

The height of the drifting snow is determined by the first formula, the second is used for the estimation of concentration of the snow transport free of deflation.

The ratio of the estimated value of concentration to the value obtained at 2 m level while drifting of the snow with snowfall Is a correction coefficient to snow accumulation in the gauge. Measured values of total precipitation corrected by means of these coefficients have shown good correlation with other elements of the water budget.

f •4 i MPR-I-6

'it VARIATIONS IN ANTARCTIC SEA ICE AND TEMPERATURE

W.F. Budd

Antarctic Division, Department of Science, Melbourne, Australia

An analysis of long term records at Laurie Island reveals a strong correlation between variations in the annual mean lemperaturi- and the duration of the sea ice, such thai a change of 1 C in the annual mean temperature corresponds to about 70 days variation in the duration of the sea ice.

Variations in sea ice duration with latitude around the Antarctic provide a relation between the duration and the mean maximum latitudinal extent of the sea ice.

Combining these results gives a relation between variations of annual mean temperature and the mean extent of the sea ice, viz. a 1 C change corresponds to approximately 2. 5 Lat. variation in the maximum sea ice extent. For larger temperature variations however this factor decreases, which suggests that the interaction between sea ice extent and temperature is stable rather than unstable. Records of ice extent and temperatures over a much shorter period for the region between Iceland and Greenland show a similar but weaker correlation.

General relations between annual mean temperature, freezing degree days, sea ice thickness, and latitude allow an estimate to be made of how the thickness of the sea ice around the Antarctic varies with time through the year.

An analysis of records of annual mean temperatures around Antarctica shows large scale anomalies of thousands of kilometers, extent with considerable variation from one year to another.

From 1967 on satellite photographs are available which show considerable variation in the sea ice extent in different years. These differences seem to persist consistently over entire seasons.

In general there seems to be considerable association between the regions around the Antarctic with the coldest temperatures and the regions of greatest sea ice extent. These results confirm that large scale variations in sea ice extent and surface mean temperatures are related and persist over the time scale of seasons or greater.

Measurements of heat budget over sea ice and ocean water throughout the year near Mawson are used with other data to estimate the effect of the variations in sea ice extent on the heat budget of the southern hemisphere throughout the year and from year to year. MPR-1-7 A STUDY OF HEAT BUDGETS OVER SEA-ICE AND WATER NEAR MAWSON ANTARCTICA

Ian Al lison

Antarctic Division, Department of Science, Melbourne, Australia

During 1969 a micrometeorological study was carried

out for nine months continuously over an Antarctic annual sea-ice

cover near Mawson. Profile and radiation measurements were

made over open watt,' before the ice formed, during the formation

and growth of the ice cover and during the early part of the decay

before the eventual break-up of the sea-ice.

The energy budget terms are evaluated and presented

for mean ten day periods throughout-the year. Comparison of the

energy budget during the different stages of the ice history shows

in particular the large differences in energy transfers for open

water and an ice cover. The sea-ice cover, acting as a reflector of radiation and as a physical barrier to the underlying water cuts

the various heat transfers by almost an order of magnitude.

The growth of the ice cover and the annual heat budget are compared and contrasted with the results of a similar micro- meteorological study made at the same site, but for a shorter period, in 1965. In addition the climatic factors affecting the formation and growth of sea-ice at Mawson are discussed. M MPR-I-8 MPR-I-9

THE COMBINED HEAT-, ICE-, AND WATER-BALANCE OF McCALL GLACIER, ALASKA

G. Wendler and N. Ishikawa

University of Alaska, Fairbanks, Alaska

McCall Glacier lies in the eastern part of the Brooks Range, in the Romanzof Mountains, at latitude 69 18'N, longitude 143 48'W. The glacier has an area of 6. 22 km and an altitude span from 1340 to 2720 meters. It Is one of the few small glaciers which exist in the low precipitation environment of the Brooks Range at altitudes above 5 000 meters. A combined heat-, ice-, water- batance was conducted under the auspices of the International Hydrologica"! Decade (IHD) from 1969-1972. McCall Glacier is the only arctic glacier currently being studied in the United States of America, and is of special importance as it lies at the inter- section of two glacier "chains" recommended for intensive study in the IHD: the Arctic Circle and the American chains.

In this paper, the combined heat-, ice-, and water- balance is discussed for a 36-day period of good observational data in summer 1971. To the authors* knowledge it is the first time that such an estimate for a whole glacier basin has been attempted. Previously, only comparison of ice- and water- balances have been carried out with various degrees of agreement, depending on the accuracy of the measurements and the liquid storage capacity of the glacier.

The ice balance was measured in the conventional way with 54 ablation stakes and pit studies. A complication was the refreezing of the meit water at deeper layers in the firn basin which amounted to about 80%. This amount was estimated using temperature profile measurements at different points in the firn basin. To determine the precipitation in the basin, seven precipitation stations were established and the evaporation was estimated. for a short term heat balance study, which was carried out o\/er a moraine surface.

The water balance was calculated, using discharge measurements on the McCall Creek, where the stream level was recorded and calibrated with a current meter. The most difficult pant was to determine the heat balance for the whole glacier surface. Our main station was over ice, and it was assumed that this value was valid for the whole ice surface. Another second class station was over snow, which was assumed to be correct for all snow surfaces. The radiative fluxes were corrected for slope. The glacier receives 1.7% less direct solar radiation than a horizontal surface during the short ablation period owing to its northerly exposure. The screening affect of the mountains is more important and for the same period results in a loss of 39. 9% in time or 13. 4% in energy as compared with the horizontal. The albedo of the snow was measured, and using temperature measurements, the outgoing long wave radiation was I corrected for the mean height of the glacier. Using the three methods, the following values were found for the run off of the 36-day period, 6 3 measured 2. 67 x 10 m

b) calculated from ice balance 2. 28 x 10 m

c) calculated from heat balance 2. 90 x 10 m

which shows a disagreement of -14.6% and+8. 6% respectively, which can be considered as satisfactory for a study of this kind. MPR-II-1 THE RADIATION BALANCE OF THE EARTH-ATMOSPHERE SYSTEM OVER BOTH POLAR REGIONS FROM MEASUREMENTS OF THE SATELLITES NIMBUS 2 AND NIMBUS 3

MPR-11

Ehrhard Raschke

Universitat Koln, F. R. G.

Global measurements of reflected solar and emitted terrestrial radiation were obtained during the periods 16 May to 28 July 1966 from Nimbus 2 and 16 April to 15 August, 3-17 October 1969 and 21 January to 3 February 1970 from Nimbus 3. These data were used to compute spatial and temporal variations of the radiation balance and its components.

In this paper the results obtained over both polar regions between about 50 and 90 latitude are discussed in detail. They are mostly presented in maps of high (250 x 250 km per grid point) spatial resolution. Also, possible interannual variations as picked up by both satellites are considered.

It was found in particular, that the Arctic icefields over the entire year are considerably warmer than the higher elevated Antarctic areas. But both areas absorb almost equal amounts (0. 1 1-0. 15 cal cm min ) of solar radiation during a year. Thus, the resulting zonal energy gradienfbetween the tropics and both polar regions is larger over the northern than over the southern hemisphere. MPP-II-2 TRENDS IN SOLAR RADIATION, TEMPERATURE AND CLOUD AT SCOTT BASE, ANTARCTICA

Donald C. Thompson

New Zealand Meteorological Service, Wellington, New Zealand

Measurements of total solar radiation, temperature and cloud at Scott Base (77° 51'S, 166° 4B'E) since 1957 have been surrrrarized. In the first part of the paper the c!ear-sky radiation flux has been evaluated at times of fixed solar elevation angles of 10,15 and 20 , this procedure being chosen to eliminate certain instrumental errors. The results obtained show a sharp decrease in total (sun + sky) clear-sky solar radiation following the eruption of Mount Agung in 1963, and a gradual return to a new equilibrium value spread o\/er some 7-8 years. This recovery from the Agung eruption is less rapid than was previously thought to have occurred at high southern latitudes but is consistent with recent low-latitude Northern Hemisphere results. The new equilibrium value appears to be somewhat lower than the pre-Agung condition.

In the second part of the paper attention is turned to annual totals of solar radiation, for all days. Between 1958 and 1972 these totals show a downward trend of almost 9% per decade, which is not attributable to instrumental errors. O\/er the same period there is an upward trend in the annual mean temperature of about 1. 6 C per decade. These trends are probably associated with changes in the mean cloudiness, and a good negative correlation is observed between annual means of radiation and cloud. The cloud data are not, however, of uniform quality and further confirmation is sought and found in the relation between radiation and other cloud- dependent parameters such as the mean daily temperature range.

The interpretation of these trends in terms of changes in the circulation in the Ross Sea area is discussed.

1 MPR-1I-?

MAIN PARAMETERS OF THE COMPONENTS OF THE MOISTURE "3 TURNOVER IN THE POLAR REGIONS MPR-U

A.I. Voskresensky and L.P. Burova

The Arctic & Antarctic Research Institute, Leningrad, U. S. S. R.

Integral characteristics of the moisture content, moisture turnover coefficients in the polar atmosphere were studied. Upper- air data of 100 stations for the layers between the surface and 500 mb level for the period of 1956-1969 were analysed. Considering uneven distribution of stations in the studied areas (northward and southward of 65 parallels) the grid-point method was used.

Moisture content in Antarctica ranges throughout the year from 9. 66 ton in July to 36. 42 ton in January, with the mean annual value of 19. 32 ton. For the Arctic area this value is 60. 24 ton in January, 317. 18 ton in July and the mean annual value of 145. 14 ton. Comparing with Greenland Antarctic water vapour content is only one third of the Greenland value. The water vapour content in the atmosphere of the polar regions is known to be extremely small, in particular its value in Antarctica is two orders of magnitude less than over Sahara.

The field of the total annual moisture transfer over Antarctica is characterized by a well-marked zonal ity and large horizontal gradients directed toward the continent. The largest values are found at the southern boundary of the Ross and Amundsen seas (800 kg/m/s). At the continent high plateau it never exceeds 25 kg/m/s, being about 12 kg/m/s in the centre of the high plateau area.

The field of the total moisture transfer in the Arctic within the middle troposphere has a well-pronounced meridional ity. The largest horizontal gradients are found over the North Atlantic seas, where the total moisture content varies from 1350 kg/m/s at 65 N to 350 kg/m/s at the Greenland Coast. The Arctic Basin is characterized by a small gradient field with the value of moisture transfer ranging from 500 kg/m/s in the vicinity of the New Siberian Islands to 350 kg/m/s at the northern coast of Greenland. Over the mountain areas of East Siberia and Alaska there are two regions of typical small moisture transfer values. Annual coefficients of the moisture turnover In the Arctic show their large variability in certain areas (1. 04 - 1. 24) and this is attributed to a number of factors, governing the water vapour- content in the atmosphere, precipitation and evaporation. Quantitative estimates of advective and local precipitations were obtained. MPR-lt-8

MOVEMENT OF SEA ICE AND THE CONDITIONS OF THE ICE PACK IN THE BEAUFORT SEA

Gerd Wendler and K. O. l_. F. Jayaweera

Geophysical Institute, University of Alaska, Fairbanks, Alaska

Sea ice conditions of the Arctic Oceans are of great Interest scientifically, as they influence the climate, and practically for shipping and offshore activities. Land observations of the sea ice are not sufficiently far reaching and ship observations give only point measurements. Aircraft observations are good, but long-term aerial surveillance over an extensive area is extremely expensive. Hence, satellite measurements have been more and more used to observe and predict the ice conditions. However, these satellite measurements have several shortcomings. For many purposes, the resolution has been insufficient, and a grey scale, in which satellite data are normally available, are difficult to work with quantitatively.

ERTS I satellite, which was launched in summer of 1972, gives high resolution data (100m) in three visible and one near infrared band. The quality of these data is very good, and furthermore, they can be obtained in digital form on magnetic tape. At the latitude of northern Alaska the satellite has a four day overlap, and good quality data have been obtained. Instead, of using visible interpretation of these data, the CDU (Color Display Unit), built by Interpretation System Incorporated, Kansas, in connection with aVP-8 television display unit and the University of Alaska IBM 360/40 computer is utilized, to obtain the following three goals:

1) by density slicing the sea ice conditions can be determined 2) by deducting the images of the same band on successive days the ice movement can be determined. This is discussed as a function of the wind velocity and the ocean current. 3) by using ratio of different bands (visible and near infrared), it can be determined whether the surface is melting or non- melting, as the reflectivity in the near infrared drops drastically, when melting occurs. MPR-I1-4

OZONE VERTICAL DISTRIBUTION AND THE TROPOPAUSE STRUCTURE OVER ANTARCTICA

A. S. Alexandrov and G. U. Karimova

The Arctic & Antarctic Research Institute, Leningrad, U. S. S. R.

Ozone profiles over Antarctica were analysed together with their related thermal structures of the lower stratosphere and tropopause. The generally well-pronounced ozonepause over Antarctica is shown to locate on an average 0. 3 km lower than the tropopause boundary. In most cases {72 percent) the difference between the location of the tropopause and ozonepause do not exceed 0. 5 km. The ozonepause is below the tropopause in 53 percent of the cases, and it is above the tropopause in 20 percent of cases. In the Arctic the cases when the ozonepause locates above the tropopause are rare (4 percent), which is due to a strong effect of the downward air motion In the north polar area.

The largest differences of tropopause and ozonepause heights over Antarctica amounting to 2. 5-3. 2 km are found early in spring, when below the tropopause vertical temperature gradients drastically decrease. This can be attributed to the effect of the horizontal advectfon processes, common to the transitional seasons.

Sharp changes of vertical temperature gradients in the middle and upper troposphere seem to be a better indicator of the start of ozone concentration increase with height than the level of the lower boundary of the tropopause. This circumstance might explain considerable discrepancies in the estimations of the tropopause - ozonepause distance referred to by many authors.

Inland Antarctic stations indicate large variations of the ozonepause height at the time of the polar night. In Mary Byrd Land area abnormally low ozonepause (6. 5 km) was found in the presence of a double structure of the tropopause, simultaneously partial ozone pressure tends to increase with height immediately over the lower boundary of the first tropopause. The highest ozonepause over this area was found at a height of 12 km.

Since the annual course of the tropopause over Antarctica, contrary to the Arctic, is characterized by larger values in winter and lower ones in summer and considering the above mentioned relationships between the location of the tropopause and ozonepause, we may suggest that the increase of partial ozone pressure starts over Antarctica on an average at a height of 8. 2-8. 6 km in spring .mH .r. hinh .-V. o. 7-10. o k in winter. MPR-II-5 PECULIARITIES OF THE DISTRIBUTION OF ATMOSPHERIC PRESSURE, WIND SPEED AND THE STRUCTURE OF THE TROPOPAUSE IN THE ANTARCTIC

1_. A. Gavrilova and L. V. Dolganov

The Hydrometeorological Institute, Leningrad, U. S. S. R.

Seasonal low pressure centers are identified in the constructed many-yearly mean monthly atmospheric pressure maps covering inshore waters and the continent. The centers are situated over the Ross Sea (960-980 mb), over the Bellingshausen and Weddell seas and over the area of the stations Mawson-Davis {975 mb), over the areas of the stations Lazarev-Molodezhnaya and Wilkes (975-980.mb) and over the D'Urville Sea (975-985 mb). Pressure change at sea level from less than 925 mb up to 1005 mb in the areas of cyclone stagnation is responsible for the fact that the annual pressure amplitudes are 100 mb.

The areas of cyclone stagnation are characteristic of especially heavy winds, their annual wind speed being higher than 15 m/sec and maxima are higher than 60 m/sec.

The lowest of the maximum wind speeds (25 m/sec) are typical of East Antarctica. Slightly higher than 25 m/sec values of maximum speeds are typical of West Antarctica.

General conclusions on storm winds of the Antarctic coast are obtained from analytical considerations of katabatic winds, the pressure gradient being taken into account.

The existence of an intense cyclonic activity over the inshore waters of the Antarctic evidences of the intralatitudional exchange which occurs not only in the lower troposphere but also in the upper troposphere. This exchange is responsible for the corresponding structure of the tropopause. The multi-layered tropopause caused by the flow of warm air masses can be observed in any area of Antarctica independently of the season of the year. The double tropopause—the lower Antarctic one (8-9 km) and the upper one of the moderate latitudes (12-14 km)—has the highest recurrence in August. At Mirny Station the recurrence amounts to 42%, at Novolazarevskaya Station - to 23%, at McMurdo Station - to 19%, while at Vostok Station it amounts to only 5%.

This type of the tropopause is associated with the passage of high intense warm fronts or occlusion fronts occurring within the entire troposphere and well seen in the temperature and wind field. In some cases the wind speed in jet streams was »v,: y$ ' MPR-IT-6 ON THE VERTICAL EXTENT OF THE POLAR CYCLONE AND ANTICYCLONE

S. S. Gaigerov, 8. P. Zaichikov, M. Ya. Kalihman and V. V. Fedorov,

Central Aerological Observatory, Leningrad, U. S. S. R.

Circumpolar vortices in the upper stratosphere are .n general located in the stratosphere and mesosphere. Preliminary mean 0. 1 mb contour charts compiled for January and July for the northern hemisphere reveal that the winter cyclonic vortex and the summer anticyclone can be traced up at least to 60-70 km.

The polar cyclone dominated the circulation of the stratosphere and lower mesosphere during most of the year. The analysis of rocket data obtained at Molodezhnaya station in Antarctica points out that cyclonic circulation no longer prevails •"'»? j in the upper mesosphere. On the contrary, easterly winds have been observed at these levels for most of the yeer.

The mean 0. 001 mb northern hemisphere contour chart for January based on both rocket and meteor data shows that the polar cyclonic vortex is well marked in mid-winter at the height of 90 km. Data obtained at Molodezhnaya point out that in spite of general stability of the winter vortex, considerable variations of wind speed take place even in mid-winter in the upper mesosphere. This fact enables us to suppose the possibility of changing the cyclonic circulation in this layer to the anticyclonic wind regime. MPR-JI-7 f

SOME PARTICULAR FEATURES OF THE ATMOSPHERIC *'• CIRCULATION OVER ANTARCTIC AND NAVIGATION OF AIRCRAFTS £

P. Astapenko and K. Bezvikonniy

U. S.S. R.

Various atmospheric situations are observed in the pre- surface layer of the Antarctic atmosphere. The situations should be attributed to the influence of orography and peculiarities of the underlaying surface. The wind regime was studied during expedition flights in 1972-1973 over the Land Enderby, in the region of meteorological station MoJodejnaya and over Lambert glacier in Prince Charles mtns. The studies enabled the determination of the range of favorable flight regimes with regard to the wind and persfstance of meteorological conditions. The katabatic winds appeared to be the determining factor during most of the year. In summer, the gradient wind together with the transition of baric systems becomes dominant.

For each geographical region there exists a critical wind speed above which the possibility of flights operations are excluded. Other meteorological parameters are not important since a super- critical wind causes heavy blowing snow and a white-out.

For the region of Molodejnaya the critical wind equals 1 it m/sec. :

In a numerical climatological model of wind charge for j the runway used at the airport of the expeditions, the above "; mentioned features of the seasonal wind regime should be taken into S consideration. , H-K US-I-1 1 A STUDY OF HIGH LATITUDE JET STREAMS IN <: THE SOUTHERN HEMISPHERE • • U S -1 't' T.T. Gibson - ) Meteorology Department, University of Melbourne, Parkville, Victoria, Australia

f Though the jet streams of the southern hemisphere are

I"-:- s undoubtedly important features of the atmosphere's general circulation, details of their structure and behaviour are still largely • unknown, even in a basic climatological sense. And most of the published material refers to the sub-tropical jet stream (STJ), and leaves the question of the extra-tropical jet streams (ETJ's) open.

ThJs study represents an attempt to describe some of the climatological characteristics of southern hemisphere ETJ's, [•.:-'v using data from the best available series of hemispheric upper- \'.•>;-. level analyses - the 500 mb analyses prepared by the South African \,j' Weather Bureau for the IGY period.

j,;'• The work is essentially an extension of earlier studies : f* by Berggren and by Mclntyre for the northern hemisphere. Frequency j I distributions of 500 mb wind speeds for given values of 500 mb £% ' temperature were constructed for two three-month periods pi (representative of summer and winter conditions). On those (>;,* occasions when temperatures, but not winds, were observed, a jjj geostrophic wind speed (read manually from the analysed contour f* pattern) was used in place of an observed wind speed. In view \':i\ of the consistently high quality of the South African analyses, \r- this procedure should not lead to significant errors. 1 „ [J. I he results indicate the existence of 3 separate ETJ &*• axes (at the 500 mb level) for both the summer and the winter |bv- seasons. Typical values of associated 500 mb temperatures (and p^ inferred thicknesses) will be presented, and their seasonal ? Ift > " variation will be discussed. ?'. The existence of 3 separate ETJ's throughout the year is t given further support by a study of NIMBUS A THIR 6. 7>t- m data f ' for the Austral ian region. Time-sections (for given longitudes) |r were constructed for the winter of 1970 and the summer of 1971, jp showing jet-axis latitudes inferred from the THIR data. These | results will be presented, and their significance discussed. US-I-2

MERIDIONAL FLUXES AND THE SUB-TROPICAL JET STREAM IN THE AUSTRALIAN REGION

R. R. Brook and K. T. Spillane Commonwealth Bureau of Meteorology, Melbourne, Australia

A study of the meridional fluxes of angular momentum, heat (both total and latent) and kinetic energy between the surface of the earth and 100 mb In the vicinity of Australia is reported. These quantities are important both for understanding the mechanisms of the General Circulation, and as bench marks in numerical modelling. They are conventionally evaluated relative to earth fixed axes which tends to mask the role of features such as the subtropical jet stream. The axes for this analysis were relative to the sub-tropical jet stream, and are based on Krishnamurti's (1958)scheme. In this way the aims of the present study, to elucidate the roie of the subtropical jet stream in the transfer processes of various quantitites and to provide data on these fluxes in the Australian Region, were assisted.

Using the daily 2300Z 200 mb analyses the latitude of the core of the subtropical jet stream at each 10 of longitude between 100 E and 180 E for the years 1962 to 1968 were extracted. From these data the coordinates n, s were assigned to each of up to 30 aerological stations. Here n is the normal distance of the station from the jet stream, and s classifies the shape of the jet stream in the vicinity of the station as either NW stream, ridge, SW stream or trough. The upper air data are then grouped by n and s and the monthly mean fluxes norma\ to the jet stream axis (due to the mean flow, or "standing eddies", averaged o\/er one month and the perturbations, or "transient eddies", from this mean), are calculated, at eleven standard pressure levels by the usual covariance methods.

By averaging the vertical integration of the fluxes over i all months a pattern emerges of poleward fluxes on the equatorward side of the jet stream in the troughs and NW streams on the poleward side in the ridges and SW streams in all but the latent heat case where there is a tendency for the opposite effect. These fluxes are mainly due to contributions by standing eddies. The integration over s gives the equivalent to the latitudinal variation of the vertically integrated *, meridional transport for earth fixed coordinates. The seasonal ^ values of these are presented and compared with those obtained by • other workers. The implications of this approach are discussed. US-I-3

EULERIAN AND LAGRANGIAN INTERPRETATION Cf THE SOUTHERN HEMISPHERE EOLE BALLOON EXPERIMENT US-1

Peter J. Webster, David G. Curtin and Yale Mintz

Department of Meteorology, University of California, Los Angeles, U.S.A.

The EOLE satellite-balloon system provided dense data

distributions in the upper troposphere of the Southern Hemisphere

between August fSTI a-->a..-Jy 1572. VJSC 5 —»_:- _-r :- s ,:j:.i :>• i1 infer aspects of the hemispheric climatology. Arrays of various mean measured and derived quantities for periods varying from

one year to one day are presented and discussed in their relation

to the large scale structure of the Southern Hemisphere. The

Eulerian and Lagrangian Interpretations of the EOLE data are

compared with earlier estimates made using conventional data and

the similarity and differences explained. The momentum flux due

to standing and transient eddies is discussed as a function of both

time and space scales and their relevance in the maintenance of

the general circulation of the Southern Hemisphere. bOME ASPtCTS OF THE DYNAMIC CLIMATOLOGY OF THE SOUTHERN HEMISPHERE

P. G. Price

Commonwealth Bureau of Meteorology, Melbourne, Australia

The energetics of the Northern Hemisphere's circulation have been investigated extensively by many workers during recent years, especially following Lorenz's revival of the concept of available energy as a small fraction of the total energy. Research along these lines hps been severely hampered in the Southern Hemisphere due to the lack of adequate data: most studies have been restricted to kinetic energy and have used the IGY analysis series whfch encompassed only the lower troposphere. With the implementation during 1972 of a full, multi-level numerical hemispheric analysis programme at the Melbourne World Meteorological Centre, data have now become available for a more thorough examination of the Southern Hemisphere's energetics.

A study is made here of the variation of the zonal and eddy components of the hemispheric available potential and kinetic energies based on data for the 12 month period, May 1972 to April 1973, and at the four levels 1000, 500, 300 and 200 mb. The eddy energies are further subdivided into components associated with eddies of longitudinal wave numbers one to twelve; the eddy spectra are shown to be described by the usual simple power laws over the range of the smaller waves and their exponents are evaluated.

The various results are compared with similar estimates for the Northern Hemisphere and the major differences, which are felt to result from the differing land/sea distributions in each hemisphere, are highlighted. US-1-5 THE STRUCTURE OF A MAJOR FRONT-LIKE WEATHER SYSTEM OVER AUSTRALIA IN APRIL 1970

H. W. Hill

New Zealand Meteorological Service, Wellington, New Zealand

In April 1970 a major weather system having the appearance of an extensive frontal cloud belt of great latitudinal extent, moved eastwards across Australia. It extended from the Tropics northwest of Australia to the southern ocean and gave widespread rain. It appeared associated with cyclonicity in the southern ocean and might, on the sea level maps be drawn as a cold front extending into low latitudes. Examination of the system in three dimensions and consideration of the trajectories of the air in isentropic surfaces showed, however, that it was complex. It consisted of a relatively shallow baroclinic front associated with a higher latitude cyclonicity but this reached only the southern edge of the continent. In sub-tropical latitudes there appeared to be large scale ascending motion in mid-troposphere accompanying a strong isotach maximum of the sub-tropical jet stream. In the very low latitudes it extended into a belt of cumulo-nimbus masses probably having their origin as a tropical convergent zone in the lower atmosphere. Complex front-like systems of this type appear to be a fairlv common feature of the region. US-1-6

RANDOM AND SYSTEMATIC VARIATIONS I HI ATMOSPHERIC RADIOACTIVE TRACERS < I II_AT ION IN Till. SOUTHERN HEMISPHERE

G. l-.iniUTt**, J. Sanak*, G. Polian*** and B. Ardouin*

The combined utilization since 1959 of natural and

artificial radioactive tracers enabled us to give evidence for three

main types of variations of the atmospheric circulation in the

Southern Hemisphere.

- First the atmospheric concentration of these tracers

presents typically random fluctuations.

- Next it is possible to point out some permanent

characters:

a) the latitudinal distribution of fission products, due to nuclear

tests, as well as that of other aerosols of stratospheric origin

are found to be reproductible year after year b) practically all tracers measured in the subantarctic and

antarctic areas present very clear seasonal effects

c) Radon concentrations measured in antarctic and subantarctic stations have shown the existence of 26-30 day periods.

*Centre des Faibles Radioactlvites, Laboratoire mixte CNRS-CEA .'' 91190 - Gif-sur-Yvette, France {

**Also Universite de Picardie .

***Also Terres Australes et Antarctiques Francaises •'] - Finally, there is strong evidence for the existence of a long-term effect in the atmospheric circulation of Lead 210 aerosols. Measurements of Lead 210 concentration in firn cores from Antarctica and the mean values of Lead 210 atmospheric concentration at Dumont-Durville (Terre AdSlie) from 1960 to 1971 are summarized in fig. 1 and show a remarkable correlation with the annual means of Sun spot numbers. This result implies that the general atmospheric circulation, at least in the Southern Hemisphere, should be to a certain extent modulated by the Solar activity.

a b c

a Pb2io aerosols moyennes annuelles i0"3 dpm.m'3 I- 100 b Pb2io neve dpm.kg"' c W nb toches soloires

I-

1960 1970 US-I-7 PHYSICAL ANALOGUE OF LARGE-SCALE HEAT EXCHANGE AROUND THE ANTARCTIC

M.I. Mishina and E. I. Klimova

U. S. S. R.

Simulation of some atmospheric processes can be achieved ; in rotating containers with a liquid providing that similarity criteria ;L are observed. ', 4;-: The results of simulting the mechanism of vortex formation . in the upper latitudes of the Southern hemisphere in a rotating cylindric /J container with a circumferential heater and central cooler (a model of '•.; the Antarctic) are presented in this paper. '; £ ;• -I -2 '? ' The experiments revealed that for values of Ro"-10 - 10 4. the mechanism is as follows, ; *

A vortex of anticyclonic pattern with several spiral flows J, which are a sort of surface of Interface between warm and cold water ;•• •» masses in the model is formed over the surface of the Antarctic. *'t''

Obviously, the spiral flows can be regarded as the analogue !j; of sections of the Antarctic front. Under certain critical temperature :\Jr gradient values cold masses of liquid can invade the relatively warm "}'i surrounding surface on the boundary of the complex anticyclonic fet formation. Disturbances in the form of such attacks of cold masses 4't'; on the surface of the interface turn in the direction of general rotation, !•:.!

thus the vortex of cyclonic pattern is brought about. >i;'•

* •/•! Despite the application of a simplified experimental model, yp.'i the vortex system of cyclonic type obtained on the interface surface is 4t>. identical to typical synoptic situations observed under natural conditions, lit

The model revealed that the vortex was periodically getting '.%£<•; stronger and weaker. Most likely, it is connected with energy trans- ?n formations in the large-scale heat exchange system and indicates the -, i possible existence of auto-variations in such a system. "*•,

*i Evaluation of the conditions for radically changing the Jt heat exchange system is to be followed. '?} ->. US-I-8 !•::•. CYCLIC VARIATION OF THE SOUTHERN HEMISPHERE: \*? VACILLATION TYPES AND INDEX CYCLES t

•';&•• Peter J. Webster and John L. Keller

h Department of Meteorology, il. University of Cat ifornia, Los Angeles, U.S.A.

'•{ Time-spectra of various measured and derived quantities 1 |f obtained from the EOLE satellite-balloon experiment in the Southern * |; Hemisphere, indicate various strong statistically significant peaks.

;|j These periodicities are shown to fall into two major categories, ;t each of which are observed in the spectra of a Zonal Index parameter .Jt;f (defined as the ratio of the zonal mean kinetic energy and the •' perturbation kinetic energy). These are:

! (i) a barotropic wave vacillation, which Is categorized *• by a strong 20-25 day rhythm. Cross-spectra between the two components of the Zonal Index parameter show a coherence of^ear unity at this period and a phase difference of nearly 180 . This suggests a strong barotropic cycle between ihe mean flow and the perturbations; and (ii) a baroclinic wave vacillation or potential energy vacillation. Certain spectral peaks ( 30 days) show significant cross-spectra between distinctly baroclinic processes. Such peaks may be identified as periodicities in the hemisphere available potential energy balance.

Finally, space-time spectra are constructed to determine the spatial scale preference of each process and their significance discussed in relation to general circulation of the middle and high latitudes of the Southern Hemisphere. N .;?," us-ii-i V,- AUTOMATIC CLASSIFICATION OF METEOROLOGICAL VJff'- PATTERNS AND PROBABILITY FORECASTS 7t<; US-II <;]'• G.V. Gruza

'r i Obninsk Hydrometeorological Centre, _-':.j\ . Obninsk, U. S. S. R.

';* The scheme for predictive parameters retrieval and com-

;,'••• ••• posing logical rules of objective weather forecasting and the scheme

' •. ,V for probability forecasting using Bayesian method are suggested. ••••,, t The results of the computer classification of several _' , meteorological patterns are used to obtain some informative predictors ,. of a discrete type. The classification includes atmospheric processes and H,'.- fields of different scales: fields of energy characteristics over the ' Northern Hemisphere, upper-air frontal zone structures, local : , temperature fields and temperature change processes over short •; time intervals. The latter are also considered as predictands. The classification of local parts of baric fields has been made for middle latitudes of the Northern and the Southern Hemispheres The difference between standard baric fields in the Northern and the a '*" Southern Hemispheres is analyzed. i The results of testing the procedure of temperature fore- k casting for several days are described. b us-n-2

HORIZONTAL (MEAN AND TURBULENT) FLUXES OF HEAT, ANGULAR MOMENTUM AND MOISTURE IN THE FREE ATMOSPHERE OF THE EARTH

;< I. G. Guterman

All-Union Scientific Research Institute of Hydrometeorological Information, Moscow, U. S. S. R.

During the last few years statistical processing of observations, made by 500 radiosonde stations of the Earth for a long- time period (1958-1965) was accomplished in the USSR. Along with the main climatic characteristics of wind, temperature and moisture, horizontal mean and turbulent fluxes of some atmospheric substances were calculated. The analysis of all statistics was made by plotting distributions on the 850 and 200 mb surfaces for January and July. In this study the meridional and latitudinal transfers of angular momentum, heat and moisture are investigated. The fields of mean and turbulent fluxes over oceans and continents, their annual vertical variations are considered. The data in the same seasons of two hemispheres are compared.

1 -

i I US-I1-3 ON THE PROBLEM OF THE GLOBAL STUDY OF SEASONAL STRATOSPHERIC WIND REVERSALS

Lsn

( '• Dr. Jacek Walczewski

Rocket and Satellite Research Division, Institute of Meteorology and Wo'er Economy, Cracow, Poland

The Spring and Autumn Reversals of stratospheric ,\ind^ are important indicators of the seasons in the upper atmosphere. The time when the circulation pattern, characteristic for the coming season, establishes on some altitude level, is variable from year to year and different for various levels; in this connection the reversals observed over some particular station have been classified into several types. It is quite logical to suppose that these phenomena are remaining in close relation to the general circulation of the atmosphere in whole. In this connection, some hypotheses have been created by different authors - among others, it is supposed that a correlation exists between the date of Spring wind reversal and the phase of quasi-biennial cycllcity in tropics, and - that a correlation may be determined between the date of Spring wind reversal and the character of Summer season in the troposphere, for some geographic regions.

By this reason - and by many other reasons - the investigation of seasonal stratospheric wind reversals is of great pract'eal importance. The main questions that should be answered refer to the time-space structure of the reversal particularly the regularity of originating the new season in higher or lower layers of the atmosphere, and to such problems like variability of reversal dates, possible cyclicities and correlations with quasi-biennial cycle, explosive warmings, solar events, etc. Heretofore, these problems were examined unsatisfactory, mainly because of inadequate observational possibilities.

Rapid progress in the atmosphere sounding methods and development of global research structures in the framework of GARP make now possible to propose an experiment devoted to the investigation of the stratospheric wind field on the global scale in reversal periods. Author tries to make a preliminary estimation of the observational requirements based on the known synoptic features of the reversals. The experiment should be conducted through several ycjr-j, 5 months oac;h year - 3 months in Spring and 2 in Autumn. It should cover" h*.M«j'>t rccjion 30 60 km, with time resolution not worse than 3 days

•4* \ us-n-4 LASER SOUNDING OF STRATOSPHERE AND MESOSPHERE

G. N. Glazov, V. E. Zuev, G. M. Krekov, A. I. Popkov, V. G. Astafurov

Institute of Atmospheric Optics of the Siberian Branch of the U. S. S. R. Academy of Sciences, Tomsk, U. S. S. R.

The results of theoretical-numerical experiments directed to the investigation of possibility and informativity of laser sounding of the upper atmosphere are discussed.

The limits of applicability of approximate radar equation in different schemes of sounding are shown on the basis of numerical solution of the total radiation transfer equation for a reflected lidar signal. The numerical estimates of profiles of backscattering for different models of the stratified atmosphere and different frequencies of optical sounding are presented. Consideration of optical properties and forecast of noctilucent clouds is discussed separately. The range of values of photoreceiver sensitivity necessary for obtaining finely stratified structure of aerosol and upper cloud level is determined.

An algorithm of estimate of potential accuracy and resolution at lidar measurements of profiles of vertical concentration of atmospheric aerosol is suggested and numerically illustrated. The cases of single-channel and multichannel processing of a fluctuating signal of backscattering are considered. The results are given characterizing the dependence of potential accuracy of aerosol concentration definition as a function of height, method of processing and lidar space-time resolution. US-11-5 STRATOSPHERIC RESPONSES TO SOLAR PROTON EVENTS

Christos Zerefos

Department of Physics, National Hellenic Research Foundation, Athens, Greece

Twenty four hour height changes of the 100 mb and 50 mb pressure surfaces following a proton flare are described. Objective criteria were used to select from the bibliography of solar events, for the period 1956-1969, a total of 33 of the more energetic proton flares for study. The analysis was limited to the checked radiosonde data for the Northern Hemisphere, North of latitude 35 . The principal results can be summarized as follows:

1) The 24-hour height changes of the 100 mb and 50 mb surfaces after a proton flare are greater than may be expected by chance. The statistical significance of the result is tested by a comparison with the height changes before a flare.

2) At both pressure surfaces north-of 50 degree latitude there is a predominance of height falls following a proton flare.

3) North of 65 degree latitude the mean temperature of the layer between the isobaric surfaces 100-50 mb increased on the average by approximately 0. 1 deg. C over the 24 hour observation period in which the proton flare occurred. This amount of heating requires an energy flux six orders of magnitude greater than the energy supplied to the layer by solar protons. However, the observed warming could be produced by the increased absorption of sunlight by an increase of ozone in the layer of only J%. us-n-6 COMPARISON OF CERTAIN FEATURES OF DYNAMIC AND THERMAL PROCESSES IN THE UPPER LAYERS OF THE POLAR ATMOSPHERE

L.R. Rakipova and L. K. Efirnova

U. S. S. R.

Synchronous comparison of thermal effects of chemical Influxes of heat in the mesosphere of the polar regions of the Northern and Southern hemispheres Is made. Winter season of the Northern hemisphere is chosen (for definiteness).

There Is atomic oxygen in the mesosphere of the Northern as well as Southern hemisphere, but polar regions of both hemispheres are characterized by different physical conditions of formation of influxes of heat connected with recombination of atomic oxygen.

Dependence of recombination influxes of heat on intensity of the sources of atomic oxygen, vertical velocity and turbulence is estimated. Also, this dependence is investigated taking into account the feed-back between values considered.

A model of the circulation and thermal regime of the mesosphere is constructed taking into account the recombination influxes of heat. It is shown that dynamic and radiative processes make recombination influxes of heat for the summer season of the Southern hemisphere less effective than for the winter season of the Northern hemisphere.

It permits the conclusion that possible variations of atomic oxygen concentration in the mesosphere of the Southern hemisphere in summer, in contrast to winter, could not lead to dependence of its circulation and thermal regime on solar activity.

Meridional cross-sections of the temperature and the three components of wind velocity for the Northern and Southern hemispheres are constructed on the basis of the model calculations. Characteristic features of the cross-sections of the temperature is the temperature rise from the summer to the winter pole, increasing with greater solar activity. US-2I-7

RESULTS OF OPTICAL STUDY OF NOCTILUCENT (MESOSPHERIC) CLOUDS

Ch. J. Vtllmann

Institute of Physics and Astronomy of the Estonian f Academy of Sciences, Tartu, U. S. S.R.

Results of solving direct and inverse problems in the

investigation of Noctilucent (mesospheric) Clouds are considered.

V-ose i.-.i .-;. ji'oi-j ".=\e> :^en carried out fc* different phvsicai

models and morphological structures of Noctilucent Cloucs.

Questions of complex ground surface and space optical

soundings of Noctilucent Clouds will be discussed. •'i. ^ • • • US-H-8 I ON THE BEHAVIOUR OF THE ES-LAYER AT MIDDLE LATITUDES

-.. '•'*

M. Bossolasco and A. Elena

Istituto Geofisico e Geodetico, Unlversita di Genova, Genoa, Italy

The detailed structure of the Es-iayer above

Genoa-Mt. Capellino (Italy) is investigated and discussed in

relation to wind shears and frontal Irregulartties. In summer

and equinoctial months there is a maximum of fEs at sunset

(sunset effect). Sudden increases or decreases of fEs occur

mostly just after the sunset. The occurrence of fEs-flashes

is maximum in winter - Over the Far East, where the

Es-ionfsation is stronger, a quasi-blennal variation of the

Es-layer has been found. us-n-9 ROCKET MEASUREMENTS OF HIGH ALTITUDE MOLECULAR OXYGEN

J. H. Carver, B. H. Horton and Mohammed Myas

Department of Physics, University of Adelaide, Adelaide, Australia

A method is described whereby a combination of two

simple ion chambers can be used to calculate the molecular oxygen concentrations from 70 km to 140 km (enveloping in the Interesting region of 100 - 120 km). The additional advantage of the system is that Solar Minimum Brightness temperature and solar fluxes can be inferred in the well suited wavelength band 1570A-1660A.

Oxygen denslttes are presented for the height range of

70 - 130 km determined from two detectors flown on a rocket launched from Woomera, Australia on 23 November 1972. Allowance has been made for variation of oxygen absorption cross section within the effective bandwidth of the detectors. Also calculated is ' the Solar Minimum Brightness temperature corresponding to the ' transition region between the upper photosphere and lower chromosphere. I us-ru-1 CHEMICAL IDENTIFICATION OF ATMOSPHERIC AEROSOLS

•: r US-IH E. K. Bigg and A. Ono

Division of Cloud Physics, CSIRO, Sydney, Australia

Some simple but useful chemical tests can be performed on very small atmospheric particles collected directly on electron microscope screens. For low altitude work, electrostatic precipitation using screens with conducting surfaces are convenient *" *. for capturing particles, while at high altitude impaction methods may be used. After particle collection half of each screen is "shadowed" with an inert metal such as gold-palladium alloy evaporated In a vacuum from a hot wire. This provides a permanent record of size distribution and concentration of untreated particles. The remainder of the screen Is then covered with a thin film of some reagent, again in a vacuum by evaporation from a hot source. For example, to detect sulphate particles a thin film of barium chloride may be used. Next the specimen is exposed to the vapour of a suitable solvent for a lengthy period then shadowed with gold-palladium and examined with an electron microscope. Less recrystallization of the reagent and more distinctive reaction products can be obtained using low vapour pressure solvents, although the reaction may take longer to proceed to completion. For example, with the sulphate test n-octanol gives better results than water. Liesegang rings are commonly observed with many reactions, while distinctive crystalline products occur with others. Tests for many simple organic ions or radicals are quite successful and have the added advantage of magnifying the original particles. However, the appearance of the reaction products can depend critically on thickness of reagent, solvent used and inadvertent

1: exposure to humid atmospheres. There is no obvious reason why some organic substances could not be identified similarly by their crystalline derivatives.

*•

A. Typical stratospheric partictes from an altitude of 21 km collected on a carbon surface on 3 April 1973 over Australia.

o B. Similar particles after coating with 60 A of BaCI« and exposing for 24 hours to air saturated with n-octanol vapour.

The use of such tests is to provide the size distribution and concentration of particular constituents of an aerosol. The bulk sampling technique usually used is capable of yielding more detailed information on substances present but not how they are distributed nor how they are associated. This knowledge is often of considerable importance In considering the effect of the aerosols on human health or the environment generally. us-in-2 ATMOSPHERIC PARTICULATE SIZES FROM POLARIZATION MEASUREMENTS US-Ill

J. G. Kuriyan

Department of Meteorology, University of California, Los Angeles, California, U.S.A.

The skylight polarization and intensity measurements

made by the UCLA-TRW polarimeter have been used to infer the

sizes of participates in the atmosphere. The results show a

-1 surprisingly large number of particles with radii in the range of

1 0. 05 to 0. 5 )j — a region that cannot be probed using the

existing in situ techniques. This successful (and self-consistent)

interpretation of these measurements establishes the polarimeter

as a viable tool for investigating, remotely, the sizes of scatterers

in planetary atmospheres. «js-in-3 LASER OBSERVATIONS OF AEROSOLS IN THE TROPOSPHERE AND STRATOSPHERE

W. G. Elford and S. A. Young

Department of Physics, University of Adelaide, Adelaide, Austral ia i

Observations of the back-scattering from aerosols

have been carried out at Adelaide, South Australia since 1969.

An annual variation in the stratospheric scattering is interpreted

in terms of transport from an equatorial reservoir. Possible

long term changes in the concentration of the stratospheric

aerosol Jayer are discussed.

The scattering from tropospheric aerosol are

discussed in terms of the nature of the aerosols, temperature

inversions and humidity. The results of a study of tropospheric

structure and winds from slant scattering profiles will be presented. , i Vi MODELLING OF THE ATMOSPHERIC PROCESSES BY THE ';'., SYSTEM OF EQUATIONS FOR MULTIPHASE MULTICOMPONENT T' MEDIUM IN ELECTRO-MAGNETIC FIELD

Y. M. Denisov and V. P. Ovcharenko

U. S. S. R.

The paper discusses a model considering the Boltzmann type equations for describing the behaviour of the aerosol particles behaviour, the Maxwell-Lorentz equations for describing electrical and magnetic properties of the particles and the atmosphere and ;the continuous medium equations for the behaviour of air and water vapour.

It is assumed that aerosol particles are of one of the following combinations: pure mineral particle, ice, water, , ,i . mineral nucleus-ice, mineral nucleus-water, ice nucleus-water, mineral nucleus-ice-water. The succession of phases is numbered from the centre. Interaction of the discrete phase with the continuous medium Is realized through the interfaces. The particles are characterized by means of the distribution function with variables such as time, geometrical coordinates of three-dimensional space, velocity components, volume, surface, temperature and the charge of the particle, surface energy and relative volume of each phase in the volume of particle.

The equation for the variation of the distribution function with respect to time comprises the full derivatives upon the time from the enumerated variables at the left hand the colHsion integral at the right one. The equation of motion for particles takes into account the requirements of the dynamics of the material point with variable mass and comprises body force, Archimedean force, Coriolis force, Lorentz force and drag force proportional to the first and second power of the particle speed. The equation for the variation of the total heat content with respect to time depends on the incident, scattered and long wave radiation, heat of phase transition inside and on the surface of the particle, frictional heat dependent on tin- motion of a particle with a force proportional to the tir-.t .mil -.einiij power of the particle speed.

Changes of the surface and volume of the particle are bound with the vaporization and phase transitions. The change of the surface energy of each phase is taken as proportional to the particle's temperature variation. The change of the charge is considered to be caused by seizure of ions, electrical conductivity of the air and by the leakage of charges owing to alteration of the i, curvature of surface cf the particle.

The system of continuous medium equations contain equation of motion and equation of state of the air and vapour, homogeneous equation of continuity for the air and nonhomogeneous one for the vapour and the energy equation for the air.

Electrodynamical equations represent Maxwell-Lorentz system p.nd nonhomogeneous equations of conservation of the charge considering the requirements of the formulation of the problem. For the ions suspended in the air the equations oi motion and nonhomogeneous equations for the conservation of the charge and for the number of ions of each kind, the total number and the complete charge of the ions are recorded.

These equations with the corresponding boundary and initial conditioris represent the closed system of equations modelling the atmosphere as a moving colloidal medium plunged into electro- magnetic field.

This equations system gives the possibility to sclve such task as the modelling of the human influence on external environment and the description of the formation processes of clouds and rainfalls, dust storm and others.

9 I

k. us-in-6 NEW RESULTS ABOUT THE TROPOSPHERIC BACKGROUND AEROSOL

Ruprecht Jaenicke

Max-Planck-!nstitut fur Chernie (Otto-Hahn-Insti tut), Mainz, Federal Republic of Germany

About three quarters of the troposphere are filled with a low concentration aerosol often referred to as the tropospheric background aerosol. • This aerosol is of considerable importance with respect to inadvertent climate effects because it occupies most of the troposphere and because it is very sensitive to anthropogenic influences on a regional and global scale. The effects on the atmospheric energy budget are both direct - by scatter and absorption of short wave radiation - and indirect - by modifying the albedo of water clouds. Despite this importance we know very little about this background aerosol except that its origin and * composition is rather complex with components from polluted continents, arid zones, the ocean surface and organic constituents. £•; In view of this situation we developed a program on background ;, aerosols which concentrates on the following topics:

1) The size distribution and behavior of the mineral dust « component in air originating from the Sahara,

2) The chemicai composition of the organic fraction of the background aerosols, and L

3) The size distribution of the background aerosol below * ; about 0. lytv radius.

After developing special techniques in all three areas ^. applicable for the low concentration background aerosols data will ;•• be obtained over the Atlantic Ocean from expeditions to the Cape £ Verde Islands and with the research vessel Meteor on east west $.*• crossings. The expedition to the Cape Verde Islands is just ^ finished and the data are in evaluation as this abstract is written. T"s Meteor e^oed't'cr w'il be ir Octobe-. Trie -es^lts obtained !•; et these evpecit'or.s vvi"! be presentee =-c t-e'- 'rr.p 'catiors wit" £/ respect to our understanding of the tropospheric background (•'- aerosols will be discussed. f •• us-m-7 SOME REMARKS ON THE STRATOSPHERIC NUCLEI COUNTS

J. Podzimek and J. C. Carstens

Graduate Center for Cloud Physics Research, University of Missouri, Rolla, Missouri, U.S.A.

Last measurements of the background of air pollution in the stratosphere led to the conclusion that the concentration of Aitken Nuclei (AN) might be higher than formerly measured by C. Junge (1961). Remsberg's article ;1972) called attention to the fact that the applied injection of clean air prior to the expansion in the Junge's AN counter can be responsible for the complete evaporation and therefore for low counts of AN, assuming that the majority of nuclei were drops of sulfuric acid.

This paper deals theoretically with the more realistic case of the evaporation of drops of a volatile substance during the compression of stratospheric air in the AN counter. Discussed are the individual terms influencing the heat and mass transfer around evaporating droplets in a small chamber, e.g. the dis- continuity in heat and vapor density field around a droplet. On the basis of the calculations performed some of Remsberg's state- ments are corrected and conclusions are made for AN counting techniques in stratospheric levels. Attention is also paid to the possible composition of submicron particles in the stratosphere and to whether or not we can assume complete evaporation of a nuclei of volatile substance in the counter. US-I1I-8 GENERAL - ELECTRIC STRATOSPHERIC AITKEN NUCLEI COUNTER AND THE RESULTS OF ITS PRELIMINARY TESTING

J. B. Habcrl, Ordnance Systems, General Electric Company, Pittsfield, Maryland, U.S.A.

J.L. Kassner, J. Podzimek, J. E. Wegrzyn, Graduate Center for Cloud Physics Research, University of Missouri, Roll a, Missouri, U.S.A.

Preliminary information on the features, design and ; calibration of the GE - Stratospheric Aitken Nuclei Counter is j-- presented. The counter, designed under the support of the U.S. Department of Transportation, is going to be used for the ,•"] investigation of the possible effects of stratospheric air transport i',.., on the pollution of the stratosphere with its effects on the biosphere. * ,i Comparing the new counter with the well known GE - counter we j find several substantial changes, which are mainly due to the j ? requirement of measuring very low concentrations of AN (smaller j',* than 10 particles per ccm), such as the improved optical system « f in the critical space of the counter and the air pressurizing and •{/' humidification system. Major problems were related to the !,; design of the pressurizing unit and to the evaluation of the optimum |; sampling and air pressurizing time. • ;;•

The description of laboratory tests with well defined ;. ' AN is presented together with the preliminary results from the 'p. calibration of the GE - Stratospheric Aitken Nuclei Counter at f normal (ground level) pressure. The data show some of the ;•'! ' features of the counter and the comparability of the measured • "' concentrations with the University of Missouri at Rolla AN Counter "j': and with the ordinary GE - AN Counter. \.J

On the basis of preliminary tests and theoretical investi- ;;• ' gations some conclusions are made for the application of the GE - f/S, Stratospheric Aitken Nuclei Counter in the program mentioned. |v

•i?' EFFECTS OF STRATOSPHERIC AEROSOLS OK TROPOSPHERIC TEMPERATURE.

Stephen H. Schneider

National Center for Atmospheric Research, Boulder, Colorado, U.S.A.

The effect of increases in stratospheric aerosol loading on the tropospheric temperature is investigated with a one-dimensional (vertical coordinate) radiative-convective model of the earth-atmosphere system. A range of aerosol optical properties is assumed: i.e., absorption, backscattering and optical thickness parameters. in most previous studies of the possible effects of increases in atmospheric aerosols on the nlobal climate a change in global albedo from aerosols was computed, under the assumption that albedo was the most relevant climatic parameter and could be directly related to surface temperature. While the albedo of the earth-atmosphere system is probably the most important measure of any potential climatic effect of aerosols in the troposphere (which is a region that is well-mixed vertically), changes in the albedo resulting from increased stratospheric aerosol loading are probably not sufficient to determine even the algebraic sign of temperature response by the troposphere. The reason for this is that a stratospheric global aerosol will reduce the downward flux of solar radiation reaching the troposphere, regardless of the relative efficiency with which that aerosol absorbs or beck-scatters sunlight. The magnitude of tropospheric temperature response to various perturbations in stratospheric aerosol concentrations is computed with a radiative-convective model of the earth-atmosphere system that includes simultaneously the visible and infrared radiative effects of atrrospheric water vapor, carbon dioxide, ozone and a fixed amount of clouds, as well as the dynamical effects of vertical convection. The latter is treated by the imposition of a convective adjustment. us-iv-i

MEASUREMENT OF ANGULAR DISTRIBUTION OF SKY RADIATION USING A SKY PHOTOMETER US-IV

S. Rangarajan, India Meteorological Department, Poona, India

and

R. Vijayakumar, Indian Institute of Tropical Meteorology, Poona, India

A simple instrument has been developed for the measurement of the angular distribution of the intensity of sky radiation. A narrow-aperture photometer fitted with a green filter is mounted on a theodolite to scan different portions of the sky and measure the relative intensities of sky radiation at 0. 5 micron wave-length at normal incidence.

The sky radiation under cloudless conditions as mapped with the aid of the instrument is found to be highly anisotropic with reference to the position of the Sun. Excluding the radiation from the Sun's disc and that from a region 15 around it, the integrated radiation falling on a spherical surface from one half of the sky containing the Sun is calculated to be nearly 3 times that from the opposite half for elevations of the Sun 30 to 60 . Such a marked anisotropy caused by aerosol scattering could be applied to many practical problems including design of buildings.

The instrument is also used to measure the angular distribution of intensity of scattered light along the solar almucantor. The rate of decrease of intensity from 3 to 30 from the Sun is found to be inversely correlated with the magnitude of the prevailing size distribution parameter for aerosols and thus the technique offers a simple method of determining this parameter. US-IV-2

OPTICAL PROPERTIES OF ATMOSPHERIC AEROSOL AND THEIR SIGNIFICANCE FOR THE STUDY OF TRACE ATMOSPHERIC CONSTITUENTS

G. I. Kouznetzov

U. S. S. R.

The results of the author's recent observations of ?'

spectral aerosol attenuation o*.made in continental, oceanic and •}>

mountainous regions as well as in the free atmosphere are reported.

The results of theoretical evaluation of polydispersive aerosol

attenuation for different aerosol models are also presented. |

The optical and microphysical properties of atmospheric |".

aerosols in different geographical regions are compared and studied |*

theoretically and experimentally. Great differences were observed ^5

in aerosol concentrations and spectral properties. Nevertheless, fy

ocean and mountain regions often display similar spectral tendencies £$. for 0* . i!f,i

During the cruise of scientific ship "Professor Wiese" in if 1 the Atlantic during March-June 1969 along 30 W very stable geo- .!>.;; graphic pecularities of aerosol distribution were observed, e.g. the |>; influence of the African continent. Results of such observations p*j together with date of ozone content are presented. If'!

mmi US-IV

In the tropical Atlantic a noticeable diurrel variation cf

OX with increasing Angstrom coefficient by noon has been i observed. Perhaps, it is connected with phase transitions of

water. In this way microphysical characteristics of aerosol

might be estimated.

The results of aircraft observations of aerosol size dis-

tribution are also discussed.

The influence of spectral aerosol attenuation on the

accuracy of spectrophotometric observations of trace gaseous

constituents of atmosphere was studied. US-IV-3

EFFECT OF AEROSOL SIZE DISTRIBUTION ON A SCATTERED RADIATION IN THE INHOMOGENEOUS OZONE ATMOSPHERE CALCULATED BY USING THE "ADDING" METHOD

T. Takashima

Meteorological Research Institute, Suginami, Tokyo, Japan

The importance of satellite measurements has been

clearly discussed in relation to the investigation of the amount

and the distribution of the atmospheric ozone. Hence in order to

estimate the feasibility of indirect optical methods to model the

earth-atmosphere system, the comparisons of the results of the

satellite measurements with that of the theoretical computations

have to be taken into account. However, in most cases of the

theoretical computations of the backscattered radiation in the

region of between 0. 30 u and 0. 32JJ, the aerosol distribution in

the atmosphere was neglected, since the computation time would

be prohibitively long if the aerosol is in the atmosphere.

In this paper, the method of computing the diffuse

reflection radiation from an inhomogeneous plane-parallel

planetary atmosphere including ozone and aerosols is discussed.

Furthermore, the computational results are discussed in relation

to the effect of aerosol size distribution on the polarization features

of the scattered radiation through the ozone atmosphere.

' ii" US-IV-4 MULTIPLE SCATTERING MEASUREMENTS AS A FUNCTION OF WAVELENGTH BY USE OF A DYE-LASER

' Ariel Cohen

; Department of Atmospheric Sciences, | The Hebrew University of Jerusalem, Israel f f j

! Dow latex monosized spheres were used as scatterers \ in a laboratory system containing a dye-laser as the light source (the system has been described elsewhere ). Eight samples of different particle concentrations were prepared and the optical depth of each was measured. The two lowest concentrations gave the same relative Mie Scattering intensity curve as a function of wavelength as is expected when merely single scattering occurs. The shape of the curve started to change with the further increase in the number density of the particles. The main characteristics of the changes was the gradual disappearance of the minima and for higher concentrations - also the maxima.

Special measurements were made to ensure that the beam path and the sample volume were big enough to include most possible multiple scattering effects influencing the scattering intensity. Thus, this experiment provides (within a specified degree of accuracy) the multiple scattering Mie curves vs. optical depth for a range of 1000 A .

1, A. Cohen, V. E. Derr, T. McNice and R. E. Cupp, Appl. Opt. April 1973. US-IV-5

AIRCRAFT MEASUREMENTS OF THE ALBEDO OF THE EARTH AND OF CLOUDS OVER INDIA f> r

A. Mani, O. Chacko, V. Desikan and V.V. Abhyankar

India Meteorological Department, New Delhi and Poona, India

Measurement of global and reflected solar radiation and of •:. earth's albedo over extensive land areas in India and over the adjoining [ oceans were made from a Canberra aircraft during July - August 1972 f: as part of an Indo-UK Project "Storm Exchange". Two thermoelectric y pyranometers, one facing upwards and the other facing downwards were ij used to measure the global and reflected solar radiation, a photographic f;f recorder with suspended coil mirror galvanometers recording the data £ continuously in flight. f

Twenty aircraft flights were made from three bases, 7 from I Bangalore (1 3°N 77°E), 8 from Poona (18°N 74°E) and 5 from Calcutta f (22 N 88 E), over both land and sea covering areas from 7 N to 24 N i and 71 E to 88 E, with the aircraft flying at heights above ground/sea [' varying from 150 to 15000 metres. f,

The values of global solar radiation recorded were of the frf, order of 1. 60 - 1. 80 cal/cm /min, when there were no clouds; thin }' cirrus reduces this value by about 16 to 20 percent and other clouds I *{ by larger amounts depending on their type and thickness. Reflected <; radiation was higher over cumulus and cumulonimbus clouds than over | ' any other type of clouds. •

The albedo over the sea was found to vary between 0. 04 to ^ ' 0. 13, depending on the state of the sea and that over the ground between ? • . 10 to . 25. The albedo over active cumulus clouds was about 0. 40 to ,,»\ 0. 60 and that over cumulus of smaller extent between 0. 25 to 0. 40. • •« fjj* Stratocumulus clouds have smaller albedo, 0. 20 - 0.40 and stratus, :?->;'. 0. 15 - 0. 25. The albedo of altostratus clouds was found to lie between ^ 0. 25 to 0. 35. The albedo of the cirrus remains of dissipating cumul- /V , onimbus clouds was about 0. 45 to 0. 55. In a growing cumulus cloud 5?. 1 the albedo changes from 0. 20 to 0. 55 depending on the stage of growth .'£•. and albedo values change from 0. 16 - 0. 27 to 0. 30 - 0. 36, after stratus _V and stratocumulus clouds acquire a cirrus and cirrostratus ceiling. %

The observations are compared with satellite and ground observations of surface albedo over India. I US-IV-6

MEASUREMENT OF THE TOTAL PRECIPITABLE WATER IN THE ATMOSPHERE USING AN INFRA-RED SUN PHOTOMETER

S. Rangarajan

India Meteorological Department, Poona, India

By making use of the general principle of the Sun

Photometer and by the application of a square root law for the

absorption by water vapour in the near infra-red region of the

, solar spectrum, a method has been developed for a quick and

1 accurate determination of the total water vapour content of the

atmosphere. A dual wave length Sun Photometer fitted with

, narrow-band optical filters and a portable operational amplifier

are employed to measure the relative intensities and of the

solar radiation at 0.94 and 1.06 micron wave-lengths respectively. i

A calibration procedure has been developed making use of radiosonde-

derived water vapour content to determine two instrumental constants

K and K . These constants enable the photmeter readings and

i to be rapidly converted into the total water vapour 'W. The

•I instrument has been found to be stable in operation and capable of

j measuring water vapour contents ranging from . 05 gm to 7. 0 gms/cm I ! Each complete determination takes a timo of 2 or 3 minutes only.

A method of providing an absolute calibration independant i , of radiosonde observations has also ber»n s 1 i US-IV-7 MEASUREMENTS OF THE ATMOSPHERE RADIANCE IN THE 8-I2MICRON BAND

A. G. Gorelik, R. B. Bielitch, S. F. Kalachinsky, A. S. Novokrestchenova

Central Aerological Observatory, GUGMS, Moscow, U. S. S. R.

The analysis of experimental data of intensity measured

at the surface in the 8-12 micron band is presented for cloudless and ; i cloudy atmospheres. These intensity measurements were made by

means of an infrared radiometer in the spring, summer, and autumn >

seasons during 1970-1972 at middle latitudes. The absolute error |

of the measurements is 0. 022 mvt/cm sr (roughly 0. 3 at the K

temperatures 250-300°K). i

By using the radiosonde data, obtained simultaneously \

with the IR-radiance measurements, the theoretical intensity values ; were calculated. The agreement between the experimental and the ,' calculated values is shown for the different seasons. The dependence j of the measured intensity data upon total atmospheric moisture content j;1 t is considered for different viewing angles. It is shown that this j t relationship approximates a straight line. The root mean square « deviation of this is 0. 3 mw/cm sr. ;, '

Features of the angular distribution of the downward '•• radiant intensity are explored for the cloudless atmosphere. It is '•' shown that in spring when the atmospheric moisture content is low f the secant law for downward radiance holds. ,',

The measured data allowed some statistical radiance t. characteristics to be obtained for different cloud forms. The i>-,

l calculated average intensity values (J ), their dispersions ( V1T ), r* the correlation coefficients of the downward intensity value with the

lower cloud boundary-temperature { riT ) and heights of the latter

are shown in the table.

\tfoud Sc Scop St Ns Ac Ac op Ci Cuhum Cumed Cu cong

2 3.3J 3.38 3.64 3.57 306 3.39 1.33 2.65 2 72 3 48

0.52 0.05 009 0.11 0.08 0.06 0.11 0.15 0.14 0.48

f 0.66 0.87 009 0.61 0.68 0.85 0.88 IT 0.31 0.53 0 53 rIh -0.22 -0.42 -0.13 -0.66 -0.54 -0.56 -0.69 •0 39 -0.18

US-1V-8

RADIATION EFFECTS ON RADIATION FOG FORMATION AND EVOLUTION PROCESSES

Y. S. Sedunov and I. M. Zakharova

Institute of Experimental Meteorology, Obninsk, U. S. S. R.

The radiation fog is formed as a result of IOCTI air cooling by means of radiative and turbulent heat exchanges. In ti e present work the physico-mathematical model describing the radiation fog formation and evolution processes is considered. The model includes the heat transport equations (with regard to the radiative heat exchange), water vapour (with regard to the phase transformations) and water content (with regard to the gravitational force action). US-32-8

The eddy coefficient is taken to be an unknown quantity, that is why for its estimation the equations of the planetary boundary layer dynamics are used. The heat exchange processes on the underlying surface and in the soil taken into account by introducing the thermal soil conductivity and earth's surface thermal balance equations into the model. In this mathematical model as a first approximation the relation between the macro- and microprocesses has been found.

The mode) investigated gives the possibility to follow the dynamics of the radiation fog formation and evolution processes. The comparative consideration of radiative and turbulent heat exchanges in the atmosphere allows to estimate their role in the boundary cooling process. Besides the consideration of the radiative heat exchange in the atmosphere allows to obtain the fine radiation effects in the boundary layer of the fog and to consider their effect on its further growth.

The inclusion of the eddy coefficient in the number of the unknown quantities of the model allows to take into consideration the variations of this factor as a function of the wind and temperature regime changes in the atmosphere.

As for the inclusion of the macro- and microprocesses relation into this model it gives the possibility to take into account the effect of the meteorological field variations on the inner fog ' structure and of the fog itself on the thermal and dynamic regime changes in the atmosphere.

The calculation results showing the known physical peculiarities of thermal and dynamic regimes prior to and during fog formation and evolution are given. These results are in agreement with the available, relatively few In number, experimental > data obtained from macro- and microphysical characteristics of the ) fog. The specific character of the radiation effects is discussed. i V

p1 *. US-V-1

STATISTICS OF THE FINE STRUCTURE OF TEMPERATURE IN THE ATMOSPHERIC BOUNDARY LAYER us v

R. A. An ton i a

Department of Mechanical Engineering, The University of Sydney, Sydney, Australia

The statistical characteristics of the fine scale structure

of temperature in a turbulent flow are affected by both "X and £ ,

the local rates of dissipation of the temperature and velocity fluctuations respectively. An analysis based on a consideration of the structure functions of temperature fluctuations for scales in the viscous range predicts the flatness factor of the temperature derivative, as measured by Gibson, Stegen and Williams (1970) for the atmospheric boundary layer over the ocean, fairly well.

The analysis assumes that XP and i-r , the dissipation rates averaged over a small volume of linear dimension t , are log-normal.

An indication of the magnitude of the correlation between Xr and 6P is obtained from laboratory measurements on the axis of symmetry of a heated turbulent jet. US-V-2

WIND SPEED VARIATIONS IN AN INDUSTRIAL ENVIRONMENT

M. R. Thomson

Aeronautical Research Laboratories, Department of Supply, Melbourne, Australia

i A easel la 3 cup anemometer has been operating in an J industrial environment over a period of 12 months. The anemometer !• was situated 14 metres above the ground, being four metres above f the average nearby roof top level. This paper describes some of [' the statistical properties of the wind speed which was measured : every second throughout the year. r

Energy Density Spectra were computed using the Fast I Fourier Transform Algorithm, using all 12 months of data to define * the energy within each frequency band between 1800 and 0. 005 cycles j per hour (periods between two seconds and eight days). This method '•: of analysis excludes the possibility of bias in the selection of data ^ which some observers see as a possible reason for the "spectral gap" i first reported by van der Hoven. The shape of the spectra above a j. frequency of two cycles per hour is described as a function of time ; and the 30 minute mean wind speed. )V

This paper also discusses the variation of the wind speed probability distribution as a function of time, as well as the probability distribution of gusts above and below the 30 minute mean wind speed. Other statistical properties of this large amount T of wind data will also be discussed. • S:

P US-V-3

CORRELATION OF HAY-PASQUILL SCALE PARAMETER EXPERIMENTAL RESULTS

S. Chandra

North Carolina Agricultural & Technical State University, Greensboro, North Carolina

The Lagrangian correlation coefficient R (j£ ) has been interpreted by Hay and Pasquill in terms of Eulerian properties by assuming that Lagrangian and Eulerian correlations are similar in shape and that the ratio of the Lagrangian to the Eulerian scale is a parameter to be estimated from experiments. It can be shown that a change in the shape of the correlogram is much less important than a several-fold change in scale. Thus, as long as the requirement of similarity in shape is satisfied roughly, the assumption of precise similarity is unlikely to introduce large error. R (.£ ) for a particle might then decay with time in a similar manner to the Eulerian coefficient R (t) measured at a fixed point but with a different time scale. Thus, R (£ ) = R (t) when Jf =jB t, where J5 is the ratio of the Lagrangian to the Eulerian time scales. A definite relation between !he corresponding spectral functions can therefore be obtained and Taylor's equation relating the displacement of a particle to R (,£ ) be used to obtain ft , the Hay-Pasquill scale parameter. Chandra obtained data by allowing helium puffs to diffuse into the air stream within a neutral boundary layer, p -values in the 4-18 range were obtained for travel distances between 1 ft. and 4 ft. from the source. US-V-4 REGRESSION RELATIONS FOR TURBULENCE PARAMETERS IN THE ATMOSPHERIC BOUNDARY LAYER WITH INHOMOGENEOUS UNDERLYING SURFACE

W. Gerstmann

Meteorological Service of the GDR, Meteorological Main Observatory, Potsdam, German Democratic Republic

On the measuring site of the Meteorological Main

Observatory, Potsdam, of the Meteorological Service of the GDR

the fine structure of each of the three wind components and of the

temperature was determined by a sonic anemometer, made by

Kaijo Denki Comp. and gradient measurements were made using

conventional instruments.

From these data the turbulent heat flux, the components

of the friction tensor, and the spectral variance of the vertical

wind component were calculated. For each of these parameters

regression relations and the associated confidence intervals were

calculated. On the basis of these relations the parameters can

also be calculated for specified times at which only gradient

measurements are available and the stratification is unstable. The

quality of the relations was found to be remarkable in spite of the

rather inhomogeneous terrain. US-V-5

SOME CHARACTERIST1CS OF THE DYNAMIC AIR-SURFACE INTERACTION IN CENTRAL EUROPE

K. Bernhardt

Humboldt-UnTversity at Berlin, German Democratic Republic

"* Some boundary layer parameters, characterizing the

dynamic air-surface interaction, are deduced by statistical data

processing from routine surface and aerological observations in

the German Democratic Republic. For instance, mean values are i obtained for the surface-to-geostrophic wind velocity ratio, for

the angle between the direction of geostrophic and surface wind

and for the geostrophic drag coefficient, especially, in dependence

on geostrophic wind, boundary layer stratification, season and

time of day. The results are compared with conclusions from the

boundary layer similarity theory, and with the Kazanskii-Monin's

resistance law for the barotropic boundary layer; the constant "A"

of the resistance law is determined from rawinsonde data. Generally,

the dependence of the investigated parameters on the geostrophic

wind velocity is more, but their dependence on the stability of

stratification is less pronounced in comparison with theoretical

calculations, and a marked dependence on geostrophic wind direction

is found in some cases, too. US-V-7 j- NUMERICAL MODELLING OF WIND AND TEMPERATURE [ OVER MOUNTAIN-VALLEY TERRAIN |"

Wen Tang

Institute for Storm Research, Inc., Houston, Texas, U.S.A.

and I.- Lowell Technological Institute, Lowell, Massachusetts, U.S.A. 'J'

A numerical model is developed to investigate the dynamics ^ of the local climate of the undulating two-dimensional mountain-valley t, terrain. This model considers linear interaction between the larger ,';' scale prevailing flow and thermally induced flow near the earth surface. |. Typical steady state day and night circulation and temperature field are {'> obtained. Many important features of the circulation in the computed | results are in good qualitative agreement with observations obtained f from different parts of the world. A large separated cell is developed J1 over the lee slope during the day and a thin elongated separated cell is JV developed o\/er the windward slope during the night. Computed wind |? velocity and potential temperature fields will be presented. Transient J solutions from noon to early morning of the next day for different imposed 'f,f turbulent flow and thermal boundary conditions are also obtained. Under ,jM". generally turbulent flow conditions with stable thermal condition near r|; .

the surface, a strong wind is developed in the lowest layer of the ,j§:.r atmosphere similar to that observed in mountainous country during the : ]> night. As to the much less turbulent condition, stream function solution '|ii for midnight yield flow pattern very similar to the steady state solution. r1; , A theoretical method in calculating the ground surface temperature and '$'• then the heat flux to the air over the present model terrain is also •$:•• developed. This method is based on the energy balance equation which jf°\ includes the shadow effect of the mountain during the day time and will .-&; be applied in the refinement of the boundary condition and thus the local <-^] circulation. The application of the knowledge of the mountain-valley $$''1 climate to air pollution problem will also be discussed. .ft! US-V-8

ON ALGORITHMS OF OCEAN AQUATORIUM OBJECTIVE CLASSIFICATION ACCORDING TO CLIMATIC QUASI-HOMOGENE IT Y

V. V. Filippov, A. S. Kaganeky, P.f. Krivilo

U. S. S. R.

, Taking into consideration the rate of World ocean economic

* development and accumulation of hydrometeorological observations, 1

i the specification of the climate of its aquatorium should be con-

: sidered urgent. The assimilation of large quantities of information

> may be realized with the aid of numerical methods anii modern com-

putors.

• It is reasonable to begin the above-mentioned specification , from the physical and geographical base of World ocean climato- i

- graphy, i.e. from the substantiation of representative? areas grid,

» within which the climatic stability is observed. In this case the

\ traditional generalization by ten-degree squares should be considered i

> a historically established first approximation.

| The climatic quasi—homogeneity is considered as the more

' accurate definition of the real situations of hydrometeorological i I elements medium fields, averaged in space and time. i

j We shall call the three-dimensional (latitude, longitude,

> time) area quasi-homogeneous, if its internal conditions are very

{ close to stationary in time, homogeneous and isotropic in space and, besides, if the empiric laws of proabilitity distibution according

to the data of this area approach to the limit.

(n order to select homogeneous areas, S r ^\ • ^ f is defined,

as the class of densities distribution, satisfying the conditions of

homogeneity A.

Now, let there be an ensemble of hydrometeorologica!

observations 1 Y I , dealing with some area \) . Using the iA )5 >V{_ let us estimate the empiric density of probabilities >

distribution ^P(Y.\ an^ introduce the functional

where ^[j is the contribution value of the area T). , where hy dro-

meteorological element )( has distribution +•(*); I

The totality of j <^f- f,-( X) < , corresponding to the minimum 1

of the functional gives the contribution values and distributions of ?

quasi-homogeneous areas J) i , the summing of which is the initial !

area J) . *

Now let us divide ihe area J) into sub-areas Pj and for

each of them find Qft - the contributive value of the areaD^j , '

nas i.e. the area, where X distribution T((x^ ; then

T\ * considered to be probability apriori. Accurate to sub-area \j\

it is possible to construct a map Q(j for each L . The Geometrical

locus &.. = ^.-y> is the boundary of the quasi-homogeneous area. f US-V-9 STUDIES OF DUST AND AEROSOLS AND THEIR EFFECT ON ATMOSPHERIC ELECTRICITY AND TURBIDITY PARAMETERS

A. Mani, B. B. Huddar, C. P. Joseph, O. Charko and A.K. De

India Meteorological Department, New Delhi and Poona. India

Regular measurements of the dust and nuclei content of the afr near the ground have been made at a fev\ stations in India to study the characteristic elements of natural pollution npar the ground, its origin and variation with tice, ^fa-uns and altitude. The electrical field strength, the positive and negative electrical conductivity of the air and the number of positively and negatively charged small ions in the atmosphere? near the qround were a!so measured at the same time.

Atmospheric turbidity using Angstrom ;>\ rhel iometers and Volz sun photometers hcive a!c-o her:- inade it .; number of stations in India for many years. The results < f the observations and the effect of dust and aerosols on atmobpher.t- e|>" <"tric; t; parameters are discussed.

The dust content and the electric field s-bou sva.-onnl and diurnal variations opposite to iho-e of the sma'i inn density and electrical conductivity. The dust content i.- a maximum in the hot dry pre-monsoon months, while the electric field is a maximum during the monsoon months. A spectnruhr fall \n the dust content is noticed with the arrival of the monsoon dt Delhi, value falling from 84 to 11 per cc in a day.

An eight to ten fold increase in the dust and condensation nuclei content has been observed at Poonn during the last 30 years, indicating a change from a rural to an urban environment with a corresponding decrease in small ion content and electrical conductivity. Atmospheric electricity conditions are strongly anthropogenic and the large increases observed in these atmospheric parameters during the last 30 years have to be ascribed to the increase in urbanisation, traffic and industrialisation in the region round Poona.

Turbidity coefficient B also shows striking seasonal variations both at Poona and Delhi with maximum values in the hot pre-monsoon months, April to May and minimum during the winter months, October to December, The seasonal variations are more pronounced in Delhi. There is a sharp fall in turbidity with the arrival of the monsoon. The variation of the wave length exponent & of aerosol extinction, which depends on the size spectrum of aerosol particles, is different at Poona and Delhi. At Poona ^generally lies within the range 0. 5 to 2. 0 and has a mean value of 1. 0 and is fairly constant during the different seasons. Only occasionally does ct fall to 0 or increase to a value of 3. 0. The size spectrum of aerosols at Poona is fairly constant. At Delhi the summer values of of are much lower than that of winter, the aerosol size spectrum undergoing a sharp decrease, Ci having a mean value of less than 0. 5, due to the large scale influx of bigger particles brought over the station by dust storms and dust raising winds from the adjoining desert areas. US-V1- 1 THE MOVEMENT OF TROPICAL CYCLONES

F.A. Lajoie US "VI

Commonwealth Bureau of Meteorology, Melbourne, Australia

Using satellite pictures and the hest-possible tracks of tropical cyclones operating in the Austral ian region, a study of the distribution and pattern of clouds within 800 km of the centres of the cloud vortices has revealed that cacti tropical cyclone cloud system has some characteristic features which are cjood indicators of their subsequent direction of motion. The significant cloud features are: (a) the cumulonimbus-free sector, defined as a sector, relative to the cyclone centre, devoid of massive cumulonimbus clusters but which may contain cirrus or small cumuli, and (b) the most developed cumulonimbus cluster at or near the downstream end {in the cyclonic sense) of a line of conveclivc clouds or fpederband. The latter are entities separate from the central cloudmass (diameter about 200 km) of a tropical cyclone and generally end abruptly in one of the southern quadrants some 200 to 600 km from the vortex centre. This feature is easy to detect in some pictures, but difficult to find in others because of the cirrus canopy aloft which sometimes masks the low cloud pattern. Some guides to cintnrt this feature are given in the paper.

The following guidelines can be used to forecast the direction of movement:

(1) A tropical cyclone will not continue to move, or curve, towards any direction within a cumulonimbus - free sector; if moving in such a direction it will curve awa\ from that direction.

(2) A tropical cyclone centre will move or curve, within twelve hours of picture time, towards a direction given by a line joining the present position of the vortex centre to the present position of the most developed cumulonimbus cluster at or near the downstream end of the feeder cloud- band.

(3) When a tropical cyclone has two feederbands and Is moving at, or just prior to, picture time roughly towards the most developed cumulonimbus cluster near the downstream end of the feederband it will curve within 12 hours of picture time towards the most developed cluster near the downstream end of the other feederband.

The speed of movement of a tropical cyclone along the forecast direction, is shown to be the speed of the integrated "total outflow current" in the convective layer just ahead of the downstream end of the feederband. US-V1-2 AUSTRALIAN CYCLONIC STORM SURGES - FORECASTING AND MODELLING

K. P. Stark

Department of Engineering,

James Cook University of North Uuevn;..land, Australia

A storm surge is the short term change (rise or fall) in sea level produced by u meteorological ti; turbance such as a cyclone. Every tropical cyclone is accompanied by a storm surge, developed initially by an inverse barometer efh-ct; however, as the cyclone crosses the coast the combined effects of ocean bed-slope, speed of cyclone movement and oth-.r characteristics of the cyclone can produce a coupling effect which may magnify the inverse barometer effect a number of times.

Prediction of surge heights under certain idealised boundary conditions has beun describc-d in the- literature. These methods have been applied to Australian conditions and a nomogram chart for design purposes has been prociuced. Details of a number of Australian cyclones and their associated surjes are included.

Particular coastal configuration can affect the surge characteristics quite markedly. The magnitude of those effects can be studied by a numerical model of the appropriate coastal region.

A numerical model of the coastal area (100 miles north and south of Townsville) is described. The dynamic equations for storm surges include terms for Coriolis effect, bed friction, wind shear, inverted barometer effects, rainfall and inertia. The equations are solved usinq an explicit leap-frog finite-difference technique within a space coordinate system parallel to latitude and longitude gridlines. The stability and sensitivity of the finite difference scheme and the appropriate boundary conditions for coastline configurations and tidal changes are discussed.

The model is described in terms of a standard cyclone with defined characteristics and for calibration purposes is tested by modelling cyclone 'Althea' (24. 12.71) for which the associated surge has been documented. US-VI-3 HURRICANE-OCEAN INTERACTION PROCESSES REVEALED BY THE 1973 HURRICANE SEASON FIELD PROGRAM A PRELIMINARY REPORT

Peter G. Black, R. Cecil Gentry National Hurricane Research Laboratory, NOAA, Miami, Florida, USA

Mark Goldstein International Business and Research, Inc. Coral Gables, Florida, USA

and

William G. Mai linger Weather Modification Program Office, NOAA, Miami, Florida, USA

An experiment has been designed to determine the immediate and long term response of the ocean .to a hurricane. Using a light aircraft, airborne expendable bathythermographs (AXBT) are planned to be dropped every 20-40 km along a baseline ahead of a hurricane and again at intervals of two days for up to two weeks, after the hurricane has passed the baseline. Using a NOAA hurricane reconnaissance aircraft, a sequence of larger AXBT's will be deployed on the 20-40 km space scale throughout the hurricane as it passes over the baseline.

It is hoped that the data will yield new answers to the questions of how the mixing and upwelling processes operate in hurricanes, how the ocean restores itself after the disturbing affects of a hurricane and how the disturbed ocean may affect the hurricane intensity. US-VI-4 PSEUDOGEOSTROPHIC APPROXIMATION TO THE BAROTROPIC VORT1CITY EQUATION, VALID COR THE EQUATORIAL ATMOSPHERE

S. Panchuv

Department of Metuorolony, University of Sofia, Bulgaria

Starting from the so-called balance equation

stream in which /_- ftjj V .-B/35 , A = V^ TU 6*VVS, V " '

function, Y' -geopotential, the Grimes' [JJ "pseudogeostrophic"

formulae are rederived: ,j

+ ^t is the ab.r>olutr vorticity and |!

f i is the energy function. From (2) we find [ t—: * (4) J

subject to the limitations I £F I < Of and \7 X \7C 0 <5 •

By introducing of (4) into the barotropic vorticits equation

\7 /• = ~^Vxt^ -~ V^£A , the latter is reduced to

In the equatorial atmosphere J ^ O / <^ -^ 0 and we %

F obtain A (VtF)-*2(jAF, F) ~A^ > AF>^» (6) I V The new equations (5) and (6) are of Poisson-type with | | respect to \Z r and for their solution can be used the numerical ft: <• Si technique developed for the analogous equation for the stream function ^ $ in quasisolenoidal approximation £ US-VI- 5 TROPICAL CLOUDS

M. J. Sonter

University of Papua, New Guinea

Tropical cloudscapes provide vivid illustrations of a

variety of processes. A series of slides will be presented

showing Cu-Nim development over the Astrolabe Ranges,

cellular convection patterns, shear-induced billows and lenticular

waves, cloudstreets and thermal bubbles, pileus cloud over low

cumulus, and a variety of less easily identifiable phenomena.

To what extent can visual observation give useful numerical

data?

'IK .i US-VI-6 THE CYCLIC ACTION OF THREE METEOROLOGICAL SYSTEMS IN NORTHEASTERN BRAZIL

D. M. Strang and R. G. Brophy

Instituto de Atividades Espaciais - CTA, Sao Jose dos Campos, S. P. , Brazil

A previous study of the pluviometric data of Northeastern Brazil, over the 30-year period, 1931-1960, indicated that three meteorological systems operate in a cyclic manner over this region. In an attempt at a further clarification of this assumption, radiosonde data from various stations within, and surrounding, the region were analyzed. Vertical profiles of the wind, humidity, temperature, and pressure, to the 100 millibar level, were examined. Preliminary analysis indicates that tho wind directions, humidity levels, and moisture transport tend to confirm the hypothesis, Following the end of the dry season in October, the tropical continental system predominates in the region to the south- west of the area of interest, strongly influencing the climatology of the region, particularJy during December. Interactions occur with this and the equatorial maritime system until the latter, influenced by Northern Hemisphere circulations, becomes the dominant force during the March-April period. Finally, the tropical maritime system, a resultant of the permanent high pressure area of the South AH antic Ocean, appears to force the return of the easterly wind flow pattern by June. This wind pattern normally exists throughout the dry season which usually commences in July. i* US- VI- 7

J EXTENSION OF THE EQUATORIAL WALKER CIRCULATION INTO r/ HIGH LATITUDES OF THE SOUTHERN HEMISPHERE

J. W. Zillman

Commonwealth Bureau cf Meteorology, Mel bourne, Aus tr al i a

The existence of large-scale east-west mass circulations in the equatorial troposphere is now fairly well established from analysed wind data and conventional thermodynamic arguments. This paper provides a view of the thermodynamic origin of the east-west ('Walker') circulation from the different standpoint gained by use of isentropic coordinates. The unique feature of the isentropic coordinate system which makes it particularly appropriate to the search for large-scale thermally-driven circulations on the rotating earth is the coupling between the horizontal mass flow and the distribution of diabatic heating which is inherent in the isentropic continuity equation. In this study a time-averaged form of the continuity equation is solved to give the distribution on isentropic surfaces of a mass transport potential. The 'thermally forced' zonai mass transport is then found from the east-west gradient of the potential. The diabatic heating fields which provide the forcing were modeled to simulate mean January and July conditions in isentropic coordinates. Though primary interest wys directed to mass circulations in the southern hemisphere, the solution included the entire tropical belt. The Inferred zonal circulation along the equator is in good agreement with the best estimates available from analysed wind data and the solution generally supports the established picture of at least two major zonal circulation cells with their common ascending branch north of Australia. On most isentropic surfaces the alternating belts of easterly and westerly mass flow associated with the equatorial circulation cells extend with comparable strength into high latitudes, even to the Antarctic. The interpretation to be presented is pertinent to the question of the mode of coupling between tropical and extratropical latitudes and the mechanism of the Southern Oscillation. US-VL-8 SHORT-PERIOD CLIMATIC FLUCTUATIONS IN GLOBAL SURFACE DATA PARAMETERS

J. W. Kideon

New Zealand Meteorological Service, Wellington, Now Zealand

A series of global analyses of surface pressure, temperature and rainfall has been made using mean monthly data from January 1951 to December I960. The resul ting analyses have been examined for evidence of coherent short-period climatic fluctuations through the use of empirical orthogonal functions. fn each case, less than JO components are required to account for the significant variation over the three 120-point grids for each hemisphere and the tropical belt. The major components reflect seasonal changes in the surface heating and land-sea contrasts.

No pressure pattern has been obtained which exactly matches current representations of the "Southern Oscillation" but certain pressure and rainfall components appear to be closely related to it.

A biennial oscillation is quite marked in the Northern Hemisphere from (955 onwards with a modulation in the intensity of the zonal circulation and all "centres of action" being most appearent in the winter months. Little evidence can be found in the present analyses for a biennial oscillation in the Southern Hemisphere. US-VX1-1 DERIVATION OF THE TEMPERATURE DEPENDENCE OF EQUILIBRIUM OZONE CONCENTRATION NEAR 50 KM ALTITUDE BY COMPARISON OF NIMBUS IV BUV AND SCR MEASUREMENTS us-vn

J. J, Barnett

Clarendon Laboratory, Oxford, U.K.

Measurements by channel A of the Selective Chopper Radiometer on Nimbus IV, which relate to the temperature of the 7. 5-0. 6 mb (33-52 km) layer of the atmosphere, are compared with retrievals of the ozone mixing ratio derived from measurements by the Backscatter Ultraviolet Spectrometer on the same satellite. Correlation and regression coefficients are used to show the relation between simultaneous values of the logarithm of ozone mixing ratio at a given, pressure and the reciprocal of channel A equivalent temperature, for different orbits but at the same latitude, local time (noon), and time of year. Results used were for 60 S and 45 S and 2 mu and 1 mb during 15 orbits on 4-6 September 1970, a time of large zonal temperature variation (- 17K) associated with pianetary waves and a sudden warming in the Southern Hemisphere. Correlation coefficients for 2 mil rxrocd 0. 95 at both latitudes and are 0. 84 and 0. (68 ior 1 mb at 45' S jiui 60 S. However, correlation of 1 mb ozone mixing ratios with SCR measurements from one orbit (26.8 ) further east gives improved coefficients of 0-96 and 0. 82. This is taken as evidence of the continuation above 2 mb of a westward tilt of the temperature anomally with increasing height observed at lower levels ti} other- channels of the SCR. Values of 3 log [O-] /d T are in the range 704-1134K. Consideration of dynamic factors and the theoretical photochemical time constant shows that, at le.i>-.| .)! 4f> S, these values represent the temperature iVperuie'n <• oi tin- ,»fieio chemical equilibrium mixinrj ratio, with j be^t er-tim.ite oi approximately 1100K. This value is consistent with that calculated by the classical oxygen model of the ozone equilibrium. Thr result is important in modelling the stratosphere and meso- spherc, since the variation of ozone concentration with temperature is a feedback mechanism which damps temperature perturbations. Elementary calculations give a decay time of 3. 3 days for perturbations at 50 km at the equator using the above value, compared with 5. 3 days for a temperature independent mixing ratio.

US-V1I-2 OZONE NEAR THE STRATOPAUSE

J. S. Randhawa Atmospheric Sciences Laboratory, US Army Electronics Command, White Sands Missile Range, New Mexico, U. S. A.

On 18 September 1972, a 38 million cubic foot balloon was launched from Holloman Air Force Base {32 51 N, 106 06 W) at 0404 local time. The balloon carried a pay load consisting of two chemi luminescent ozone detectors, a photometer for measurement of ultra violet flux, a mass spectrometer and detectors for temperature, pressure, water vapor, positive ion and Lyman «, . As the balloon rose to high altitudes, the whole payload was reeled down 400 meters to keep the instruments away from Us influence. The sunrise occurred on the balloon at about 40 km altitude and a decrease in ozone concentration was recorded at that level. The balloon floated for nearly three hours at an altitude of 48. 5 km and ozone was recorded continuously by two different techniques (chemiluminescent and photometric). The results obtained are in good agreement with each other. As the solar elevation increased the chemi luminescent sensor recorded a decrease in ozone concentration. A possible explanation for the change may be the diurnal temperature change at the stratopause level in addition to the increased photodissociation of ozone molecules by the penetrating solar radiation. US-VII-3 ROCKET MEASUREMENTS OF NOCTURNAL OZONE DENSITIES

J. H. Carver, B. H. Horton and R. S. O'Brien

Department of Physics, University of Adelaide, Adelaide, Australia

Nocturnal ozone densities, In the height range 30 - 70 kms,

have been measured from rockets usfng broad-band photometers In

the region of the Hartley absorption bands (2000A - 3000A). The

source of light was the solar radiation reflected from the moon.

The photometers consisted of photomultiplier tubes

mounted behind thin film interference filters - these photometers

0 O

had band passes of the order of 150A - 200A.

The results indicate that the ozone densities at night

range from 5 x 10lz molecules/cm 3 at 30 km to 5 x 109 molecules/cm 3 at 70 km. These results are consistent with those obtained by a variety of methods by other workers. US-VII-4 ON THE ESTIMATION OF STRATOSPHERIC NO- CONCENTRATIONS FROM PARACHUTE OROPSONDE MEASUREMENTS OF OZONE

Norman V. Sissons

Australian Defence Scientific Service, Department of Supply, Adelaide, South Australia

Parachute dropsonde measurements of the stratospheric ozone distribution below 60 km from Woomera (31 S) are presented.

These results are compared with ozone profiles measured from other locations.

A 1-dimensiona! photochemical model based on approximations adopted by Leov/y was extended to incorporate the catalytic removal of odd oxygen allotropes by nitrogen oxides as suggested by Crutzen and Nicolet. Ozone profiles were synthesized numerically to match experimental data by adjusting NO- concentrations below 50 km. The model contained vertical transport as parameterized by an eddy diffusion coefficient and operated for )0 simulated days for the sun fixed either at 50 or 0 zenith angle.

The peak NO- mixing ratio was located at 35 km for mid- latitude examples and the NO_ mixfng ratio profile agreed closely with that determined by Ackerman andMulfer for altitudes between 28 km and 20 km. : • ''

Above 20 km, the derived NO. columan densities varied from 5. 5 x 10 to 8. 0 x 10 molecules cm" |Sec * = 1.6) compared with the recent experimental estimate of 5 x 10 molecules cm" by Harries. US-VII-5 THE USE OF ULTRAVIOLET RADIATION DATA TO DETERMINE THE PHOTOD1SSOCIATION RATE CONSTANT OF NO,

James T. Peterson

Environmental Protection Agency, National Environmental Research Center, Research Triangle Park-, North Carolina, U.S.A.

An essential parameter ot most photochemical pollution models for urban areas is the rate constant {k ) for the photodissociation of nitrogen dioxide (NO ). The variability of k in time and space basically depends on the variability of the actinic irradiance; i.e., the photochemicaHy active ultraviolet (UV) energy incident on a molecule of NO- as a function of wavelength. This paper presents methods whereby k. can be routinely determined from either measurements or theoretical calculations of ultraviolet radiation.

Field experiments to gather dala for photochemical model verification and development typically have relied on broad-band, horizontally oriented UV radiometers to measure incident irradiance. An empirical scheme to convert such data to actinic irradiance is presented herein. It is based on the spectral distribution of UV radiation, its partition into direct and diffuse components.and a" estimate of the effective zenith an^jle cf the scattered energy. The author's measurements, made during clear and-hazy conditions at various solar angles, are used to determine typical values of these variables. The direct and diffuse components of UV energy were measured by a filter wheel instrument with 100 A resolution. The diffuse radiation intensity over the upper hemisphere was observed by a collimated UV photometer. k was then calculated from the

actinic irradiance by using values of NOO absorption coefficient and photodissociation quantum yielrf.

Another method for determining k is described which is applicable for estimates of k on very dear days or at the top of a polluted atmospheric layer. Jt utilizes the theoretical, multiple- scatter calculations of Diermendjian and Sekera and assumes UV attenuation by Rayieigh scattering and stratospheric ozone absorption only. Values of actinic irradiance are calculated as a function of wavelength, solar elevation and ground albeao, and from these k. is determined. Although results are presented only for cloud-free conditions, a technique to account for variable cloudiness is also discussed. Values of k. determined from several broadband UV measurements during clear atmospheric conditions are compared with corresponding results from the theoretical scheme. In addition, data from the empirical technique are compared with those from other methods suggested in the literature. Finally, the dependence of k, on soJar elevation, cloudiness and haze amount is discussed. US-VII-6 THE ASPENDALE ATMOSPHERIC CARBON DIOXIDE MONITORING PROGRAMME - TWO YEARS OF DATA

G. I. Pearman and J. R. Garratt

CSIRO, Division of Atmospheric Physics, Aspendale, Victoria, Australia

The CSIPO (Australia) baseline atmospheric CO. monitoring programme was initiated in early 1972 to provide Southern Herrisphere mid-latitude data not previously available, and is based on the collection of discreet air samples (in glass flasks) from aircraft over S. E. Australia and nearby ocean areas. The present paper summarises the measurements made in the first two years, with particular emphasis on the space and time variations of CO, throughout the troposphere. The latter provide information on the Jarge scale movement of CO through the atmosphere and between atmosphere and surface.

The variation of CO_ concentration with height through the troposphere shows a distinct seasonal variation, increasing with height during winter and decreasing during summer. The vertical gradients imply, for a large scale vertical eddy diffusjvity of 2 x 10 cm s" , vertical fluxes of magnitude 10 g cm s , positive (downwards) in winter and negative in summer. They are comparable both in magnitude and sign with the exchange rate of CO_ between ocean and atmosphere due to the seasonal variation In ocean surface temperature and hence CO- solubility in water. Data from the iower stratosphere indicate vertical differences ~ 1 p. p. m. across the tropopause, but are too few to indicate a relation with tropospheric vertical ,ariations.

The seasonal variation of the mean CO. content at 4 km has an amplitude ~ 1 p. p. m., whilst that at 10 km *s near zero. Thr times of maximurr and minimum are close to those for the South Pole but are five months delayed relative to those in the Northern Hemisphere (the seasonal amplitude is an order of magnitude smaller south of the equator). The 40 S seasonal cycle is interpreted in tertrs of the North-South meridional transfer of the 45 -70 N seasonal cycle, related to the photosynthetic activity of vegetation in that latitude, band. . The implied large scale meridional eddy diffusivity ~ 10 cm s is realistic for trans-equatorial transfer.

Evidencefor a secular change in CO. concentration at 4f S is discussed and compared to the known changes occurring in the Northern Hemisphere and at the South Pole. US-VII-7 TRACE SUBSTANCES IN THE TROPOSPHERE

Ian E. Galbelly

CSIRO Division of Atmospheric Physics, Aspendale Victoria, Australia

There are very few measurements of nitric oxide and

nitrogen dioxide in the' background atmosphere. One year of

measurements at Aspendale are sorted according to air trajectory.

Measurements on those occasions when the airflow is from Bass

Strait and the Southern Ocean give some estimate of the back-

ground concentration of oxides and nitrogen in the troposphere.

Associated measurements of ozone in the surface air are examined for correlation w'th the oxides of nitrogen measurements. us-vn-e CLIMATIC FLUCTUATIONS AND LONG RANGE TRANSPORT OF PARTICLES AS INFERRED FROM THE CHEMISTRY OF PRECIPITATION

M. P. Paterson

Department of Mathematics, Imperial College of Science & Technology, London, England

The near field deposition of particulates by the atmosphere Js governed by the source characteristics. With man-made pollutants, such as heavy metals bearing particles, this form of deposition can be controlled by the engineering design of the source. The distant field deposition, which happens at much lower concentrations, is controlled by meteorological factors and can be influenced only by our choice of the total quantities emitted. In the case of sulphate particles the deposition at great distances is at present a matter of controversy. Of greater importance is the transport of a number of species of particles from large land area sources which are dominated by our agricultural methods.

The study of long range transport of some natural particulates casts light on the properties of the atmosphere which also control the distant field deposition of man-made particles. The data collected by the European Atmospheric Chemistry Network, the longest- lived series of such observations, permits estimates to be made of the long range transport of calcium, magnesium, potassium and sodium. Each of these elements has its natural sources and a characteristic dispersion and deposition pattern, both in geographical distribution and in time of year. These patterns, as observed with a network of inland stations in Scandanavia, are discussed and the transport over long distances estimated. Climatic fluctuations can greatly influence such transport. In regions where the supply of the various chemical species by the atmosphere is a substantial fraction of the total annual suppiy a very modest change in the tropospheric circulation may result in a large and biologically significant change in the supply.

Large fluctuations in the transport and deposition of acidic compounds in western Europe have been recorded by the European Atmospheric Chemistry Network. If the source of such compounds is the sulphur In fossil fueis it is evident that the climatic fluctuations will contribute more to the future variation in deposition than will any increases in fuel use. CR-1-1

THE STRUCTURE AND DYNAMICS OF CLOUDS CR-I

P. Squires

Desert Research Institute, University of Nevada System, Reno, Nevada, U. S. A.

A discussion of the processes leading to cloud formation, and of the factors which influence their growth and decay. These include precipitation formation and turbulent mixing with adjacent volumes of dry air. Cloud microstructure and precipitation processes are largely influenced by the properties of the pre- existing aerosol, as well as by the dynamics of the cloud process itself; on the other hand, the economy of the aerosol is largely determined by precipitation processes which are largely responsible; for atmospheric cleansing. CR-t-2 REVIEW PAPER ON THE COUPLING BETWEEN CLOUDS, RADIATION FIELDS AND DYNAMIC PROCESSES

S. Twomey

Institute of Atmospheric Physics, University of Arizona, Tucson, Arizona, U.S.A.

A survey of the literature shows that radiative effects

have been invoked as important contributors or even primary causes

of cloud formation. The more important of thase suggestions (some

of which go back almost half a century) will be outlined. The results of measurements and theoretical or numerical calculations reJating

to such questions which have already been made will be reviewed and the discrepancies or disagreements (which unfortunately are numerous) pointed out. An attempt will be made to identify the measurements and theoretical work which needs to be done to clarify some of the questions raised. "~ ' CR-I-3

DETERMINATION OF THE COMPLEX REFRACTIVE INDEX AND SIZE DISTRIBUTION PARAMETERS OF CLOUDS AND AEROSOLS

CR-I

Alain L. Fymat

Jet Propulsion Laboratory, California Institute of Technology, Pasadena, California, U.S.A.

Discussion of an extensive series of numerical experiments aimed at demonstrating the capabilities of the author's Minimization Search Method in retrieving the complex index of refraction and the model parameters of typical size distributions from scattering measurements. Examples treated will include, in particular, the determination of: (i) the real refractive index and the radius of a single particle or of a monodispersion from the ratios at two distinct wavelengths of the scattered intensities in the forward and backward directions or near these directions (a test of an earlier proposal of van de Hulst, 1957, and its extensions to near forward and near backward directions and to values of the product, refractive index x size parameter, considerably larger than the prescribed value of 0.8); (Ii) the complex refractive index from single scattering on Mie poly- dispersfons typical of terrestrial and Venusian conditions utilizing either of the two states of orthogonal polarization, or the total intensity, or the degree of linear polarization of light scattered within a 10 (approx.) forward cone (a complement to the works of Shifrin et al. , 1955-69, and the author, 1972, aimed at reconstructing the size distributicn from diffracted light). CR-I-4 INTERIOR RADIANCES IN OPTICALLY DEEP ABSORBING MEDIA

Gilbert N. Plass, George W. Kattawar, Stephen J. Hitzfelder

Physics Department, Texas A&M University, College Station, Texas, U.S.A.

The interior radiances are calculated by the matrix operator method within an optically deep absorbing medium scattering according to the Rayleigh or the haze L phase functions. The results for the radiance and flux are presented for a range of solar zenith angles and for single scattering albedos from 1 to 0. 1. The development of the asymptotic angular distribution of the radiance is illustrated. It is shown that this asymptotic distri-

bution is probably physically unobservable when u0 <. 0. 8, since the flux is less than 10 of its original value at the beginning of the asymptotic region. The ratio of the upward to downward flux is calculated and is shown to be remarkably constant within the medium except very close to the boundaries. The heating rate within the medium is found to be verynearly proportional to the downward flux, except near the boundaries. When the single scattering albedo is small, the direct solar flux makes a significant contribution to the total flux even at great optical depths within the medium. The total downward flux decreases exponentially with optical depth away from boundaries when the single scattering albedo is greater than or equal to 0. 9; when it is less than or equal to 0. 5 only an approximate exponential fit can be obtained within the region accessible to experimental observation. The variation of the polarization of the reflected and transmitted radiation as a function of the thickness of the cloud layer is discussed. The variation of the Babinet, Brewster, and Arago points with the optical thickness of a Rayleigh or haze L atmosphere is illustrated. CR-I-5 RADIATIVE HEAT GAIN IN WATER CLOUDS UNDER INFLUENCE OF SOLAR RADIATION

Giiohi Yamamoto, Masayuki Tanaka and Shoji Asano

Geophysical Institute, Tohoku University, Sendai, Japan

As an extension of our previous paper on "Radiative

Heat Transfer in Water Clouds by Infrared Radiation11 (J. Quant.

Spectrosc. Radiat. Transfer, \), 697-708), radiative ht?at pnin at each level inside clouds due to absorption of the near infrared solar radiation is estimated, taking into account radiative processes due to both cloud droplets and gaseous constituents. CR-I-6 ABSORPTION OF SOLAR RADIATION JN A CLOUDY ATMOSPHERE ABOVE THE OCEAN

Ehrhard Raschke

Universitat Koln, Federal Republic of Germany

In this paper results of multiple scattering calculations

of the transfer of solar radiation between 0. 25 and 3. 2B.A4-IT in a

realistic model of the atmosphere - ocean system are discussed.

The computational method is based or an iterative solution of the

radiative transfer equation, which allows to account for aniso-

tropical scattering and absorption in both media.

The model of the atmosphere is based on ELTERMAN's

(1968) vertical profiles of dust, molecule and ozone extinction coefficients with additional absorption by water vapor and carbon dioxide and extinction by various cloud layers.

The results indicate a very strong absorption by atmospheric aerosols in the atmosphere accounting for up to 50 percent of total solar heating. The cloud layers alter according to their position and optical thickness significantly the structures of vertical profiles of radiative flux divergencies. They cause some additional radiative heating in the lower stratosphere. CR-I-7

INFLUENCE OF CLOUDS ON SOLAR RADIATION AND ITS SPECTRAL COMPOSITION

Guy A. Franceschini

Dept. of Meteorology, Texas A&M University, College Station, Texas, U.S.A.

Clouds serve as thermal Insulators of the surface of Earth. In this role they cause a reduction in radiation lost by the surface, as well as a reduction in solar energy made available to the surface. However, there are times when insolation at a point may be larger than the clear-sky value due to multiple scattering and reflection by clouds. In addition, clouds serve to change the spectral composition of solar radiation received near the surface.

The role of different cloud types in reducing, enhancing and changing the quality of insolation will be discussed. Results are based on measurements made aboard research vessels in the polar regions of the South Pacific and Indian Oceans, and in the Gulf of Mexico. Standard hemispheric pyranometers were employed. Four wavebands were treated: blue, 260-500 nm; green, 500-630 nm; red, 630-700 nm; and Infrared, 700-2, 800 nm.

In general, decreases in Insolation ranged from 13 to 26 percent with cirrus, and from 65 to 97 percent with cumulonimbus. Increases In insolation ranged from 4 to 6 percent with cirrus, and from 12 to 38 percent with cumulonimbus. Under overcast conditions, the fraction of the flux contained in the infrared b3nd was cons is tentU : smaller, ofler "n excess of 20 r

30 percent. These rrzet' J-™3 c'.'-re •i>-\-jl*. wvi.-" \.i- t-i? f>\,ovc" * with solar attitude, were generally sirader with ^tratocumuius clouds than with stratus and altocumulus. Calculated values of the gross fractional extinction by stratus were found to be a maximum, r. e., 82 percent, in the ir-band, and 66 percent in the blue band. For stratocumulus, extinctions were 75 percent in the infrared, and 60 percent In the blue. Minimum extinctions were found with altocumulus, viz., 70 percent in the infrared, and 42 percent in the blue band. Lesser changes in the green and red bands were noted. CR-I-8 ATMOSPHERIC RADIATION AS IT EFFECTS THE CHARACTER OF CLOUD

G. W. Paltridge

CSIRO, Division of Atmospheric Physics, Aspendale, Victoria, Australia

It is shown how radiation may be a dominant control on the thickness, water content, rate of dissipation and rate of formation of many types of stratiform cloud. Two situations are discussed. The first is of low-level radiatively-cooled strato- cumuius over the sea at the base of an inversion and the second is of high-altitude radiatively-warmed cirrus. Both situations involve a feedback mechanism dealing with instability caused by radiative energy exchange, consequent turbulence and entrsinment of dry air, and finally release of latent heat which may amplify the original instability. The model of stratocumulus predicts stable equilibrium cloud thickness and water content controlled by the radiative cooling - for instance daytime shortwave heating should lead to thicker cloud. It predicts also that explosive penetration of the inversion will occur when the local mixing ratio difference across the inversion exceeds about 7-8 g/kg. The model of cirrus again suggests how mean thickness may be determined by radiative warming. 6 CR-It-1 EFFECTS OF CLOUDS ON THE RADIATIVE HEAT EXCHANGE IN THE ATMOSPHERE ^ CRII

E. Feigelson

Institute of Atmospheric Physics, Pyzhevsky 3, Moscow, U. S. S. R.

Specific features of long-wave radiative cooling out of the atmosphere under the conditions of stratified clouds are described. The description is based on the experimental and theoretical data.

The wave lengths of photons in clouds due to multiple scattering are considered. The knowledge of these wa^s and of the integral transmission function for the near infra-red radiation makes ?t possible to give a method for simple evaluations of the heating of the cloudy atmosphere by solar radiation.

The results of an investigation of the statistical structure of the radiative fluxes with cumuli clouds are given according to the experimental and theoretical data.

The possibility is considered of the evaluation of cloud amount with the aid of the fluxes measurements.

The solution of a theoretical problem is given on the coupling of heat and moisture exchange with clouds as a feed-back regulator. CR-II-2 EFFECTS OF CLOUD PATTERNS ON THE RADIATIVE COMPONENT OF THE ENERGY BUDGET

Professor Stephen K. Cox

Department of Atmospheric Science, Colorado State University, Fort Collins, Colorado, U.S.A.

A single cloud of large areal extent may have signi-

ficantly different effects on the radiation field than many smaller

clouds, the sum of whose areas is the same as the area of the single, larger cloud. This effect will be illustrated with numerical results obtained from a Monte Carlo computation. It

Is suggested that this difference was, in part, responsible for high planetary albedo estimates in the pre-satellite era.

A brief review of experimental techniques used to establish the radiative component of the energy budget in the presence of clouds will be given. Proposed techniques for this determination in GATE will be mentioned and their relative merits and disadvantages wiil be discussed.

Illustrations of various configurations of radiative heating and cooling by different cloud types and patterns will be given. A short review of literature reporting coupling between radiation fields influenced by clouds and atmospheric dynamics will be discussed. THE CALCULATION OF INFRARED RADIATIVE COOLING RATES INCLUDING THE EFFECTS OF WATER AEROSOLS

R. D. Hoy

Commonwealth Bureau of Meteorology, Melbourne, Australia

The variation of aerosol absorption and scattering

cross sections in the infrared is discussed for various radius

ranges of aerosols with a Junge size distribution. Aerosols

with radii between 0. 1 and 4 microns appear to be most signifi-

cant for infrared radiation transfer, depending partly on the

Junge size distribution slope. Aerosols may be considered to

act radiatively as water spheres for relative humidities greater

than 70% and this allows an approximate relation between the

concentration of aerosol water and an equivalent amount of water vapour. This enables water aerosols to be included in radiation chart calculations for determining radiative cooling rates. CR-II-6 EFFECT OF CLOUDS AND PARTICULATES ON THE TERRESTRIAL RADIATIVE FLUXES OVER INDIA

A. Mani, R, R. Kelkar and V. Srinivasan, India Meteorological Department, New Delhi and Poona, India

Results of rreasu-ements of infrared -ao/atVe fiuxes, ^ e so^cer c*~'-*g 1£"1-73, ---ade at trree stat'o-s 'Cjghu a'org the 75"E ms-ic^", at Trivanc^um, Poor.a arc New De'.'nl, S , 18 and 23 norm of the equator ere presented.

The natural division of the year over north and central India into mafnly dry, cloudless winters, dry. dustrv,, cloudless summers and cloudy monsoon months enables one to study independently the effect of dust, water vapour and cloud on the radiative fluxes and on the radiative cooling and warming rates in the atmosphere.

The largest contribution to the infrared cooling comes from water vapour. In winter the maximum water vapour concentration in the lower levels of thi> atmosphere over India lies o\/er the equatorial region with the lowest values over northwest India. In Juiy the situation is reversed with the maximum over north and northwest India and the minimum over the equator. This reversal arises from the large seasonal changes in the vapour mixing ratio. For example, at the 850 mb level the values over northern India vary from 3 to 16 gm/kgm, while over the equator the values remain more or less constant at about 10-12 gm/kgm.

The distribution of total cloud amount over India also shows variation similar to that of water vapour. During January - April, the total cloud amount is 3 octas or less over most of central India, with slightly higher amounts in the north and south. In July when the monsoon Is established over almost the whole of India, cloud cover exceeds 6 octas throughout India, except in the northwest. High values of the order of 5-6 octas persist over south India in October with values diminishing rapidly to almost zero in the northwest.

The observed values of net flux and cooling rate at various levels were compared with numerical computations made with a mode) which incorporated the effects of water vapour, CO_, ozone and clouds but no dust. It was possible to isolate the effect of dust on the radiative cooling by using this model for New Delhi and Poona in the pre-monsoon period when dust concentration is pronounced. The same model, used for all the three stations, with data for the monsoon season but with the assumption of a cloud-free atmosphere yielded the effect of ctoud layers. ^:f CR-I1-7

^SATELLITE MEASUREMENTS OF THE INTERANNUAL VARIATION OF THE ^EQUATOR-TO-POLE RADIATION GRADIENT, RESPONSE OF THE LARGE ATMOSPHERIC CIRCULATION, AND THE EFFECT OF CLOUDS

,1 Thomas Vonder Haar and James Ellis

V'* Department of Atmospheric Sciences, j&- Colorado State University, Fort Collins, Colorado, U.S.A.

*| Interannuai variations o* £.">e

With the mean annual cycle removed there is an apparent 3 to 6 month lag between equator-to-pole radiation gradient and such large scale circulation parameters as thermal wind, eddy available potential energy and zonal kinetic energy. The satellite data are shown to have good signal above instrument noise for this application although possibilities for improved measurements will be discussed. Interpretation of the results from both hemispheres Includes discussion of the non-reciprocity of planetary albedo and infrared radiant exitance arising from varying cloud fields. CR-ii-e HIGH RESOLUTION GLOBAL RADIATION SOURCES AND FLUXES

James E. Lovill

Lawrence Livermore Laboratory, University of California, Livermore, California, U.S.A.

The measurement of the heat flux over the entire globe at frequent intervals to a high degree of resolution is highly desirable for a great variety of problems that relate to the atmospheric interaction with sea and land surfaces. This paper will describe a system that is now available to perform measurements of this type from 0. 4 to 1. 0 m/u {the visible and near infrared region of the spectrum).

The data that will be discussed were obtained from an operational Air Force satellite that, over the night sector of the globe, highly amplifies radiation in the 0. 4 to 1.0 mu spectral interval. For operational purposes, clouds are made visible during all but the new moon lunar phase.

High resolution examples (to 3200 meters) will be presented of a night volcanic eruption and an estimation of the energy measured during successive days wil! be given. Several regions of gas flaring of oil wells will be shown. Examples of night observations of radiation over Australia and the western U. S., with special emphasis on Sydney, Melbourne, and the San Francisco Bay Area, will be correlated with inversions and cloud {ice and water) over the regions.

A discussion will be given of the program to measure global heat sources and fluxes (from the large- to near micro-scale) by scientists at the Lawrence Livermore Laboratory. CR-1I-9

HIGH CLOUDS AND THE CLIMATE

CM. R. Platt

CSIRO, Division of Atmospheric Physics, Aspendale, Victoria, Australia

Detailed and average longwave emissivities and

shortwave albedos of some mid-latitude cirrus and cirro-

stratus cloud systems have been calculated from experimentally-

determined values of their infrared emissivities at lO^tun to

12 jyjn, shortwave optical thicknesses at 0. 694/*wn, their altitudes and their temperatures and their depths and density variations. Shortwave absorption by the clouds is estimated.

Heating rates within the clouds are calculated and the effect of the high cloud systems on the radiative equilibrium of the earth and atmosphere is discussed. CR-II- 1 0 EFFECT OF CLOUD COVER ON THE WINTER TEMPERATURE AT FAIRBANKS, ALASKA

K. O. L. F. Jayaweera and G. Wendler

Geophysical Institute, University of Alaska, Fairbanks, Alaska

During the winter months, the polar regions receive little or no solar radiation. Therefore the outgoing long wave radiation from the surface tend to decrease the surface temperature unless advection brings in sensible heat or a cloud cover so that the back radiation from the cloud compensate the loss by the ground. In this paper we discuss the relationship between the presence and absance of low cloud on the surface temperature of Fairbanks, Alaska. The station represents atypical valley station in the continental Arctic. In addition to discussing the effect of cloud cover on the temperature, efforts to produce an artificial cloud with the intention of inhibiting the radiative cooling will be discussed.

Under the clear skies the temperature of Fairbanks decreases steadily and leads to the formation of strong surface inversions. Graphs will be shown to illustrate the cooling at 2. 5 cm, 1, 4, 8, 16 and 200 m levels.

The increase of the 1 m air temperature of Fairbanks when the sky is completely cloud covered after a clear period is discussed. Here only cases of low clouds {below 7000 ft. cloud base) and 100% cloud cover will be considered. The increase in surface temperature is plotted as a function of time with cloud base temperatures grouped in S C ranges varying from 0 to -30 C.

The theory and experiments to generate artificial clouds over an area under clear sky so as to inhibit radiative cooling are discussed. The results of the 1972-73 experiments showing the number of occasions suitable conditions existed for forming artificial clouds and the radiation effects of these clouds will also be discussed. SB-I-1

NEAR-SURFACE CO- CONCENTRATIONS OVER LAND At SB I

;, O. T. Denmead

:* CSIRO, Division of Environmental Mechanics, f..*~ Canberra, Australia

Studies of carbon dioxide exchange by vegetated land surfaces in recent years have provided some documentation of near- surface atmospheric CO. concentrations in rural areas. These measurements show marRed seasonal, day-to-day and diurnal variation in CO. concentration for a number of reasons, including: seasonal and diurnal variation in CO. uptake and release by plant communities; variations in the extent of atmospheric mixing; and changes in the trajectories of air masses over land. They are thus only of limited use for examining secular trends in the global atmospheric CO« concentration; but they do provide some insight into the effects of vegetated land masses on the global CO. balance. Moreover, they have considerable practical interest in studies of plant cirowth in the field since measurements of CO, uptake b\ plants in control Ied environment chambers have shown a*strong linear relation between the rate of photosysthesis and the ambient CO. concentration.

Field measurements in the U.S.A. , Australia and Europe have shown that in periods of active vegetative growth, the average minimum CO- concentration near the land surface over periods of some weeks may be 40 to 50 ppm (ess than the free atmosphere value with extreme depletions of as much as 80 ppm. . Day to day variations in the minimum CO, concentrations attained have been found to be as much as 50 ppm. Examples from a number of sources will be given.

tn addition, an analysis will be presented of the two- dimensional transport of CO. over land. It takes into account the effects of the ambient concentration on the uptake of CO by vegetation, and attempts to predict the effects of photosynthesis and distance of transport on the surface CO concentration ami the surface CO_ exchange rate. These predictions will be compared with measurements of near-surface CO. concentration for orcisNuis on which the trajectories of air have been r.-ilrulatcil, nn

J. R. Garratt and G. I. Pearman

CSIRO, Division of Atmospheric Physics, Aspendale, Victoria, Australia

Observations of the horizontal and vertical variations of carbon dioxide concentration in the atmospheric boundary layer, together with time variations on a day-to-day and seasonal basis, are described. Such variations show a dependence on the previous history of the air mass, upon the horizontal medium scale variations in the surface-atmosphere vertical flux of CO (F ) and on the time scale for which F acts on the air mass. ' For instance, air moving frorr sea to (and is depleted in near-surface CO_ {mid-day values) by **- 10 p. p.m. for t(time) ~ 1 day {i.e. x(borizontal distance) ~ 500 km) for land acting as a surface sink. At 1-2 km this is reduced to ~ 1 p. p. m.

The above observations are generally consistent with a simple boundary layer model utilising the two dimensional diffusion equation which can be used to predict changes In the vertical CO. profile due to surface flux variations. In the model the time scale of interaction Is limited to t < 1-2 days, since effective mixing of the boundary layer with the free atmosphere generally occurs at times greater than this, and so places an upper limit on the near surface depletion or accumulation.

The observations are consistent with taking F *- 1-2 x \O g^cm" s~ , K (vertical eddy diffusivity) -v 10-10 cm s and boundary layer depth

J SB-I-3

LOCAL STRUCTURE OF DUST STORMS AND VERTICAL- DISTRIBUTION OF DUST SB-I

G.I. Barenblatt and G. S. Golitsyn

Institute of Mechanics of Moscow State University, Institute of Atmospheric Physics of Academy of Sciences of USSR, Moscow, U. S. S. R.

Dust storms are one of the effective sources of aerosols for the atmosphere. In many regions of the Earth the^ are a natural calamity. They transfer large amounts of dust and frequently are accompanied by very strong winds. The quantitative theory of this phenomenon Is practically undeveloped. Hwere we try to describe the local structure of a mature dus! storm when the mot ion of a tlow with dust can be considered as st3tionary. Usina :viu;u:.i.-> i a\ in- equations for a fluid with a heavy pollutant and taking into account the thermal stratification we obtain vertical profiles of wind, concentration and temperature. The non-dimensional parameters which determine the structure of the flow are the Richardson and the Kolmogorov flux numbers, the latter describing the part of turbulent energy spent on suspension of heavy particles. The work rolatod to the suspension is always positive, which results in a decrease o' tin* turbulent energy and this increases the stability of the flow. There- fore, other conditions being equal, the flow is accelerated. Obser- vational data are presented which confirm this effect. There is a self-limilar singular solution describing the saturated flow with the largest possible amount of dust. Other solutions approach this limiting one with increasing altitude. It is shown that the finer the dust, the slower its concentration decreases with height. The role of the thermal stratification for the determination of the flow structure increases its importance with height. Under the thermally stable conditions the dust concentration decreases exponentially with height while under the convective conditions it approaches a constant value. SB-I-4 ON THE DISTINGUISHING FEATURES OF A TURBULENT REGIME IN A FOREST CANOPY

A. S. Dubov, L..P. Bykova, S. V. Marunich

Main Geophysical Observatory, Leningrad, U. S.S. R.

The results of measurements of the mean values and fluctuations of wind velocity at a 42 m mast installed in a fir-wood with average tree height of 26 m are presented. It is shown that under neutral stratification conditions the roughness parameter of a horizontally homogeneous forest increases with wind velocity, and the height of displacement decreases.

The profiles of tangential stress, dispersions of wind speed pulsations and the speed of turbulent energy dissipation both inside the forest and over it are given. The logarithmic wind profile and the constancy of tangential stress with height, as well as the invariability of the relations between the dispersions of wind velocity components pulsations and the square of dynamic velocity are only fulfilled in the layers higher than (1.2 - 1. 3) h where h is tree height.

The spectral density of horizontal wind gusts averaged over 43 cases has been obtained. Unlike the similar data over a plain, here two parts of spectrum correspond to a "-5/3" law and are separated by a narrow transitional zone of wave length of the order of distances between trees. An assumption is expressed that near the tree crowns the energy transfer to disturbances of comparatively small scales is carried out not only through the usual cascade mechanism from disturbances of large scale to smaller ones, but also through direct fragmentation of large atmospheric vortexes against tree crowns.

The non-linear system of equations suggested by G.V, Menzhulin is solved numerically for the mean profiles of wind velocities and such characteristics as the turbulent exchange coefficient, the turbulence energy, the components of the turbulence energy balance equation both inside the forest canopy and through the whole thickness of boundary layer over the forest. The calculations have shown, in particular, a considerable turn of the wind velocity vector inside the forest canopy, which is confirmed by the data of natural observations made by Smith, Carson and Oliver. The above-mentioned system of equations with the addition of components characterizing the horizontal non-homogeneity is used for studying the transformation of air when it flows through a wind- break. To close the system of equations in this case the relationship for mixing path is used that was suggested at one time by Kholmogorov and widely used in the works by Rotta.

SB-I-5 TIME VARIABILITY OF TURBULENT FLUXES ABOVE A WHEAT CROP

E. F. Bradley

CSIRO Division of Environmental Mechanics, Canberra, Australia

The statistical variability inherent in turbulent flux measurement creates a sampling problem which is overcome, in most micro-meteorological investigations, h\ integrating ,i substantial body of data. Observations normally est«v>»i ,^ ,M- st«\ «*>-.I weeks, at a site carefully chosen for relatively constant Mirt.K c conditions. In many agricultural studies, however, smh suu.ion.u-v conditions do not exist. As crops develop, their characteristics for exchange of heat, water vapour, CO- and momentum change progressively. Furthermore, short-term variations in the fluxes are of interest and Importance. Examples arez the contribution to transport, within the crop, of low-frequency gusts; the influence of stow stomatal oscillations on the fluxes of water vapour and CO ; the effect of intermittent sun on the heat exchange and metabolic response of the crop as a whole. In another context, observations of momentum bursts and thermal plumes have been reported and attempts made to relate these to real physical mechanisms. Transient behaviour of the fluxes is obviously most complicated during the rapid change of stability regime at morning and evening. 6&-I-5 Integral (gradient) methods fail to measure this short-term variability of the fluxes in sufficient detail to penetrate the basic mechanisms involved. On the other hand the "direct" fast-response eddy-flux method may also fail to resolve the phenomena because of the sampling problem noted above. In this paper we examine time- serfes measurements of heat and momentum fluxes using sonic anenometers at two heights above a wheat crop, to determine the significance of apparent short-term divergence of the fluxes. Com- parisons with Bowen ratio-energy balance measurements establish that half-hourly averages are in good agreement over a wide range of values.

It is also demonstrated that the so-called structure function method of analysis produces values for the turbulent shear stress which agree with those determined by direct eddy-correlation and from a low-level drag coefficient. Involving only the fluctuations of horizontal velocity (but invoking some arguable assumptions) the method avoids the exacting orientation requirements of the eddy- correlation and the vexed question of determination of the length parameters z and d in the wind equation. At the same time, the analogous determinations of heat flux produce values systematically one-half those of the eddy-correlation and energy balance methods. The reasons for the discrepancy are as yet unexplained.

Observations of the time-variability of turbulent fluxes of water vapour and CO- over a young wheat crop are also presented. SB-I-6 THE ACCUMULATION OF RADON DAUGHTERS AND AJTKEN PARTICLES ON TOBACCO TRICHOMES AND VEGETATION SURFACES: IMPLICATIONS TO PLANT CONTAMINATION AND HEALTH

E.A. Martell

National Center for Atmospheric Research, Boulder, Colorado, U.S.A.

Radioactive daughters of atmospheric radon become attached preferentially to Aitken particles, particles to. 1 JJ radius, resulting in high specific activity of 21(Pb on such particles. The latter accum- ulate by Brownlan capture on the sticky exudate coating of the glandular heads of trichomes on tobacco leaf surfaces. The measured 2 J °Pb activity of individual trichomes from North Caroline flue-cured tobacco -6 ' is ~ 3 x 10 pCi per trichome. Curing and combustion of exudate produces highly insoluble material which is enriched in z ! *Pb. When inhaled and deposited in the bronchi of smokers, exudate particles should persist and allow ingrowth of aPo. The cumulative alpha radiation dose from such particles, an estimated 100 rem or more for 20 years of exposure, may account for the incidence of bonchial cancer among smokers. The measurement of 2 1 'po,2 l0Bi and 2 ' aPb on vegetation surfaces provides means of assessing the accumulation and residence times of submicron aerosols on vegetation surfaces. The results are applicable to the behavior of natural and pollutant aerosols of similar particle size range. The results for tobacco shed some light on the origin and distribution of tobacco mosaic virus. sB-n-i A MICRO-METEOROLOGICAL ANALOGUE NETWORK SB-II

P. Schwerdtfeger

Flinders University, Bedford Park, South Australia

The fluxes that determine the terrestrial energy balance near the surface of the earth can be summarized by a set of climat- onomical equations first suggested by Lettau and latterly also developed by others. One approach is to consider the net solar radiation as a forcing function to which the magnitudes and phases of the other boundary layer fluxes can be referred and indeed calculated if conditions are'adequately specified. It is probable that the main interest )ies in the diurnal and annual frequency components of these fluxes.

Although the solutions can be found numerically, the form of the equations suggests that an electrical analogue could be of great instructional value as well as operational simplicity. The one-dimensional analogue network which has been developed includes circuits for the simulation of solar and infra-red radiation, the latter responding as required to the fourth power of the surface temperature, heat conduction in the ground as well as sensible heating of the atmosphere and evaporation, which require the facility for responding to atmospheric stability.

In addition to providing information on the actual fluxes, the temperature at any point (and time), in the ground or atmosphere included in the range of simulation is available. By means of a visual display, almost instantaneous results are available so that the micro-meteorological consequences of boundary layer modification, inciuding albedo changes can be appreciated quickly. There appears to be some scope for application in assessing activities which have a physical impact on the environment. SB-II-2 PHYTOMETEOROL.OGICAL PROCESS MODELLING

G. V. Menzhulin

U. S. S. R.

Meteorological conditions in the plant community is a problem of some importance in ecology. Investigations of this problem have an obvious agronomical significance. Finally, the study of energy and mass exchange in vegetation reveals the properties of a "canopy" as a natural underlying surface. These are essential for solving-a number of meteorological problems and those of the physics of atmospheric boundary layer.

The present state of phytometeorology, which has long been an empirical and descriptive branch, can be characterized by an extensive and successful use of mathematical approaches. Some mathematical models of various processes in vegetation are developed which greatly contribute to the progress in phytometeorology.

Modelling procedures developed in the Main Geophysical Observatory during the last few years have enabled the construction of a complex meteorological model with the proper account for natural interaction effects of various characteristics of vegetation. The numerical experiments based on the model offer the possibility of discovering the complex influence of environmental conditions on phytometeorological parameters and vital activity of plants. Vertical distributions of some functions in and above the vegetative "canopy" are computed. They are:

(1) Phytometrica) parameters; (2) Turbulent airflow characteristics (wind velocity, turbulent energy and coefficient); (3) Vegetation thermal characteristics (air temperature and humidity, surface plant temperature, specific values of heat exchange and evapotranspiration); (4) Shortwave and thermal radiation. SB-II These characteristics were used for calculating the integral dynamic interaction and similar parameters of transpi- ration, heat and gas exchange of the plant community which are the functions of environmental factors and geometrical vegetative structure.

Extrapolation of the theory formulated for the case of horizontally non-uniform "canopy" can be useful when calculating land-improvement effects of protective forest-belts.

A complete model which takes into consideration the factors determining both the meteorological conditions and carbon dioxide concentration within a community has been developed. This model suggests a numerical estimation of the phytoproductivitv of climate and an evaluation of some potential agricultural resources of various regions. SB-II-3 INFLUENCE OF URBANIZATION AND INDUSTRIALIZATION ON LOCAL ENERGY BALANCE

J. Paszynski,

Institute of Geography, Polish A.cademy of Sciences, Warsaw, Poland

Attempts to determine the influence of urbanization and industrialization upon the atmospheric environment have shown that it is important to know the role of various anthropogenic factors in the modification of the local energy balance. To investigate this problem comparative studies of the energy balance on the earth- atmosphere interface were carried out in the Upper Silesian Industrial District and in the surrounding area. The relative changes of main components of the energy balance: incoming and reflected solar radiation; atmospheric long wave radiation; heat conduction; turbulent transfer of the sensible and latent heat, are discussed with reference to such parameters as atmospheric turbidity, heat capacity and thermal conductivity of the underlying material, roughness parameter, moisture covering factor, albedo.

Particular attention is paid to the heat reaching the earth-atmosphere interface from combustion of fuels for industrial, domestic and transportation purposes. The average annual rate of the heat flux of this origin in the central part of the Industrial District reaches even 15 percent of the incoming solar radiation. SB-1I-4 RADIATION REFLECTION THEORY FOR PLANT CANOPY

J. Ross

Institute of Physics and Astronomy, Academy of Sciences of the Estonian SSR, Tor aver e, Tartu, U. S. S. R.

A theory for the reflection of direct and diffuse solar radiation from plant canopy is proposed. The theory is based on the solution of the equation describing radiation transfer in anisotropic turbid media. Formulae for the albedo and the brightness coefficient of the system "soil - vegetation" in dependence of illumination, the optical properties of leaves and canopy architecture are derived. Main conclusions drawn from the theory are as follows: (i) Radiation reflection from plant canopy is essentially anlsotropic, even at mat leaves. The reflection is maximum in back and mirror directions and minimum in cross-plane to an incoming beam.

SOLAR ULTRA-VIOLET CLIMATOLOGY OVER AUSTRALIA

N. Sundararaman California State University, NorthrJdge, USA

D. E. St. John S. V. Venkateswaran University of California! Los Angeles, USA

and

P. J. Webster University of Washington, Seattle, USA

This paper attempts to establish the present-day ultra-violet radiation climatology over the continent of

Australia and adjacent regions. Data relating to total amount and vertical distribution of ozone from twelve stations are used.

The relevant radiative transfer problem is solved for a plane- parallel, inhomogeneous and cloudless atmosphere for arbitrary albedos of the planetary boundary. The effect of ground haze is also considered. 5B-II-6

ULTRAVIOLET RADIATION MEASUREMENTS AT POOMA

O. Chacko, C. G. Rahalkar and A. Mani

India Meteorological Department, New Delhi and Poona, India

Results of measurements of solar ultraviolet radiation from sun and sky on a horizontal surface made at Poona for about two years from 1972 to 1973 are presented. The measurements were made with an Eppley ultraviolet radiometer responding to the wavelonoth ran^e from .290 - . 390 . The radiometer consists efsentiall\ of a We^ton selenium barrier-layer photoelectric celt with a sealed-in quart;* window, a bandpass filter to restrict the wavelength response of the photocell to the desired value and a diffusing disc of opaque quart.?. The linearity and cosine response of the instrument are of the order of - 2 percent. The calibration of the radiometer is periodically checked with a tungsten-in-quartz iodine vapour lamp.

The instrument was exposed on the roof of the Central Radiation Laboratory at Poona at a height of 11 m abovo ground where a practically free exposure to the sky is avilable,. The oi tput of the radiometer was connected to a Honeywell potentiometric recorder, global solar radiation values being also recorded on it, for purpo/o* of comparison. The hourly and daily su.ns of ultraviolet radiation were computed from the records.

The diurnal and seasonal variation of ultraviolot radiation, its variation in relation to global solar radiation and its dependence on solar altitude and turbidity have been studied. An attempt ha* also been made to study the influence of ozone on the ultraviolet radiation received at the ground.

During the year as a whole about 16 cal/rm*" !et radiation, the daily values ranging between 12 - 20 cal/cm /day, with lower values occurring in winter as a result of the low solar altitudes. The proportion of ultraviolet in global solar radiation varies from 3. 9 to 4 percent, with lower values in winter, again due to the lower solar altitudes in winter.

During the day, the hourly value of ultr.iviol.i r-.i global solar radiation is a maximum at noon being 4. 5 to 4. ft percent. This ratio varies during the day, but by only about 10%, the varfation being very small during cloudy days in summer.

No marked influence of turbidity on the ultraviolet radiation has been noticed, although the turbidity coefficient increases appreciably during summer. This is due to the fact that a »urbid atmosphere causes an increase in diffuse ultraviolet radiation. However, the hourly values around noon, with higher solar elevations, show a decreasing trend with increasing turbidity.