Earth's atmosphere and cosmic rays

(the point of view of an atmospheric physicist).

Vincenzo Rizi(vincenzo.rizi@aquila.infn.it)

Dipartimento di FisicaUniversità Degli Studi - L’Aquila -ItalyRossella Caruso, Aurelio Grillo, Marco Iarlori, Sergio Petrera, Dipartimento di Fisica Università Degli Studi - L’Aquila Italy,Laboratori Nazionali del Gran Sasso, Istituto Nazionale di Fisica Nucleare

First International Workshop on Air FluorescenceSalt Lake City Utah October 5-8, 2002

Summary

• Planetary atmosphere as a calorimeter: atmospheric parameters and nitrogen

fluorescence yield. • In particular, the effect of atmosphere parameterization and/or

local meteorological measurable parameters.

• Atmospheric transmission of fluorescence light and determination of energy release by UHECR.

• Role of the aerosol transmission• Estimation of aerosol transmission (with real data).• Advantages of Raman lidar in measuring the aerosol transmission.

Relevant for inversion of Lidar Raman data, see later!

~2x107 years

~3x103 years

accumulative

~6 years

Residence times Individual speciesTurbulent mixing dominant at low altitudes (<120km)

i.e., mixing ratios ~ constant with altitude

78.084%

20.946%

0.934%

Trace gases0.036%

Atmospheric models and their use in the estimation of air fluorescence yield and light transmission.

National Space Science Data CenterNASA Goddard Space Flight CenterGreenbelt, MD 20771, USA

Models of preference for specialized tropospheric/lower stratosphere work.

Homogeneous mixing Perfect gasHydrostatic equilibrium

Partial list of available models ...

U.S. Standard Atmosphere 1976NOAA/NASA/U.S.Air Force (<32km) ICAO standard atmospheresteady state atmosphere for moderate solar activity based on rocket and satellite data + perfect gas theory

parameters listed: atmospheric temperature, pressure, density, …in 1966 supplement 5 northern latitudes for summer and winter.

Availability: the Fortran code can be obtained from Public Domain Aeronautical software.

References:U.S. Standard Atmosphere, 1976, U.S. Government Printing Office, Washington, D.C., 1976.

Atmospheric Handbook 1984NOAA/National Geophysical Data Center (NGDC)compilation by V.E. Derr

parameters listed: atmospheric parameters for scattering … calculations

Availability: from NGDC via anonymous ftp.

References:V. E. Derr, Atmospheric Handbook: Atmospheric Data Tables Available on Computer Tape, World Data Center A forSolar-Terrestrial Physics, Report UAG-89, Boulder, Colorado, 1984.

COSPAR (Committee on Space Research) International Reference Atmosphere: CIRA 1986compilations (Fleming et al., 1988) of ground-based and satellite measurements (Oort, 1983, Labitzke et al., 1985)

parameters listed: temperature, pressure, densities ...monthly mean values … for the latitude range 80N to 80S

Availability: from NSSDC's anonymous FTP site

References:E. L. Fleming, et al., Monthly Mean Global Climatology of Temperature, Wind, Geopotential Height and Pressure for 0-120 km, NASA, Technical Memorandum 100697, Washington, D.C., 1988.A. H. Oort, Global Atmospheric Circulation Statistics 1958-1983, NASA, Professional Paper 14, 180 pp., Washington, D.C., 1983. K. Labitzke, J. J. Barnett, and B. Edwards (eds.), Middle Atmosphere Program, MAP Handbook, Volume 16, University of Illinois, Urbana,

1985.

How these “atmospheres” compare … parameters relevant for air fluorescence yield and light transmission?

1 0 1 0 0 1 0 0 0p re ssu re (m b )

0

5

1 0

1 5

2 0

2 5

3 0

a ltitu d e (k m )

U S S ta n d a rd A tm o sp h e rela titu d e 4 5 N

w in te r

su m m e r

0 2 0 4 0v a ria b . %

Seasonal variability

For a typical GAP site

2 0 0 2 2 0 2 4 0 2 6 0 2 8 0 3 0 0tem p e ra tu re (K )

0

5

1 0

1 5

2 0

2 5

3 0

a ltitu d e (k m )

U S s tan d a rd a tm o sp h e re

w in te r

su m m er

C IR A 1 9 8 6

m o n th ly m ean p ro file s

0 4 8v a ria b . %

Seasonal variability

1 E + 1 8 1 E + 1 9

a tm o sp h e ric n u m b e r d e n s ity (c m-3

)

0

5

1 0

1 5

2 0

2 5

3 0

a ltitu d e (k m )

U S s ta n d a rd a tm o sp h e re

w in te r

su m m e r

C IR A 1 9 8 6

m o n th ly m e a n p ro file s

4 8 1 2v a ria b . %

Seasonal variability

REAL DATA: Local atmospheric parameters recorded by means of balloon borne meteorological radiosoundings.

Dipartimento di FisicaUniversità Degli Studi - L’AquilaItaly

Vaisala radiosondes measure upperair temperature, humidity and pressure, and upper air windspeed and direction, as they rise to their maximum altitude of ~30 km.

JanF eb

Mar

A prM

ayJun Ju l

A ugSep

O ctN ov

D ec0

1

2

3

4

5

6

7

8

9

1 0n u m b er o f P T U so u n d in g s

m a y 20 0 0 - sep tem b er 2 0 0 2to ta l n u m b er o f so u n d ig s 5 1

L 'A q u ila , Ita ly , 4 2 .3 5 N , 1 3 .2 2 E , s ite e lev a tion 6 8 3 m a .s .l.

L’Aquila, Italy 42.35N, 13.22E, 683m a.s.l.

1 0 1 0 0 1 0 0 0p ressu re (m b a r)

5 0 0 0

1 0 0 0 0

1 5 0 0 0

2 0 0 0 0

2 5 0 0 0

3 0 0 0 0a ltitu d e (m )

sp rin g

su m m er

a u tu m n

w in te r

0 1 0 2 0v a riab . %

Seasonal variability

sensors systematicsSame

atmosphere of a typical

GAP site?!

2 0 0 2 1 0 2 2 0 2 3 0 2 4 0 2 5 0 2 6 0 2 7 0 2 8 0 2 9 0 3 0 0

tem p era tu re (K )

5 0 0 0

1 0 0 0 0

1 5 0 0 0

2 0 0 0 0

2 5 0 0 0

3 0 0 0 0a ltitu d e (m )

sp rin g

su m m er

au tu m n

w in te r

0 4 8v a riab . %

L’Aquila, Italy 42.35N, 13.22E, 683m a.s.l.

Seasonal variability

sensors systematics

Outlines - atmospheric models

below 20km mid-latitude seasonal variability pressure up to 20%temperature 28%density 48%

Outlines - meteorological observations

below 20km 42N (L’Aquila - Italy)seasonal variability+sensors systematics pressure 2 10% temperature 4 8%

Atmospheric local parameters variabilityand air fluorescence yield

Nitrogen fluorescence

A.N. Bunner, 1964.

Keilhauer, B. et al., Auger technical note GAP-20012-022

TNTNN

2

2

1

1

11

O-th approx.!

, Fluorescence Yield (photons per meter per electron)

AIR FL(uorescence) Y(ield) approachPaolo Privitera

N, Atmospheric number densityT, Atmospheric temperature’s, ’s, constants

T

T

N

N

Kakimoto et al., A measurement of the air fluorescence yield, Nucl. Instr. And Meth. A, 372, 527-533, 1996.Nagano, M. and A.A. Watson, Observations and implications of the UHECR, Rev. Of Modern Phys. 72, 2000

Approaches …to minimize the errors fromatmospheric parameters variability

Adiabatic model, combined with local ground temperature and pressure measurements. Martin, G., and J.A.J. Matthews,GAP 1999-037, 1999

Local balloon borne meteorological radiosoundings.Forschungszentrum Karlsruhe - Institut für KernphysikKeilhauer, B., et al., GAP 2002-022, 2002

and/or

Atmospheric transmission of fluorescence light.

3 0 0 4 0 0w av e len g th (n m )

tim e

s

AFD

CR

sIAFD(s)

Io(s)

z

CR cosmic rayAFD Auger Fluorescence DetectorT’s transmission functionss range; z altitude

T’s

AFD light measurements

AFD light measurementsIn a single pixel:

efficiency quantum PMT)(

efficiency ion transmissoptical AFD )(

AFDat intensity cefluorescen Spectral )(

bandwidth spectrum cefluorescenAir

pixel single AFDby measuredintensity )(

sight of line thealong range

)()()()(

QE

sI

sI

s

dQEsIsI

AFD

AFD

AFDby subtended angle solid

)scattering multiple (i.e., scorrectionorder high

ion transmissabsorption gas )(

ion transmissscattering aerosol )(

@ ion transmissscatteringmolecular )(

)sight of line AFD of angle elevation theis ,s(z

z altitude @intensity spectral cefluorescenair )(

41)()()()()(

d

f

sT

sT

sT

sin

sI

dfsTsTsTsIsI

abs

aer

mol

o

absaermolo

+air fluorescence yield Energy of CR

)()()()( sTsTsTsT absaermoltotal

s range along the line of sight

It can be easily estimated with sufficient precision …!?

The absorption can be neglected because of the FD optical transmission …!?

Total atmospheric transmission

...

T

T

E

E

shower

E: shower energyT: atmospheric transmission

High variability …direct measurements with Raman lidar ORstrong assumption ...

section cross gas absorbing th-i )(

h wavelengt @ , refraction ofindex , radius of

particle aerosol an of efficiency extinction Mie),,(

@ section cross total Rayleigh

densitynumber gas absorbing th-i

ondistributi size aerosol

density number molecular catmospheri

)()(σexp)(

),(),,(exp)(

)(exp)(

0

i

0 0

2

0

i

ext

mol

i

aer

mol

i

s iabsabsabs

s

aerextaer

s

molmolmol

abs

abs

mr

mrQ

n

n

n

dssnsT

dsrsnmrQrdrsT

dssnsT

Single scattering approx.!

Laser Telescope DAQ

backscattering (bcks.)

Laser wavelength

Anelastic bcks.Raman (N2, O2 ...)

Elastic bcks. molecular/Rayleigh & aerosol/Mie

LIDARThe lidar should/could measure the needed quantities.

Laser photons Back-scattered photons

Atmosphere

4)()()(

dzTringbackscattezTNzN downupo

oo

collected photons laser photonsAtmospheric attenuation:scattering and absorption

Scattering processes:Rayleigh-Mie scatteringRaman scattering Resonant scattering

solid angle subtendedby the receiver 1/z2

z is the altitude/range

Advantages of Raman lidar vs. Elastic lidar.

Elastic/Rayleigh Lidar signal

telescopeby the subtended angle solid

particle aerosol an of efficiency ringbackscatte Mie),,(

8

310

)(

55045.5)(

:section cross ringbackscatte aldifferenti Rayleigh)(

laser by the emitted photons of #

)()()(

4),(),,()()(

)()()()(

1228

4

0

2mol

o

d

mrQ

srcmnm

L

sTsTsT

drsnmrQrdrsn

sTsTsTLsL

obck

molo

mol

mol

o

absaermol

aerobckmol

absaermolo

oo

o

o

ooo

ooooo

upward travel

backscatteringdownward travel

Key features of Klett method.

ms

otot

tottoto

sCs

dsssT

sTd

ssTLsL

oo

oo

ooooo

)()(

)(exp)(

)(4

)()()(

Recasting thelidar equation

Solving for )(sT otot

ds

dsm

sLsL

ms

m

sLsL

sTs

s

s

n

n

n

tot n oo

o

oo

o

0 '

)()'(exp

2

)(

1

)()(exp

)(ln

Mandatory assumption!

Unknown!

Key features of Fernald method.

)()(

)(exp)(

)()(4

)()()()()(

ssLR

dsssT

sTsTd

sssTsTLsL

oo

oo

oooooooo

aeraer

s

o aeraer

aermolmolaeraermolo

),(),,()(0

2 rsnmrQrdrs aerobckaero

),(),,()(0

2 rsnmrQrdrs aeroextaero

)()()( sns molmolmoloo

Mandatory assumption!

Unknown!

The Lidar Ratio (LR) is the inverse of the back scattering phase function.

Solving for )(sT oaer

ds

dsdssLRsLsLRss

sLs

dssLRsLs

LR

sT

s

s

s

s

s

molnaernmol

nn

s

s

mol

aer

n n

oo

oo

o

n

oo

o

0''

22

2

''')'(3

82exp)''(''2

)()(

)(

')'(3

82exp)(

)(ln

See …: Scannin lidar based atmospheric monitoring for fluorescent detectors of cosmic showers, D. Veberič, A. Filipčič, M. Horvat, D. Zavrtanik, M. Zavrtanik, submitted, 2002.

Anelastic/Raman Lidar signal

)337.1nm @ sr106.4 :O ;sr105.3 :(N

species th-i the

of section cross ringbackscatte aldifferenti Raman)(

)1556 :O ;2331 :(N

species th-i theofshift Raman theis

)()()(

4)()(

)()()()(

1-2302

1-2302

12

12

Ramani

cmcm

cmcm

sTsTsT

dsn

sTsTsTLsL

i

iii

ooooioi

Raman

i

absaermol

i

absaermolo

upward travel

downward travel

backscattering

2

2

log

))(log(

))(log(log

N

o

aer

aer

zT

zT

kiN

o

42

2

2

2

2

1

Raman

)(

4)()(

)(log

1

1

)(log

Noo

No

N

o

sTd

snL

sL

sT

mol

No

kNo

aer

Key features of Raman method.

Assumption!

Unnecessary if Raman signals from O2 and N2

are measured!

Unknown!

Estimation of aerosol transmission with real data.

UV Raman Vertical lidar - Dipartimento di Fisica - Università Degli Studi - L’Aquilao=351nm; Raman=382nm (N2); September 2001 L’Aquila 42oN (rural site) 1/2 hour measurements

0 1 2 3 4 5 6 7 8 9 1 0a ltitu d e (k m )

0 .1

1

1 E + 1

1 E + 2

1 E + 3

1 E + 4

1 E + 5

1 E + 6

Phot

onco

unts

(a.

u.)

E la s tic

R am an

0 4E-6 8E-6

bcks coeff. (m-1sr-1 )

1.0

1.5

2.0

2.5

3.0

alti

tud

e (

km

)

0 4E-4 8E-4

ext. coeff. (m-1)

1.0

1.5

2.0

2.5

3.0

0 25 50 75 100lr (sr)

1.0

1.5

2.0

2.5

3.0

1st step from Raman N2; k=-1

2nd step from Elastic

Taer(z)

(ext. Coeff.)(bcks coeff.)

1 .0 1 .5 2 .0 2 .5 3 .0a ltitu d e (k m )

0 .7 0

0 .7 5

0 .8 0

0 .8 5

0 .9 0

0 .9 5

1 .0 0ae

roso

l tra

nsm

issi

on

Elastic

Raman

The aerosol transmission function retrieved from real lidar signals (at Univ. AQ)The continuous lines refer to the case in which only the elastic signal is used (the lidar ratio is assumed), the dashed lines with symbols show the transmission calculated using the Raman signal.

• best configuration Scanning Raman/Rayleigh-Mie lidar

• elastic lidar More infos on backscattering than extinction. For simple non-scanning lidar systemthe aerosol extinction profiles (i.e., transmission function)derived by inverting the elastic signal, and assuming the lidar ratio, might have large systematic errors.

• anelastic lidar reliable aerosol transmission with no assumptions. A combined Raman/Rayleigh-Mie lidar measures aerosol extinction and backscattering independently.

Outlines

Aerosol variability

data from RAMAN LIDAR L’Aquila - Italy (~42oN)

clear skyabove 1500m (virtual Auger FD site)

Lidar ratio (LR) seasonal & altitude variation.

2 0 4 0 6 0 8 0 1 0 0lid a r ra tio (s r )

1 5 0 0

1 7 5 0

2 0 0 0

2 2 5 0

2 5 0 0

2 7 5 0

3 0 0 0

altit

ude

(m)

L 'A q u ila , I ta ly c lea r sk y c o n d itio n s

au tu m n /w in te r

sp rin g /su m m er

(6 2 + /- 5 )sr(59 + /- 5 )sr

(49 + /- 4 )sr

0 .0 E + 0 1 .0 E -4 2 .0 E -4 3 .0 E -4

a e ro so l ex tin c tio n (m-1

)

1 5 0 0

1 7 5 0

2 0 0 0

2 2 5 0

2 5 0 0

2 7 5 0

3 0 0 0

altit

ude

(m)

L 'A q u ila , I ta ly c lea r sk y co n d itio n s

a u tu m n /w in te r

sp rin g /su m m e r

Aerosol extinction seasonal variation.

0 2 0 4 0 6 0a e ro so l a tte n u a tio n le n g th (k m )

1 5 0 0

1 7 5 0

2 0 0 0

2 2 5 0

2 5 0 0

2 7 5 0

3 0 0 0

altit

ude

(m)

L 'A q u ila , I ta ly c le a r sk y c o n d itio n s

a u tu m n /w in te r

sp rin g /su m m e r

Aerosol attenuation length seasonal variation.

0 .7 5 0 .8 0 0 .8 5 0 .9 0 0 .9 5 1 .0 0

a e ro so l re la tiv e tra n sm iss io n

1 5 0 0

1 7 5 0

2 0 0 0

2 2 5 0

2 5 0 0

2 7 5 0

3 0 0 0

altit

ude

(m)

L 'A q u ila , I ta ly c le a r sk y c o n d itio n s

a u tu m n /w in te r

sp rin g /su m m e r

Aerosol transmission seasonal variation.

Aerosol transmission seasonal variation.

0 .7 5 0 .8 0 0 .8 5 0 .9 0 0 .9 5 1 .0 0ae ro so l re la tiv e tra n sm iss io n

1 5 0 0

1 6 0 0

1 7 0 0

1 8 0 0

1 9 0 0

2 0 0 0

2 1 0 0

2 2 0 0

2 3 0 0

2 4 0 0

2 5 0 0

2 6 0 0

2 7 0 0

2 8 0 0

2 9 0 0

3 0 0 0al

titud

e (m

)w in te r

sp rin g

su m m e r

a u tu m n

L 'A q u ila , Ita ly m o n th ly m ean p ro filesc lea r sk y co n d ition s

0 1 E -4 2 E -4 3 E -4 4 E -4 5 E -4

a e ro so l e x tin c tio n @ 3 5 1 n m (m -1 )

1 .5

2 .0

2 .5

3 .0

altit

ude

(km

)

0 .8 0 .8 4 0 .8 8 0 .9 2 0 .9 6 1 1a e ro so l tra n sm iss io n @ 3 5 1 n m

1 .5

2 .0

2 .5

3 .0

S ta rt T im e

1 8 :2 0

1 8 :5 0

1 9 :2 0

1 9 :5 0

2 0 :2 0

2 0 :5 0

L 'A q u ila , I ta ly , a e ro so l-w a te r R am an lid a r F eb ru a ry 4 , 2 0 0 2 - s ix p ro file s fro m 1 8 :2 0 to 2 1 :2 0 L T

Aerosol extinction and transmission “day” variation.

Outlines - aerosol contribution to light transmission

Most of the aerosol in the planetary boundary layer (<3km a.s.l.) clear skyfrom ~ 1500m a.s.l.relative transmission mean value ~0.85seasonal variability up to 15% (3)“day” variability (over 3hours - night) ~6%

Status of Raman channel integration in Auger lidar.

o p tica l fib er

P M T # 1E la stic

P M T # 2R a m a n O 2

P M T # 3R a m a nN 2

N O s

N D sIF # 1

N D sIF # 2 IF # 3

N D s

B S # 1 B S # 2 B S # 3

L

Technical details of Raman lidar

L: field lensBS: beam splitterNO: notch filterND: neutral density filterIF: interference filterPMT: photomultiplier

ElasticRaman O2

Raman N2

telescope

laser

INFN Torino/Nova Gorica Polytechnic LIDAR

Pino TO

0 .9 0 .9 2 0 .9 4 0 .9 6 0 .9 8 1

a e ro so l re la tiv e tra n sm iss io n

1

2

3

4

5

6

altit

ude

a.s.

l. (k

m)

0 1 E -7 2 E -7 3 E -7 4 E -7 5 E -7 6 E -7

a e ro so l b a c k sca tte rin g @ 3 5 5 n m (m -1 sr-1 )

1

2

3

4

5

6

altit

ude

a.s.

l. (k

m)

MALARGUE height a.s.l.

Lower limit estimation!.

VERY PRELIMINARY!

Lidar Auger Malargue - Argentina

Malargue Lidar - zenit angle= 90°March 7, 2002 - LR=50, raw resolution 30m