WCP 86, A preliminary cloudless standard atmosphere for radiation computation

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WORLD CLIMATE RESEARCH PROGRAMME

INTERNATIONAL ASSOCIATION FOR METEOROLOGY

AND ATMOSPHERIC PHYSICS

RADIATION COMMISSION

A PRELIMINARY CLOUDLESS STANDARD ATMOSPHERE

FOR RADIATION COMPUTATION

MARCH 1986

WCP - 112

WMO/TD-NO. 24

INTERNATIONAL COUNCIL OP WORLD METEOROLOGICAL

SCIENTIFIC UNIONS ORGANIZATION

INTERNATIONAL ASSOCIATION FOR METEOROLOGY AND

ATMOSPHERIC PHYSICS

RADIATION COMMISSION

A PRELIMINARY CLOUDLESS STANDARD ATMOSPHERE

FOR RADIATION COMPUTATION

Boulder, Colorado, U.S.A.

1984

This report was initiated by the ad hoc Working Group on

a Standard Radiation Atmosphere of the International Radiation

Commission,

R. A, McClatchey, Chairman

H.-J. Bolle

K. Ya. Kondratyev.

It was finalized in cooperation with the WMO-ICSU Joint

Scientific Committee Experts Group on Aerosol and Climate,

H.-J. Bolle, Chairman

J. H.. Joseph

M. P. McCormick

Raschke

J. B. Pollack

D. SpankuCh

and the International Ozone Commission,

C. Mateer, President.

The optical aerosol models are based upon the work of

Shettle and R. Fenn

who contributed a substantial part of this report.

The global model and the comments of

О. B. Toon and J. P. Pollack

were used as a guideline for the construction of aerosol

vertical profiles.

A number of individual scientists have been contacted in the

course of the preparation of this document. Essential suggest-

ions and modifications proposed by

J. Lenoble

and

G. Hanel

have been implemented in the present version.

H. Gerber

carefully edited the aerosol part of the final draft.

TABLE OF CONTENTS

Page No.

FOREWORD 1

INTRODUCTION 2

ATMOSPHERIC TEMPERATURE AND HUMIDITY STRUCTURE 3

AEROSOL MODELS 6

General : 6

2.2 Basic Aerosol Types 7

2.3 Aerosol Size Distribution 9

2.4 Optical Model Parameters 12

2.5 Atmosphere Aerosol Profiles 24

2.6 Application of the Aerosol Models .... 27

VERTICAL DISTRIBUTION OF RADIATIVELY ACTIVE

TRACE GASES 29

. 1

General 29

. 2

Ozone 29

. 3

Carbon Dioxide 33

3.4 Methane

3 5

. 5

Nitrous Oxide

3 5

. 6

Carbon Monoxide 36

. 7

Nitric Acid 36

8 Halocarbons 37

3.9 Nitrogen Dioxide (N0

) 38

3.10 Nitric Oxide (NO) 39

3.11 Other Trace Gases 40

INTERPOLATION TECHNIQUE 42

OUTLOOK

4 4

REFERENCES 45

- 1 -

FOREWORD

For radiation computations there is a twofold demand

for standardized models:

First

to test and to intercompare radiation transfer

algorithms

and

Second, to compute the radiation terms for sensitivity

studies in climate research.

For the first purpose, the intercomparison of radiation

computation schemes, a small number of mean and extreme

atmospheric models, which need not even reflect realistic con-

ditions,

would be sufficient.

For the second purpose models are desired which get

as close as possible to natural states of the atmosphere.

The present report is an effort to provide the radiation

community with cloudfree standard atmospheres for the first

purpose,

which are also realistic in so far as they reflect

certain selected mean conditions. Thus the models presented

here may be used in first approximation sensitivity studies.

It is expected that these models will form the basis of more

sophisticated models intended especially to implement cloudi-

ness,

and to make them more useful for climate sensitivity

studies in the sense as requested by the JSC

(JSC-1,

1980).

With respect to these future extensions some ideas are

out-

lined in this report which may stimulate the discussion among

concerned scientific groups. Any feed-back with respect to

future requirements and specifications would be welcomed by

the Radiation Commission.

We would like to thank all colleagues who cooperated

in the preparation of this document for their efforts and

suggestions.

Not all proposals received could yet be imple-

mented since the objective for this report was to present a

nucleus of minimum size with a potential for future augmentation

and modification.

Innsbruck, September 1984 H.-J. Bolle

President

International Association for

Meteorology and Atmospheric Physics

'?, -

INTRODUCTION

The starting point for this report was the U.S. Stan-

dard Atmosphere (1976) and the U.S. Standard Atmosphere

Supplements

(1966).

Much of this material had been published

in the Handbook of Geophysics and Space Environments (Valley,

1965).

Distributions of water vapor and ozone had been added

to these basic atmospheric models in order to construct the

models described by McClatchey et al

(1972,

1978) which are

also published by Wolfe and Zissis (1978) and Driscol and

Vaughan

(1978).

For the purposes here, only three of the origi-

nal six models have been adopted, representing one climato-

logical mean and two extremes. Other significant absorbing

gases had originally been assumed uniformly mixed at values

identified by McClatchey et al.

(1972,

1978),

but the work of

Cadle

(1973),

provided a review leadihg to mixing ratios

which vary with altitude. More recent work has led to a re-

finement of these values and the results will be summarized

below.

The aerosol models used here are based primarily on

the work of Shettle and Fenn

(1975).

They described a large

number of aerosol models covering a wide variety of conditions

from sea level to the mesosphere. These models were developed

from many sources and the reader is referred to the Shettle

and Fenn reference for a complete list. There exist different

approaches to deal with the aerosols in radiation computations

(Toon and Pollack, 1976; Ivlev, 1967; Hanel and Bullrich, 1978;

Kondratyev and Pozdnyakov, 1981; Kondratyev, Moskalenko and

Pozdnyakov,

1983).

The ultimate choice of an aerosol m6del may

also depend on the algorithm used for radiation computations:

one or the other aerosoi model may be implemented more easily

in existing radiative transfer calculation- schemes. This

problem needs further attention and is not regarded as being

finalized at this time, though one procedure was selected for

comparative studies.

Radiative transfer in molecular absorption bands may

be treated by direct line-by-line computations or by applying

averaged transmission functions such as used in the AFGL LOWTRAN

scheme (McClatchey et al., 1973; Kneizys et al., 1980; Chedin

and Scott,

1980b).

It is recommended that a current version of

the AFGL line-by-line compilation described by McClatchey et

al.

(1973),

Rothman et al. (1983a, b) or by Chedin (1980 a)

which are periodically updated should form the basis for all

parameterizations and ultimate accuracy of the presently

available data and computation procedures (International

Radiation Commission ad hoc Working Group on Remote Sensing

Spectroscopy).

- 3 -

1. ATMOSPHERIC TEMPERATURE AND HUMIDITY STRUCTURE

Tables 1.1 - 1.3 represent three climatological atmo-

spheric models selected and proposed for comparative calcula-

tions in terms of height, pressure, temperature, density,

and water vapor density. The three models are the U.S. Standard

Atmosphere, 1976, a tropical and a subarctic winter atmosphere

taken from the U.S. Standard Atmosphere Supplement, 1966.

Water vapor is in each case given for a dry and a moist strato-

sphere.

The tropospheric water vapor profiles have been

derived from material contained in Valley

(1965).

The dry

stratosphere water vapor model is taken from the review

article by Penndorf (1978) to be constant at the level of

3.2 ppmv. The moist stratospheric water vapor model is taken

from Sissenwine et al.

(1968).

It is recommended that the

dry atmosphere be used as first choice.

Table 1.1: U.S. Standard Atmosphere, 1976

Water vapor

height pressure temp. density moist stratos. dry stratos.

(km) (mb) (K)

(g m )

1.013E+03

288

1.225E+03

5.9ЕЮ0

•>.9E+00

8.96tE+02

282 1.112E+03 %.2E«-00 «♦•2E+00

2 7.950E+02 275

1#007E*Q3

2*9E*00

2.9E+00

3 7.012E+02

269

9.093E+02 1#8E*00

1.8E+00

6.166E+02

262 8.194E+02 1.1E+00 1«1E*00

5.*05E+02

256

7#36*E*0 2

6.*E-01

b.*E-01

*.722E*02

2*9 6.601E+02 3.8E-01 3.8E-01

**111E*02 2*3

5*900E*02 2.1E-01 2ЛЕ-01

6 3.565E+02 236

5.258E+0 2

1.2E-01

3.080E+02

230

*.671E*02 *.6E-02 «♦•6E-02

2.650E+02

223

*.133E*0 2

1.6E-02

l.SE-02

Z.Z7QE+UZ 217

3«6*8E+0 2

8.2E-03

i*9*0E*02

217

3.119E+02

3.7E-0 3

3.7E-03

1.658E+02

217

2.666E+0 2

1.8E-03 1.8E-03

l.*17E+02

217

2*279E*02

8.*E-0*

•ПЦЕ-0*

1.211E+02

217

i.9*8E*0

7.2E-0*

f.2E-0*

1.035E+02

217

1.665E+0 2 5.5E-0* 5.3E-0*

8.850E+01

217

l.*23E*02

Ч.7Е-0*

Z.8E-0*

7.565E+01

217

1.217E+02

*.0E-0*

2.<*E-0*

6«*67E+01

217

1.СЛ0Е+02

*.1Е-0*

2.1E-0*

20 5.529E+01

217

8.891E+01

*.0E-0*

1.8E-0*

*.729E*01

218

7.572E+01

*.*E-0*

1.5E-0*

*.0*8E*0i

219

6,<*50E

**6E-0*

1.3E-0*

3**67E*0i

220

5.501E+G1 5.2E-0* 1.1E-0*

2.972E+01

221

*«69*Е*01 5.*E-0*

9Ф*Е-05

2*5*9E*01

222

«♦.008E

*.1Е-0*

8.0E-05

1.197E+01

227

1.8*1E*01 3.2E-0*

1.7E-05

5,7%6E*00 237 8**бЗЕ+00 1.3E-0*

1.7E-05

4 b

2.871E+00

253

3.996E+00 «♦.8E-05 7.9E-06

l.*91E*00

26*

1.966ЕЮ0 2.2E-05

1.9E-06

7.978E-01

271

1.027E+00 7.8E-06 2.1E-06

5.220E-02

220

8. 283E-0 2

1.2E-07 1.5E-07

too

3.008E-0*

21C

«♦.990E-0*

Ч.0Е-10

1.0E-09

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Table 1.3: Subarctic Winter Atmosphere

water vapor

height pressure terap. density moist stratos. dry stratos.

(km) (mb) (K) (g пГ

) (g пГ

)

1.013Е+03

257

1.373Е*03

1.2Е+00

1.2Е*00

1 8.878Е+02 259

1.194Е+0

1.2Е+00 1.2Е+00

2 7.775Е*02

256

1.058Е*03

9.*»Е-01

9.«»Е-01

3 6.798Е+02 253 9.372Е+02 6.8Е-01

6.ЭЕ-01

5.932Е*02

2%в

в.З*ЗЕ*02

«».

1Е-01 Ч.1Е-01

5 5.158Е*02

гы

7.*»59Е*02

2.0Е-01

?.0Е-01

6 <».Ъ67Е*02

23 «♦

6.6<f8E+0 2

9.8Е-02

7 3.853Е+02 227 5.906Е+02

5.«»Е-02

5,iiE-02

В 3.308Е+02 221 5.22<»E*0 2

1.1Е-02 1.1Е-02

г.вгэЕ+ог

217 *t.538E+0 2

в.*»Е-03

Ч.^Е-03

г.швЕ+ог

217 -3.878Е+02

5.5Е-03

1.1

2.Q67E+02 217

3.315ЕЮ2

З.вЕ-03

S.8E-03

1.766Е+02

217

г.еззЕ+сг

2.6Е-03

1.510Е+02

217 2.<f22E*0 2

1.8Е-03

\ч

1.291Е+02

217

2.071Е+0 2

1.0Е-03

1.103Е+02

217

1.769Е+0

7.6E-0I»

Г.6Е-0*»

16 9.Ч31Е*01 217

1.517Е+0

•>.ОЕ-0<» З.ОЕ-О*»

17 8.058Е+01 216

1.300Е+02

«».ЗЕ-0«»

2.6Е-0*»

16 6.862Е+01 215

1.113Е+02

3.7Е-0*»

2.2Е-0*»

19 5.875Е*01 215 9.529ЕЮ1

3.7Е-0«»

1.9E-0*t

го

5.01«»Е+01 21 «» 8.159Е+01

3.7Е-0*»

1.SE-0*

21 <».277Е*01 21<»

6.976Е+01

«♦.1Е-0*»

1.*»Е-0<«

гг

3.6«»7Е*01 213

5.965Е+01

*».3E-0*f

1.2Е-0«»

гз

3.109Е+01

212

5.099Е*01

'♦.вЕ-О'»

1.0Е-0<*

гч

2.6<»9Е+01 212 «».357Е+01

5.1Е-0<»

8.7Е-05

25 2.256Е+01 211

3.721Е+01

5.6Е-0*

7.«»Е-05

1.020Е+01

216

1.6«*5Е*01

2.9Е-0»»

J.3E-05

35 «».701Е*00 222

7.371Е+00

1.1Е-0*

1.5Е-05

«♦0

2.2<»ЗЕ+00 235

3.329Е+00

*.1Е-05

6.7Е-06

1.113Е+00

2*7 1.570E+Q0

1.7Е-05

3.1Е-06

50 5.719Е-01 259 7.68VE-01

5.8Е-06

1.5Е-06

70 *».016Е-02

гиъ

5.69«»Е-0 2

8.0Е-08

1.1Е-07

100 3.000Е-04 210 «♦.977Е-0*»

3.0Е-10

1.0Е-09

- 6 -

AEROSOL MODELS

2.1 General

In general it is necessary to know (or to measure)

three different quantities in order to adequately describe

the aerosol extinction in the atmosphere: The complex index

of refraction of the particles, the particle size distri-

bution and particle shapes. A knowledge of the first two

quantities is sufficient if it can be assumed that the particles

are spherical and Mie theory is applicable. Here the work of

Shettle and Fenn (1975, 1979) was primarily followed in de-

fining complex indices of refraction and particle size

dis-

tributions of the several aerosol components. Some modifi-

cation of the Shettle and Fenn model has been introduced

here mainly in the boundary layer based on suggestions made

by Joseph et al. (1980) and Joint Scientific Committee

(1981).

These modifications include the following:

(1) Slight changes in the percentages of the various

aerosol components in the Continental, Urban-

Industrial,

and Maritime models;

(2) The introduction of a small (by mass) soot compo-

nent in the Continental model;

(3) The introduction of a different fine particle

size distribution representing the soot-like

component in the Urban-Industrial model; and most

importantly

(4) Application of the idea of "external mixing" in

the model construction. "External mixing"

implies that each component of a given aerosol

model is represented by a different substance

with its own single mode size distribution and

single complex index of refraction. Following

separate Mie calculations on these components,

resultant extinction coefficients (scattering

coefficients and absorption coefficients) are ob-

tained as appropriate weighted averages using the

volume percentages.

(5) The aerosol vertical profiles were modified using

the Toon and Pollack (1976) profiles for guidance.