m itoring 

atic Change 

No. 11 

SUII arv Reporl1982 

U.S. DEPARTMEIT 

OF COMMERCE 

IATIDIAL 

OCEAIIC AID 

ATMOSPHERIC 

ADMIIISTRATIOI 

EIVIROIMEITAL 

RESEARCH 

LABORATORIES 
Geophysical Monitoring 

for Climatic Change 

No. 11 

Summary Report 1982 

Joyce M. Harris and Barry A. Bodhaine, Editors 

Air Resources Laboratory 

Geophysical Monitoring for Climatic Change 

Boulder, Colorado 

December 1983 

u.s. DEPARTMENT OF COMMERCE 

Malcolm Baldrige, Secretary 

National Oceanic and Atmospheric Administration 

John V. Byrne, Administrator 

Environmental Research Laboratori es 

Vernon E. Derr, Director 
NOTICE 

~Iention of a commercial company or product does not constitute 

an endorsement by NOAA Environmental Research Laboratories. 

Use for publicity or advertising purposes of information from 

this publication concerning proprietary products or the tests 

of such products is not authorized. 

ii 
CONTENTS 

FOREWORD . 

PREFACE . 

ACRONYl'IS. 

EL CHI CHON SUNRISE AT ~~UNA LOA 

1. 

2. 

3 . 

4. 

SUMMARY ... ... . 

OBSERVATORY REPORTS 

2 .1 

2.2 

2.3 

2.4 

Mauna Loa. 

Bar row . . 

Samoa. . . 

South Pole 

CONTINUING GMCC PROGRAMS 

3. 1 

3 . 2 

3.3 

3 . 4 

3 . 5 

3 . 6 

3.7 

3.8 

3.9 

3 .10 

3 . 11 

3.12 

3 .1 3 

Carbon Dioxide 

Total Ozone. . 

Ozone Ve rti cal Distribution . 

Surface Ozone .. ... .. . 

Stratospheric Water Va por .. 

Halo ca rbons and Nitrous Oxide. 

Stratosphe ric Aerosols--Lidar . 

Surface Aerosols 

Solar Radiation ... .. 

Station Climatology. . . 

Precipitation Chemistry . 

Da ta Management. . . . . 

Atmospheri c Trajectories 

SPECIAL PROJECTS . . . . . . . 

4.1 

4.2 

4 . 3 

4.4 

4.5 

4.6 

4.7 

4.8 

4 . 9 

4 . 10 

4.11 

4.12 

4 . 13 

4 . 14 

CO 2 Modeling . . . . . . 

A Preliminary Examination of CO 2 Data in the High 

Latitudes of the Southern Hemisphere . . 

Dobson Spectropho t ometer Automa t ion and Establishment 

of the Global Umk ehr Observation Network 

Studies of Winter CO 2 Va riabi lity at BRW 

Me asuremen ts of Skylight Polarization a t MLO 

Arctic Ha ze and AGASP . .... ... . 

Light Scattering, Co nd ensation Nuclei, and Air Mass 

Trajectories at Whiteface Mount ain . . . . . . 

Lidar Observations of El Chichon Stratospheric Dust. 

Umkehr Ozone Profile Error Caused by El Chichon 

Stratos pheric Dust . . . . . . . . . . . . . . . . 

MLO Trajectory Ens embles, April and May 1979-1982. 

The Photovoltaic Power System at SMO ...... . 

Atmospheric CO 2 Measurements Aboard R/V DISCOVERER, 

Ma y-June 1982 .. . .... . . . .... . . . . . . 

Airborne Opti ca l Meas ur eme nts of the El Chichon Clo ud . 

MLO Normal Incidence Irradiance Record . . . . . . . . 

iii 

Page 

v 

vii 

viii 

x 

1 

5 

5 

11 

14 

16 

24 

24 

33 

37 

39 

40 

43 

46 

46 

52 

56 

62 

65 

67 

76 

76 

78 

80 

81 

84 

86 

89 

92 

94 

95 

97 

99 

102 

104 
5. 

6. 

7 . 

8. 

9. 

COOPERATIVE PROGRAl'IS . . . . 

5.1 

5.2 

5.3 

5.4 

5.5 

5.6 

5.7 

5 . 8 

5 . 9 

5.10 

5 . 11 

5 . 12 

5.13 

Measurements, Sources, and Sinks of Atmospheric 

Benzene and Toluene. . 

(R. A. Rasmussen and 

Aerosol Light Absorption 

(A. D. Clarke and R. 

M. A. K. Khalil) 

at LO. . . . 

J. Charlson) 

Solar Radiation Assessment for BRW . 

(G. Wendler) 

Climatology of Aerosol Concentration at SPO 

February 1974-December 1982 . . .. 

(J. A. Samson and A. W. Hogan) 

Size Characteristics of Asian Dust Sampled at 

(T. A. Cahill and D. A. Braaten) 

CO 2 and Other Air Chemistry Studies at Palmer 

(E. Robinson and W. L. Bamesberger) 

Raman Study of Graphitic Carbon Concentrations 

Western Arctic . . .. .. . . . .. .... . 

(H. Rosen and T. Novakov) 

Ultraviolet Erythema Global Measuring Network. 

(D. Berger) 

~ILO. 

Station. 

in the 

Aerosol Concentration Periodicity and Optimum Sampling 

Stralegy at ~ILO ........ . ....... . 

(M. Darzi and J. W. Winchester) 

Chemical Analyses of Atmospheric Particulates at MLO 

and SPO. . . . . .. . .. ..... .... . 

(J. R. Parrington, G. Tuncel, C. M. Thompson, and 

I,. H. Zoller) 

Electric Fields and Currents in the Vicinity of 

a Mountain . . . . . . . . . . . . 

(r. Tzur and R. G. Roble) 

Atmospheric Bromine in the Arctic. 

(W. W. Berg, P. D. Sperry, K. A. Rahn, and 

E. S. Gladney) 

Spectrum and Cross-Spectrum Analysis of Daily 

Meteorological and Chemical Data at BRW. 

(W. E. Raatz) 

5.14 Changes in the Seaso nal Amp l itude of CO 2 at MLO. 

(L. P. S tee le) 

INTERNATIONAL ACTIVITIES 

PUBLICATIONS AND PRESENTATIONS BY G~ICC STAFF, 1982 

REFERENCES . 

GtICC STAFF, 1982 

iv 

Page 

107 

107 

111 

114 

114 

117 

120 

121 

124 

124 

127 

134 

136 

140 

143 

144 

146 

149 

159 
FORE\,ORD 

When I was invited to prepare this foreword to Number 11 of the Geophysical tlonitoring for Climatic Change Summary Report series, the first and ob -

vious thought was of the opportunity for a retrospective, comparative analysis 

of this vi t a l prog ram as it moved from a single site to multiple sites ; survived the t eething pang s of difficult logistics (and bureaucratic impedimenta), 

staffing, and instrumenta tion development; and is now i nvolved i n data ana l ysis and interpretation, a massive (and almost real-time) archiving effort , and 

impressive activities in data precision and quality control. However, I think 

that this program, opening its seco nd decade, i s better vi ewed as th e maturin g 

of the co ncept of chemical clima t ology of the atmo s phere and its ro l e i n t he 

conventi onal idea of c limate in terms of temperature and precipitation . The 

next 10 years will be a decade of challenges to determine the i nventories and 

biogeochemical cyc ling of a host of trace gases ; the rol e of particulate mat erials in the transformation chemistry of gases ; and the quantitative influences of s ubmi cron particles on cloud formation/persiste nce, precipitation, 

a nd solar and IR ra diation fluxes. 

The uni que CO 2 time series at Mauna Loa Observatory, now covering 

25 years , stimulated the inclusion of changing gas concentrations i n global 

climate mode l s . Now we find, apparently, that tropospheric methane is on the 

increase. Also, the chlorofluorocarbons continue t o increase as does trichl oroethane . One could add to t he list many other compounds whose concen -

trations and trends appear to be changing . Many of these compounds absorb IR 

radiation and add to the potential CO 2 "greenhouse" effect, but their conce nt ration histo ries are mu ch l ess known. As the understanding of atmospheric 

chemistry has advanced, radical comp ounds (e.g., OH, H.O.) in the atmosp here 

have ass umed a central role in t he tra nsformation and, often, the accelerated 

r emova l of man y compound s . The role of aqueous chemistry in cloud water is 

a l so being recognized . When one thinks that about one -half of the globe is 

always cloud covered , the necessity of understandi ng these processes is ob -

vious. 

This list of unknown areas is woefully incomplete, but we do see chemical 

gradients ove r local, regional, continental , and interhemispheric scales. The 

t ra nsport of aerosols over dista nces of more than 10 ,000 km and the ubiquitous 

presence of organic and s ulfur compounds in even the clea nest of rains at 

remote sites are now do cumented. The intellectual challenges to an adequate 

understanding of atmosp heric chemistry, and of sour ces and sinks for both 

na tu ral alld anthropogenic materials , are stunning. 

To date, our documentation of clean-ai r tropospheric chemistry is from 

only a handful of permanent observatories , less than 10 globally . Fortunately , research expedi ti ons using s hip s and aircraft have provided much new 

informa t ion. A maj o r new development is t he use of indirect sensing techniques t o extend the vert ical dimension of the measurements. Such sensors 

(notably for ozone) , mounted on satellite platforms, are providing almost -

synoptic data. 

Yet it is primarily from the fixed sites that we find diurnal, seasonal, 

and interannual variability of concentration . The year-to-year variability in 

the CO 2 airborn e fraction is an important case in poi nt f or whi ch there is , as 

yet , no adequate explanation. 

v 
Thus, a second series of challenges for the next decade is to coordinate 

and correlate the new techniques and platforms to obtain the most informative 

da ta series . Determining the role of fixed, grou nd-based sites in providing 

satellite ground truth is an obvious need. However, there are other issues: 

What are the optimum sampling schedul es for the many gaseous compounds that 

must be measured, and for near-surface aerosols and aerosol profiles? What 

are the chemi cal profiles of various size fractions of the aerosols at various 

locations?--The recent multiagency study of Arctic haze provided not only 

important scientific information but also a model of coordinated observations. 

Can automation and modern data processors make continuous monitoring more 

cost- effective than periodic grab sampling i s? What new instruments are required? Can accurate multicompound nitrogenous species and continuous OH 

measurement methods be developed? Are such data required? 

Answers t o these challenges and these questions (and many others not 

stated here or not yet known) will alter the GtlCC program by 1992. What will 

not change is the continuing need for precise and accurate gas and aerosol 

meas urements from which radiation a nd cloud behavior can be derived. By 1992 

it is expected that temperature effects from the increase in CO 2 concentration 

will be detectable in relatively conventional measurements. Quantitative 

separation of this influence from effects of changes in other trace gases and 

from aerosol i nfl uen ces will require the continued dedication to excellence 

that has characterized the GtlCC staff. 

A new generation of observers and scientists will e nter the program in 

the next de ca de . They too must ca rryon this trad ition and mee t the se 

challenges. 

vi 

Donald H. Pack 

Consulting Meteorologist 
PREFACE 

This document presents a s ummary of the research operations and accomplishments by the Geophysical Nonitoring for Climatic Change (G~ CC) program 

and by outside investigators working cooperatively with GNCC in 1982. It includes descriptions of management and operations at GNCC's four baseline 

sites, scientific data from the meas urement projects, conclusions from 

analyses of data, and recent basic research achievements. 

The G~ICC program, established in 1971, is one of seve ral research programs 

within t he Air Resources Laboratory under the directorship of Lester Nachta. 

Its four observatories are located at Barrow, Alaska (in service si nce 1973); 

Nauna Loa, Hawaii (in service since 19 56); American Samoa (in service since 

1973) ; and South Pole (in service since 1957) . Background mea suremen ts of 

aerosols , gases, and solar radiation that are important to the climate of the 

Earth are made at the observatories. The primary groups within GNCC are 

Nonitoring Trace Gases, Aerosols and Radiation Monitoring, Acquisition alld 

Data Management, and Analysis and Interpretation. Specific names of individuals in GNCC are not given in the main text of the report; however, the 

memb ers hip of each GMCC group is given in sec. 9. Publications and presenLation s by GNCC staff are given in sec . 7. 

vii 
A&DM 

AES 

AGASP 

ARL 

ARH 

ASCS 

ASRC 

BDL 

BUI 

BRW 

CAF 

CDC 

CIRES 

CflA 

CN 

CNC 

CPU 

CSIRO 

ACRONYHS AND ABBREVIATIONS 

Acquisition and Data Management (GMCC) 

Atmospheri c Environment Service, Ca nada 

Arctic Gas and Aerosol Sampling Program 

Air Resources Laboratory, Rockville, Md. (ERL) 

Aerosols and Radiation Monitoring (GMCC) 

Alaska Soil Conservation Service 

Atmospheric Sciences Research Center, SUNYA, Albany, N.Y. 

Below detection level 

Bureau of Land flanagement (USGS) 

Barrow Observatory, Barrow, Alaska (mICC) 

Clean Air Facil ity 

Control Data Corporation 

Cooperative Institute for Research in Environmental Sciences 

Chemical Manufacturers Association 

Condensation nuclei 

Condensation nucleus counter 

Central processing unit 

Commonwealth Scientific and Industrial Research Organization, 

Australia 

CSU Colorado State University, Ft . Collins, Colo. 

DOE Department of Energy 

DOY Day of year, Julian 

EC Elemental carbon 

ECC 

HIL 

ENSO 

EPA 

ERL 

flO 

FPD 

GC 

G. E. 

GEOSECS 

GilA 

GHOST 

GflCC 

GSA 

HASL 

HASP 

HP 

HVO 

IAEA 

ICDAS 

IGY 

IlCA IS 

IR 

!TCZ 

IT&T 

KEY 

KUfl 

LBL 

LLL 

flLO 

Electrochemical concentration cel l 

Environmental fleasurements Laboratory (DOE) 

El Ni~o - Southern Oscillation 

Environmental Protection Agency 

Envi ronmental Resea rch Laboratories, Boulder, Colo. (NOAA) 

Flame ionization detector 

Flame photometric detector 

Gas chromatograph 

General Electric 

Geochemica l Ocean Section Study 

Greenwich hour angle 

Global Horizontal Sounding Technique 

Geophysical Hon i toring for Climatic Change, Boulder, Colo. (ARL) 

General Services Administration 

Health and Safety Laboratory (EPA) 

High Altitude Sampling Program 

Hewle tt- Pa cka rd 

Hawaiian Volcano Observatory 

International Atomic Energy Agency, Vienna, Austria 

Instrumentation Control and Data Acquisition System 

International Geophysical Year 

Interactive Instrumentation Control and Honitoring System 

Infra red 

Intertropical Convergence Zone 

International Telephone and Telegraph 

Key Biscayne, Fla. 

Cape Kumukahi, Hawaii 

Lawrence Berkeley Laboratory (DOE) 

Lawrence Livermore Laboratory (DOE) 

Mauna Loa Observatory, Hawaii (GMCC) 

viii 
NSL 

~ITG 

NADP 

NARL 

NASA 

NBS 

NCAR 

NCC 

NDIR 

NIAR 

NIP 

NNC 

NOAA 

NRL 

NSF 

NWR 

N\,S 

OGC 

ONR 

OPC 

OPEC 

OWR~I 

PI SSA 

PIXE 

PNEL 

PHT 

PRON 

PV 

p3 

RDOS 

RNS 

R/V 

SC~I 

SID 

SNO 

SPO 

SUNYA 

Tg 

TO~IS 

UPS 

URI 

USCG 

USGS 

UV 

WDC-A 

\;Y~I 

\'1'10 

\VPL 

WSU 

Nean sea level 

Nonitoring Trace Gases (GNCC) 

National Atmospheric Deposition Program 

Naval Arctic Research Labora tory , Barrow, Alaska 

National Aeronautics and Space Administration 

National Bureau of Standards 

National Center for Atmospheric Research, Boulder, Colo. 

National Climatic Center, Asheville, N.C . 

Nondispersive infrared 

Norwegian Institute for Arctic Research 

Normal incidence pyrheliometer 

National Neteorological Center , Suitland, Nd. 

National Oceanic and Atmospheric Administation 

Naval Resear ch Laboratory, Washington, D.C. 

National Science Foundation, Washington, D.C. 

Niwot Ridge, Colo. 

National Weather Service 

Oregon Graduate Center, Beaverton, Oreg. 

Offi ce of Naval Research 

Optical particle co unter 

Organization of Petroleum Exporting Countries 

Office of Weather Research and Nodification, Boulder, Colo . (ERL) 

Particulate integrating sampling sector analyzer 

Particle induced X-ray emission 

Pacifi c Harine Enviroluuental Laboratory , Seattle, \'as h. (ERL) 

Photomu ltiplier tube 

Programmable read-only memory 

Photovoltaic 

Portable press urizing pack 

Real-time Dis k Operating System (Data General) 

Root mean square 

Research Vessel 

Standard cubic meters 

Scripps Institution of Oceanography, La Jolla, Calif. 

Samoa Obs ervatory, American Samoa (G~ICC) 

South Pole Observatory, Antarctica (G~ CC) 

State University of New York at Albany 

10 12 grams 

Total Ozone Napping Spectrometer 

Universal Power Supply 

University of Rhode Island, Kingston, R.I. 

United States Coast Guard 

United States Geological Survey 

Ultraviolet 

World Data Center-A, Asheville, N.C. 

Whi teface Hountain Observa tory, N. Y. (ASRC ) 

World teorologi cal Organization, Geneva, Switzerland 

\,ave Propagation Laboratory, Boulder, Co l o . (ERL) 

Washington State Unive rsity, Pullman, Wash. 

ix 
EL CHICHON SUNRISE AT MAUNA LOA 

Photographs of the horizon taken by K. Co ulson from Hauna Loa Obs e rvato ry 

during the presunrise period on 14 Hay 1982, s howing the dramatic color induced by the EI Chichon volcanic cloud. On this day the cl oud over MLO was at 

its most strongly developed phase, as s hown by lidar meas ur ements . The top of 

the cloud was at abo ut 30-km a ltitude MSL. Local times and so l ar depression 

angl es , respectively, for these pictures were 0500, -1 0.0° (upper left); 

x 
0512, -7.5° (lower left); 0522, -5.3° (upper right); and 0540, -1.6° (lower 

right). Local sunrise time was 0548. In the first picture of this series 

(not shown), taken at 0439 (-14.4° solar depression angle), a very faint red 

glow appeared on the horizon. This evidence of sky color at such a large 

solar depression conforms with observations from various locations following 

the eruption of Krakatoa in 1883. 

xi 

GEOPHYSICAL tlONITORING FOR CLHIATIC CHANGE 

NO. 11 

Summa ry Report 1982 

1. SUHtIARY 

At MLO, a new steel building was constructed to house the lidar and pol ar imeter systems . The existing lidar dome was re quired for a new solar 

tracker on which a py rheliorneter, seven-wavelength radiomete r , and an IR hyg rometer are mount e d. Two vo lcanic cloud s appeared over Hawaii during 1982, 

the Mystery Cloud of unknown origin detected on 27 J anuary and the El Chichon 

cloud detected on 9 Ap ril. Modifications of and additions to the regular 

observational program \<r'e r e made to prov ide a complete record of these important histori ca l events. The Mystery Cloud was centered at about IB-km altitude and had a maximum total-to-Rayleigh backscatter ratio of approximately 

2.5. The El Chi chon cloud was cente r ed a t about 25-26 km and had a maximum 

backsca t ter ratio of abo ut 220. 

At BRI<, NARL remains in a ca r eta ker sta tus and BRI< continu e s to receive 

power from NARL. However , scientific r esearch at NARL has been discontinued. 

GMCC ha s request ed that 100 acres of land surrounding the observatory be 

transferred from ONR to NOAA. This l a nd is temporarily under the custodial 

ca r e of BLH. 

At SHO, the centra l a ir conditioner was r epl aced and new ducting was 

designed t o accommodate t he PV system controller installed in the instrume nt a tion room. Hajor repairs we re performed on the roofs of the GHCC housing 

units and both units were completely repainted. 

At SPO , the 14C sampl er was moved from the skylab to the high- vo lume pump 

room in CAF . At the same time , the decking beneath the pumps was replaced and 

pump-room \I.'iring h'as reconfigured. The enti re CAF wiring plan Y,l as revie\',te d 

and some changes to powe r distribution we re made in the circuit breaker box . 

A new s urvey of the entire SPO complex, including CAF, was performe d. 

The measurement programs co ntinued at the four GHCC obs ervatories . These 

programs include CO 2 ) total columnar ozone, ozone vertical dis tribution, surface ozone, strato sp heri c water vapor, CFC-ll and -12, N2 0, stratospheric 

aerosols, volumetric aerosol scattering coefficient, eN concentration, solar 

radiation, meteorological variables, and precipitation chemistry. 

The co ntinuous CO 2 mea surement prog ram continued at all f our stations . 

The entire reco rd of CO 2 data at each station has been edited, corrected, and 

converted to the X81 mole fraction scale. The four stations yield a mean 

global CO 2 growth rate of about 1.50 ppm yr- 1 . A total airborne fraction of 

about 0.54 still seems appropriate for a total industrial production of about 

36 Gt of ca rbon during 1976-1982. The l atitude gradient of CO 2 fr om BRI< t o 

SPO has remained fairly constant at about 3 .5 ppm during the la st decade, 

although variations of up to 0.5 ppm related to ENSO events occurred during 

1976, 1979 , and 1982. The_C0 2 annual cycle at BRI< and HLO has increased in 

amplitude by - 0.6%-0. B% yr l ove r the last two decades and the HLO annual 

cycle may have increased by as mu ch as 2% yr- 1 since 1975 . 
The CO 2 flask sampling sites remained nea rly the same as in 198 1, although sampling at Fal kland Islands a nd Poi nt Six Mountain, Mont., wa s discontinued and new cooperative s tations were initiated nea r Chris t chur c h, New 

Zealand ; Halley Bay, Antarctica ; Cape Mea res, Oreg.; and Kitt Peak , Ariz. The 

entire flask data set since 1968 ha s been edited, corrected, and co nvert ed to 

the X8 1 mole fraction sca le. An i mportant result from the flask network i s 

the fine definition of the latitud i na l gradient and a nnual cycle, particularly 

in the equatorial regions whe re the atmospheric concentra tion is sensitive t o 

ENSO events and oceanic upwel l ing . The flask CO 2 data a l so show a gradi ent of 

about 3 .5 ppm between BRW a nd SPO . 

Total ozone observations with Dobson spec trophotomete r s conti nued at the 

four GMCC observatories and seven contiguous U.S. stations . Observations were 

discontinued at White Sa nd s, N. Mex., a nd BRW , but a new sta t ion was es t a blished in Fresno, Ca l if. Work continued with the \mO Globa l Ozone Research 

and Monitoring Project t o upgrade for e ign Dobson spectrophotome ters . Special 

calibration lamps , which were calibrate d using World Standard Dobso n In strument no . 83 , have been s upplied for all Dobson spectrophotome t ers a round the 

world t o maintain calibration on a n absolute sca l e . Ozone vertical profiles 

were obtained i n Boulder using an automated Dobson ozone spectrophotome t e r f o r 

Umk e hr observations . This automated ins trume nt was also used to perfo rm 

sta ndard t ot al ozo ne observa tions. Mon th ly ozo nesonde flights were made in 

Boulder, Co l o ., and Hilo , Hawaii , usi ng balloon-bo rne ECC instruments for 

comp arison with ozone profiles ob t ained usi ng the Umkehr t echnique . The Hilo 

flights were initiated in Sep t emb er to study the impa c t of El Chichon a nd will 

be continued for about a yea r. Surface ozo ne meas ur eme nts continued at the 

four GMCC observa t ori es. Least-squares tre nd a nalyses for the surface ozone 

record show no significant tre nd s ; however, l arge annual cy cles are evident a t 

all four observatories . 

The stra to spheri c wate r vapor meas ur ement program was conti nu ed in Boulder , Co l o. However , because o f probl ems wi th neopr ene bal loons, only six 

s uccessful monthly fl ights were possible. 

The halocarbon and N2 0 measur ement program continue d at the four GMCC 

observatories and at NWR . I nsta llation of a n air cond itioner in the Boulder 

analysis labora tory prod uced mor e consistent results f rom the fla s k analyses . 

Ca libration gas sta ndard s we re fou nd to be stable since 1977 . CFC- II and -1 2 

data s how mean mixing ratios in the ranges 202 - 215 and 345-365 PEtv , r espec -

tively, a nd growth r ates in the ra nges o f 10-14 and 9-1 6 pptv yr I, respec -

tively . N2 0 data show mea n mixi ng ratios in the range 302- 310 ppbv and growth 

rates in the r a nge 0.6-1 . 6 ppbv yr- 1 . 

Li dar measureme nts of str a t osphe ri c aeroso l profiles co ntinued at MLO . 

In creased numbers of observa tions were made to provide more de t ai l ed descriptions of the Myste ry Clo ud and t he El Chi chon c l oud. 

Co ntinuous measureme nts of vol ume tri c aeroso l light scattering and eN 

concentrati on co ntinued at the four GMCC observato ries . The entire data set 

has been edited a nd corrected a nd a new l east-squares trend a nalysis s howed no 

significant long -term trend at any sta tion. 

The solar radiation meas ureme nts 

tories . Photometers operati ng at the 

to the program at all four stations. 

continued at the four GtlCC observa -

778 - and 862 - nm wavele ngt hs were added 

An IR hygrometer was installed at SPO . 

2 
Development of the GMCC atmospheric trajectory program continued with two 

new versions in addition to the original program that produces backward isobaric trajectories for the Northern Hemisphere. One new version uses gridded 

data for every 2 . 50 of latitude and longitude and can produce backward isobaric trajectories anywhere on t he globe, including trajectories that cross the 

Equator. The newest version produces backward isentropic trajectories that 

trace paths determined by the wind field on s urfaces of constant potential 

temperature. 

GMCC personnel conducted numerous research projects and data analyses, 

many of which are summarized in sec. 4 . Several of these studies used the CO 2 

record. A two-dimensional model was developed that simulates vertical and 

latitudinal CO 2 transport in the atmosphere; CO 2 flux into, out of, and within 

the ocean; and CO 2 flux into a nd out of the biosphere . Comparison of the 

model results with the CO 2 measurement record shows that the model can explain 

a large proportion of the variability of CO 2 during the year. A study was 

performed correlating the variability of BRW CO 2 concentration with atmospheric flow regimes, meteorological va riables, pollution aerosol measurements, and 

air mass origin. It was concluded that much of the Arctic is not a CO 2 source 

and that the Arctic is most strongly influenced by direct transport from midlatitude industrial source regions. 

In May-June, GtlCC participated in a cruise aboard the R/V DISCOVERER in 

the equatorial a nd northern Pacific Ocean. Thirty-six pairs of flask samples 

were collected for subsequent analysis by the MTG group. These shipboard data 

are valuable for determining atmospheric CO 2 gradients over this region of the 

Pacific and identifying possible marine sources and sinks of CO 2 . 

Special skylight polarization measurements were made at tlLO to detect the 

effect of the El Chichon stratospheric dust cloud . The dust cloud caused a 

reconfiguration of the polarization field compared with that for a clear 

atmo sphere . 

Aerosol and solar radiation experiments continued at WHI during the summer of 1982 . Preliminary results indicate that the most hazy conditions at 

I.HI were when trajectories arri ved from the west after passing over the Great 

Lakes region. Trajectories from the east, having a maritime origin, gave the 

clearest conditions, and trajectories from the north or south we re representative of continen tal background cond itions. A trajectory study at MLO showed 

that the springtime Asian dust event at NLO was significantly greater in 1979 

than in s ub sequent years because of a more direct transport route from the 

Asian deserts in 1979. Subsequent years show trajectories with l ess curvatur e 

a nd origi ns to the south of the Asian deserts. 

Work continued on the development of the Umkehr method for determining 

t he ozone profile in the stratosphere. The appearance of the El Chichon dust 

cloud provided an opportunity to investigate possible errors in the Umkehr 

measurement caused by stratospheric dust. 

The GMCC ARtI group participated in three NASA flights designed to establish the latitudinal extent and variability of the El Chichon dust cloud. The 

flights were near the . tropopause so that the optical depth of the stratosphere 

could be me asured as a function of latitude from BRW to New Zealand . Significant latitudinal variations existed at least 8 months after the eruption. 

Normal incidence irradiance at MLO a na lyzed by .the apparent transmission 

3 
method was compared with actual solar irradiances obtained by the Robinson 

method. Previous to the EI Chichon eruption a linear relationship existed 

between the results of the two methods. The eruption of EI Chichon resulted 

in the largest decrease in normal incidence flux measured at MLO since measurements began in 1958, and the linear relationship between apparent transmission and absol ute flux no l onger existed. 

In 1982, mlcc supported a substantial number of cooperative research 

proj ects. Fourteen summary reports resulting from these proj ects are pre -

sented in sec. 5. They cover such topics as atmospheric benzene and toluene; 

aerosol absorption, composition, and si ze distribution measured at MLO during 

Asian dust episodes; solar radiation at BRIY; CO 2 and other gases measured at 

Palmer station; Raman study of graphitic carbon in the Arctic ; a global network of sunburning UV solar radiation meters; a sampling strategy to avoid the 

problem of aliasing at tILO; a model study of atmospheric electrical properties 

above a mountain s uch as Mauna Loa; a comprehensive study of atmospheric bromine in the Ar ctic; a spectral analysis of meteorological and aerosol chemistry data at BRW; and a study of the long-term change in the amplitude of the 

seasonal cycle in CO 2 at MLO. 

4 
2. OBSERVATORY REPORTS 

2.1 Nauna Loa 

2.1.1 Facilities 

A new 14- x 20-ft steel building was constructed at the observatory site 

to house the lidar and polarimeter systems that were moved from the Ash Dome . 

The dome was req uired for installation of a new solar tracker. A special 

requirement for the steel building was a port in the roof t hat could be opened 

for taking lidar and skylight observations. The building was purchased from 

Porta House of Oakland, Calif., and erected on the site by a local contractor . 

Although the building was completed in early Nay, the instrumentation was not 

moved until 24 August. 

The tracker was delivered from Boulder to MLO in Septemb er, and its installation in t he dome was completed by Boulder personnel in early October. 

The instruments mounted on it are an Eppley pyrheliometer, a seven -wavelength 

radiometer, and an IR hygrometer. Operation of the instruments was generally 

satisfactory once a problem with the data-logging system was resolved . 

The four -wavelength nephelometer, which had been in Boulder for repairs 

during the last 6 months of 1981, was returned to MLO and put back in service 

during Nay. It operated well for the remainder of the year. 

The microammeter associated with the Dobson spectrophotometer sustained 

water damage during a severe storm on II February. No ozone measurements were 

made unLil Llle device was replaced about 2 weeks later. 

Sunphotometer SN DIOl5 was taken out of service during January and re -

placed by a new model, SN J202. Unfortunately, this latter instrument had no 

reliable calibration when it was delivered to MLO, and it was not until 

26 February that a moderately precise calibration was obtained . Another sunphotometer, SN J314, which operates in two near-IR spectral regions, was put 

into serivce at MLO on 30 June. Both instruments were used for turbidity 

measurements during the remainder of the year. 

An Optronics spectrometer was borrowed from the University of California, 

Davis, and used for solar spectral measurements at MLO at various times during 

October and November. The Eppley precision spectral pyranometers fitted with 

GG22 a nd OGI cutoff filters were reinstalled on 18 August to obtain more data 

on the effects of the El Chichon volcanic cloud. They had not been in operation for several months prior to reinstallation. 

One of the observatory automobiles, the Ford station wagon, was involved 

in a serious accide nt on the saddle road on 17 September as the observers were 

returning to Hila. After considerable delay, the car was replaced by a 1983 

Plymouth station wagon. 

During 1982, operation of ICDAS improved greatly . 

various reasons for a total of only about 265 hours, or 

It was offline for 

about 3% of the time. 

The walls and door of the precipitation chemistry labora t ory were modified during August to bring them up to GSA fire-proofing standards . The modification was effected without maj or disruption of the program. 

5 
2.1.2 Programs 

T~o volcanic clouds appeared over Hawaii during the year, a nd several of 

the programs were adapted t o maximize the amount of informati on obtai ned unde r 

such anomalous conditions . The first c l oud was originally detected by the MLO 

lidar on 27 January. The source of the cloud is not specifically known , hence 

the term "ilystery Cloud" ge nera t ed by the news medi a. When i t first appea red 

over Hawaii, the ~lystery Cloud "'as centered at abou t 18-km altitude and had a 

maximum to t al-to-Ray l eigh backscatter r atio of approx imately 2 .5 . The Mystery 

Cloud had not comp l etely disappeared from the stratos phere when it was overshado,,'ed by the so-called "ilon ster Cloud" from the 4- 5 April eruption of El 

Chicho n in ilexico . Th e ilonster Cloud was first detected at ilLO on the evening 

of 9 April, although there is some evidence of its ex i stence a da y or t wo 

prior to that date. It was i ndeed a mon ster i n comparison with previous vo lcanic clouds observed a t ilLO , and it persisted over Hawai i, with only a slow 

degradation , throughout the remainder of the year . When first observed , the 

ilonster Cloud had a peak lidar backscatter ratio of about 220, and was centered at 25 -26 km . As t he cloud matured there was a temp orary but very significant buildup of material above 25 km, probably genera ted by gas-toparticle conversion . By year's end, t he upper regi on of the cloud had decreased 1n density, and the peak backscatter ratio o f approx imate l y 10 was 

located in t he 21 - t o 22 -km altit ude region. 

These major geophysical even t s were, and still remain, of great interest 

to the ilLO program. As a result, the freque ncy of many of the regular measurements was increased, and additional obse rvations were added . The net result is that ilLO has what is probabl y the best set of observa t ions of volcan ic 

effects ever assembled by a singl e observatory . odificatio s to some of t he 

measurement programs made in resp onse to the volcani c episodes were appropriate to enable col le ction of the complete da t a set . 

The principal programs carried ou t at ~ILO during 1982 a re s ummarized in 

table 1 and fu rther descri bed be low. 

Carbon Dioxide 

The concentration of atmospheric CO 2 was continuously mon i tored by the 

URAS - 2 NDIR gas a nalyzer during 1982 . The instrument performed sa tisfactorily 

\,'ithout major problems . The al um inum i ntake line on the hi gh tower was repl aced with new tubing on 29 September . Prelimi nary results indi cate that the 

rate of i ncrease of a tmospheric CO 2 co nce ntration had decreased to a pproximately 1.0 ppm yr- 1 f or 1982. 

The GilCC weekly CO 2 flask samp ling programs at ilLO and KUiI continue d 

during the yea r. fla sks were l ost or bro ke n during shipmen t on only two 

occas i ons . 

The study of possible vertical CO 2 gra dients in the atmospheric boundary 

layer at ilLO was completed s uccessfully, with the result that th e magnitude of 

any persistent gradient was below t he l eve l of de t ec tion. 

Outgassing from the volcanic ca l dera at the s ununit of launa Loa ca used 

disrupti ons of some CO 2 records in every month o f the year. It occ ur re d mainly between midnight and 0800 LST during th e downslope wind flow regime . The 

mon thly occurrences of out gassi ng are liste d in table 2 . 

6 
Table 1. --Summary of sampling programs at LO i n 1982 

Prog r am 

Gases 

--carbon dioxide 

Surface ozone 

Tota I ozone 

Ozone profi Ie 

CFC-I l, CFC- 12, and /120 

Aerosols 

Co nden sation nuclei 

Op ti cal properties 

Stratospheric aerosols 

Skylight po larizati on 

Solar Radiation 

Global irradiance 

I)irect irradiance 

/h ffuse i rradiance 

Turbitllty 

Meteorology 

Ai r temperdlufe 

Soi I temperatufC> 

De~'point tempe f ature 

Relal lW' humidity 

PreSSUfr 

"Hnd (spero .>lld dir£'C'lion) 

Preriplt.lt ion 

I'feli!~~tion CII("mlstr}, 

I,ll 

Conomtlv lty 

Chemi (';1 1 ('ompOlw nts 

Coopera llY(' Pro rams 

Carbon dioxide 5JO) 

Surfare 502 (EPA) 

Total surfare Il.lftlruJ.He s 

([WE) 

Instrument 

UR.4.S- 2 infrared ana lyzer 

0,5- .2 glass flasks, pl 

0.5 -.2 glass flasks, through analyzer 

5 - .2 evacuated glass flasks 

Dasibi ozone meter 

Dobson spectrophot ome lers nos. 63, 65 

Dobson spectrophotometer no. 65 

Balloon- borne ECC 

300- m.2 stain l ess s t eel flasks 

Pollak CIlC 

G.E . CNC 

our -~'avelength nephelome t er 

Lidar 

Polarizing radiomet er 

Eppley pyranometers ~'ith Q, GG22, 

OG[ , ,1nd RGB filters 

Eppley pyrhel iome t ers (2) ~'i th 

Q filters 

Eppley pyrhel iometer ",'i th Q, OGI , 

RG2 , and RG8 filters 

Eppley pyrheliometer ""ith [3 filters 

Seven-...,aveleng th radiometer 

Eppley py r anomete r ~'ith shading d isk 

and Q fi ltc,' 

Sunphotome te rs ~·i th 380-, 500- , 778 - , 

and 862 -nm na rro ... 'band fi i t e rs 

Thermistor 

l1ax.-mlll . thermometers 

lIygrot hermograph 

Thermistor 

De~'Poln t hygrometer 

HY)~ ro t he rmog r.ll'h 

51 illg psyc hrom('ler 

Capacitance transducer 

llcr obarogravh 

t.'rcu l' ial barometer 

BendIX Ae r OVilllt' 

Ha i n gage, 8- i n 

Rain gage, 8-111 

Rain gage . tipping bucket 

Foskett Infrared hygrometer 

Spect r al infrdl'('d hygrometer 

I'll m('tC'r 

Conduct I ... ity hritlge 

l un l·hroma t og r.l ph 

Infrarf'd aIlJly~t'r (API'IIf'd Physics) 

5 -.2 ev.lC'uate,1 g lass flasks 

Chemi c'll hubhler system 

High-volume saml'it'r 

TotJI surfa ce particulates High - volume s.tlDpier 

( EPI\ ) 

l\ tmosl'hf'ric electrici ty 

(Unlv. of ninnesota) 

Ult ra violet radiation 

(Temple Unlv.) 

I'r e('ipl t dtl on coll e ction 

(DOE) 

Precipita t ion collection 

(EPI\) 

Precipitation collection 

(Unl v. of Paris) 

PreCipitation collection 

( IAEA) 

\oet - dry depOS i tion 

(Unlv. of Il l i nois) 

Ae rosol dlem l s t ry 

(Ulll .... of Mary l and) 

Ae roso\ chem is t ry 

(UIII\'. of ,'trl ;.:olla) 

I:lC (USGS, UCIIVCr) 

Radioc<lrbons (USGS, 

Menlo I',nk ) 

Field tnill, air comluctlvlty meter , 

surfilce .lIltC'lUhl 

Ul tr,lv l olet radlometf'r 

HASI. ~,(· dry col\f'ct o r 

~"sco model 9J 

I.lkens fUIHu·1 coll("(tor 

1.1 ken s funne I to II e("tor 

Expos('\.1 colle("tloll 1).11 Is 

Nudepo rt' filters 

Qua rtz filters 

10- 2 st.llnless st('('1 f l asks 

NaOlI collcctor 

7 

Sampl ing 

frequency 

Continuous 

paIr ~'k-' 

I pair ~'k-I 

1 pair .... k- ' 

Continuous 

3 day - 1 

, obs. ~k - I 

I ... ·k - , 

I pair ~'k - 1 

Discrete 

Con tinuous 

Con t inuous 

Discrete 

Discrete 

Continuous 

Continuous 

Discrete 

Continuous 

Cont illuous 

Continuous 

Discrete 

Continuous 

I day-I 

Continuous 

Continuous 

COll t imlous 

Cont i ntiOliS 

Lit scretc 

Con tinuous 

Continuous 

Disc r e t e 

COllt illIIous 

I day -, 

T ... ·ice ... k-' 

COll t il1UOU5 

Con tllluouS 

Contin uous 

Dlsrr(' l e 

Ihscrett' 

01 screle 

Con tinu uus 

1 pa I r ... 'k - 1 

Every 12 days 

Conti lluous 

Every 1l days 

Con tinuous 

Continuo us 

Co ntinll u~ 

Con t inuous 

Continllous 

Con t inuous 

Cont I IltIOUS 

2 ·k - I 

Ulscrete 

Rema rks 

Mountain and seacoast 

11 0untain and seacoast 

No. 63, Ja n - May; no. 65, 

Jun-Dec 

Umkehr . Nov - Dec 

From Hilo Atrport 

4 meas., ~'eekdays; 0, ~·eekends 

450 , 550, 700, 850 rum 

694.3 rum, 2 J 

8 ~'avelengths 

m.o and Kulanl l1auka 

MLa .1nd Kulanl ~Iauka 

Kulanl Iauka 

Raln ... ·.ll er collec t ions , 6 sites 

unlaln and s('a c oa Sl 

U"penc\f'lIt on ~Ind ,ll rec t lon; 

1 flll!"r 'k L 

Radial ion responSible for SUI1 -

burrllng of ski n 

N.-\DP 

Uay - nlght lhscrlmlnat Io n 
Table 2.--Honthly occurrences of outgassing from the 

volcanic caldera on Hauna Loa during 1982 

Jan Feb Har Apr Hay Jun Jul Aug Sep Oct Nov Dec 

No . of days 10 5 10 5 8 10 3 3 9 17 5 13 

Percent of days 32 18 32 17 26 33 10 10 30 55 17 42 

Ozone 

Surface ozone was meas ured continuously with a Da sibi ozone me t er . Total 

ozone in the atmospheri c col umn was me asured on about 230 days during 1982 

using a Dobson spectrophotometer. In addition , this instrument was used for 

measuring the ozone profile by the Umkehr technique 5 days per week from 

10 Hay to the e nd of the year in a n effort to determine the effects of the El 

Chi chon cloud on atmospheric ozone. 

A special series of ozonesonde observations was started during a visit of 

Boulder personnel to HLO in the last half of September, and was continued as 

an HLO program through the remaind e r of the year . This program was also 

started in response to the vo l canic cloud. Ten flights were made ove r the 

3 .5-mo period . 

Surface Aerosols 

Both the G.E. and Pollak CNC's operated normally throughout the year . 

The four-wavelength nephelometer was returned to operation in Hay and yielded 

good data for the remainder of the year. 

Stratospheri c Aerosols--Lidar 

The HLO lidar observations of the two volcanic clo uds over Ha wa ii durin g 

1982 are the most compl e t e taken a nd consti tute an excellent data set for 

characterizing the stratospheric clouds . HLO was in a very advantageous location for the observations , because the cloud was initially confined to the 

low-latitude regions of the Earth and was thus not obs erved at the numerou s 

lidar stations at more northerly latitudes. Therefore, the rapid changes of 

the cloud during its first several weeks of existence were observed only at 

HW. 

The lidar equipment operated quite well throughout the year considering 

the age and complexity of the system. Seventy observations were made in 1982, 

each obse rvati on consisting of 60-150 laser s hots. Observations of the El 

Chichoft cloud taxed the capabi lity of the system because of the high altitudes 

reached by the volca nic material and the limited dynamic range of the 8-bit 

analog -to-digital converter. In man y cases, mUltiple profiles were taken with 

diffe rent settings of signal delay and photomultiplier voltage to extend the 

range of the system. In addition, it was necessary to obtain profiles in the 

lower altitude range to determine the mo st appropriate altitude for normalization of the lidar response. 

8 
Solar Radiation 

A great deal of empha sis was put on solar radiation observations at ~lLO 

during 1982 to characterize the effects of volcanic clouds on the solar radiation regime . The freq uency of sunphotometer and filter-wheel pyrheliometer 

measurements was increased; a second sunphotometer operating at near-IR wavelengths was put i nto use; and two spectral pyranometers that had previously 

bee n removed were put back online. 

Solar-tracking capability was improved by the installation of a sophisticated active tracker . The multiwavelength filter radiometer mount ed on 

the tracker greatly extended the spectra l measurements being made. As a result of these improvements, the solar radiation observations at MLO are some 

of the best a nd mo st complete availabl e for assessing the radiative effects of 

volcanic clouds. 

The intensity and polarization of s kylight were meas ured frequently during the year to determine t he l ight-scattering effects of the volcanic cloud . 

It was found that the cloud had particularly pronounced effects on the polariza tion field, although th e skylight intensity also changed significantly. The 

maximum polarization at near-IR wavelengths was decreased by a factor of 2 by 

the cloud, a nd t he distribution over the sky was modified significantly. The 

results have been desc ribed by Coulson (1983a, 1983b), and further wo rk is in 

progress. 

Meteorology 

eteorological measurements continued withollt major problems throughout 

the year. 

Precipitation Chemistry 

Pre c ipitation chemistry continued without problems at about the same 

level of activity as in prior years . 

Cooperative Programs 

The relatively large number of cooperative prog r ams continued normally 

through 1982; some new projects were added; and some special projects were 

pursued by visiting scientists. A brief summary of coopera tive efforts 

follows. 

Aerosols continued t o be co llected on Nuclepore filters for the University of Maryland and on quartz filters for the University of Arizona. An 

e l ectronic co ntroller operated the pumps on the basis of wind speed and direc -

tion, particulate content o f the ambient air, and time of day. Both projects 

were co ntinued throughout the year, a nd filters were changed on a weekly schedule . A daily schedule was used in cha nging filters for an aerosol absorption 

study by the University of Washington. The aeroso l collection equipment of 

the University of California, Davis, was taken offline and returned t o that 

institution on 23 February. Special aerosol studies were made by W. Zoller 

a nd three students from the University of Maryland over a IO-day period in 

Hay. A. Cla rke of the University of Washington spent the peri od 20 April31 Hay making different types of aeroso l me as urements at HLO, a nd l e ft his 

col lectors for HLO person nel to operate when he returned to Washington. 

9 
J . Gras from CSIRO, Helbourne, Australia, spent 2 weeks in April at MLO collecting and analyzing aerosols. E. Butler from URI visited HLO for 3 weeks in 

September and October to collect methyl iodide and selenium aerosols . Aerosols continued to be collected by high- volume samplers for DOE and EPA. 

J. DeLuisi and E. Dutton of GHCC in Boulder made special solar radiation 

observations in Septemb er and October to characterize the radiative effects of 

the El Chichon volcanic cloud. They also installed the solar tracker and 

radiometers in the so lar dome, and trained HLO personnel on their operation. 

In November, W. Egan from Adelphi University spent a few days at HLO measuring 

the intensity and polarization of skylight in an effort to validate the aerosol models he developed for the El Chichon cloud. Erythema radiation measurements for Temple University continued throughout the year. 

Three new cooperative projects for studies of atmospheric gases were 

started at MLO during 1982. A project for supplying flask samples of air from 

the observatory on a weekly basis for OGC was started in January and continued 

for the remainder of the year. The air samples are for measurements of the 

concen trations of six radiatively i mportant trace gases in the atmosphere. A 

Brewer spectrophotometer was brought to tlLO by AES of Canada on 25 April and 

put i nto operation for measurements of the total ozone and S02 co ntent of the 

atmospheric column. The instrument was operated daily by MLO personnel during 

the last 8 months of the year. Samples of CO 2 collected by relatively longterm exposure of vats of NaOH solution at HLO were analyzed for their radiocarbon content by the USGS, Henlo Park . 

In addition to these new 

SID's CO 2 analyzer, and flask 

to SID and to USGS, Denver. 

cooperative projects, HLO continued to operate 

sampl es of air from HLO continued to be supplied 

S02 samples were taken weekly for EPA . 

HLO continued to participate in NADP by send ing wet and dry samples of 

atmospheric deposition to the Illinois Sta t e Water Survey . Bulk collections 

of atmospheric deposition were supplied all year to DOE. In addition , precipitation samples were s upplied on a routine basis to the University of Paris 

and IAEA. In a short-term project, six rainwater samples were sent to the 

Argonne National Laboratory for special analysis . 

Two sets of equipment operated at HLO throughout 1982 [or measurement of 

atmospheric electrical parameters. The equipment installed many years ago by 

W. Cobb, and now under the nominal direction of NCAR, operated well. Continu -

ous records of potential gradient, air-Earth current, and positive and nega -

tive conductivity of the a ir were obtai ned . The instruments of D. Ol son of 

the University of Hinnesota for measuring potential gradient and air- Earth 

current also continued in operation, and the records were se nt to him regularly. 

2.1.3 MLO Meteorological Museum 

The following items were added to the mu se um co llection: (1) an oZonesonde developed in Germany by H. Paetzold and F. Piscaller for the 1957-1958 

IGY, (2) sampl es of vo lcani c ash from the eruption of El Chi chon, (3) a Boller 

and Chivens anemometer, and (4) miscellaneous books and publications on meteorology and related fields . 

10 
2 . 2 Barrow 

2.2.1 Facilities 

NARL, overseen by IT&T and Calista Corporation (a southern Alaskan native 

corporation) , is still furnishing power to BRW. Scientific research at NARL 

has been discontinued, and the complex is being maintained on a caretaker 

status . 

NWS is planning 

town airport runway . 

station personnel. 

to build a new station and housing complex east of the 

G~ICC has requested two living quarters there for future 

G~ICC is officially requesting transfer, from ONR to NOAA, of the title to 

100 acres of land surrounding the observatory_ Thi~ l~nd, ~l ~g ~ith @UC!I vf 

the land northeast of the town of Barrow, is temporarily under the custodial 

ca re of BUI. 

A new Notocross 300 snowmobile was purchased for transportation on the 

open tundra when the access road becomes heavily snow covered in the winter . 

The Bambi all-terrain vehicle was back in operation after a series of repairs. 

The 1969 Chevrol et pickup truck was excessed. 

2.2.2 Programs 

Programs carried out during 1982 at BRH are listed in table 3. Comments 

on some selected programs follow. 

Ca rbon Dioxide 

Because of a broken glass rod in the reference cell chamber, the URAS-2T 

analyzer was down for a few weeks in January. In addition, errors in the data 

l inearity known as closure occurred early in the year and were corrected after 

an optical aligmnent. A new Single - source reference cell was installed in 

J une. The special ground-line sampling project designed to measure C02 flux 

near the surfa ce continued with increasingly good results. 

Ozone 

The Dasibi surface ozone meter performed well throughout the year . In 

Decembe r, Dobson spectrophotometer no. 76 was returned to Boulder for 

calibration . 

Halo carbons and Nitrous Oxide 

Weekly flask sampling went smoothly for the year. 

Surface Aerosols 

Performance of the G.E. CNC was erratic. Absorption problems with the 

humidifier wick occurred, and the vacuum pump was repaired. The Pollak CNC 

and the four-wavelength nephelometer generally performed well throughout the 

year . 

11 
Table 3.--Summary of sampling programs at BRI, in 1982 

Program 

Gases 

--carbon dioxide 

Surface ozone 

Total ozone 

eFe -II, eFe-I2, and NzO 

Aerosols 

Condensation nuclei 

Optical properties 

Aerosol chemistry 

Solar Radiation 

Global irradiance 

Direct irradiance 

Turbidity 

Heteorology 

Air temperature 

Soil temperature 

Temperatu r e gradient 

Del..'point temperatur e 

Rela tive humidity 

Pressure 

Wind (speed and dire c ti on) 

Wind (turbulence) 

Precipitation Chemistry 

pH 

Co nductivity 

Cooperative Programs 

To t al surface parti culates (DOE) 

Aerosol chemistry (URI) 

Particulates (Carnegie-~ e 1100 Un iv. ) 

Global radialion (SRL) 

Ul traviolet radiation (Temple Uo iv. ) 

Carbon dioxide (510) 

Precipitation gage (ASCS) 

Carbonaceous particles (L8L) 

Halocarbons (OGC ) 

In ciden t and reflected radiation 

(Univ. of Alaska) 

Nagnetic fields (USGS) 

13C (USGS) 

Instrument 

URAS - 2T infrared analyze.r 

0 .5-Q glass flasks, p3 

0 .5-Q glass flasks, through analyzer 

5- Q evacuated glass fla s ks 

Dasibi ozone meter 

Dobson spectrophotometer no. 76 

300 -mQ stainless steel flasks 

Pollak CNC 

G.E. CNC 

Four-wavelength nephelometer 

Streaker, Cascade impac tor 

Eppley pyranometers with Q and RGS 

filters 

Eppley pyrheliometer with Q, OGI , 

RG2 , and RGS filt e rs 

Sunphotometers with 380-, 500 -, 778 -, 

and 862-run narrowband filters 

Thermistor 

Nax. -m i n. thermometers 

Hygrothermograph 

Thermistor 

2 vertically separated thermistors 

Dewpoint hygrometer 

Hygrothermograph 

Ca pa citance trans du ce r 

Nicrobarograph 

Nercurial barometer 

Bendix Aerovane 

2 vertically separated anemometers 

pH meter (samples analyzed at ~ILO) 

Co ndu ctivity bridge (s amples analyzed 

at [110) 

High-volume sampler 

High-volume samplers 

High-volume sampl e r 

6 Eppley pyranometers 

Ultraviolet radiometer 

5-Q evacuated glass flasks 

Wyoming shie lded precipitation gage 

Dichotomous sampler 

(quartz and Millipor e filters) 

High-volume filter 

5-Q stainless steel flasks 

Up -down pyranometers 

Magnetometer 

IO-Q stainless steel flasks 

12 

Sampling 

frequency 

Continuous 

1 pair wk- I 

1 pair wk- I 

1 pair .... 'k- I 

Continuous 

3 day-I 

Ipairwk- I 

Dis crete 

Continuous 

Continuous 

Discrete (tla r-~Iay) 

Conti nuous 

Discrete 

Discrete 

Continuous 

1 day-l 

Continuous 

Continuous 

Continuous 

Continuous 

Continuous 

Continuous 

Continuous 

Discrete 

Continuous 

Continuous (Jul-Dec) 

Discrete 

2 mo- I 

Continuous 

(1 fi lter .... ,k- I ) 

Continuous (one, 

1 filler day-I; 

the o th er , on an 

episodic basis) 

Continuous (Feb lay ) 

Continuous 

Continuous 

1 pair wk - I 

2 mo - 1 

Continuous ( I set 

of filters wk- I) 

Con tinuous 

(I filter day-I) 

1 wk -1 (3 flasks 

sample-I) 

Continuous (program 

ended in Nov) 

station check wk- l 

pair mo- 1 

I 
Solar Radiation 

A new Leeds and Northrup chart recorder was installed at BRW to record 

pyranometer data. 

fleteorology 

New electronic board s to interface the meteorological sensors with ICDAS 

were installed in November. During the Arctic sunmler, two turbulence anemomete r s were insta lled on the met eo rological tower, with approximately a 6-m 

vertical separation. The turbul ence-pa rameter data will be used in a CO 2 flux 

model. CO 2 fluxes near BRW are thought to be caused primarily by photosynthesis, respiration, and decay of tundra vegetation. 

Precipitation Chemistry 

Rain samples were taken on an episodic basis. However, during the summer, samples were often difficult to obtai n because of low rainfall rates . 

ICDAS 

Because of problems in alignment and data sensin g , the tape drive system 

was r eplaced t wice . ICDAS was down most of November and De cember as a result 

of a faulty multiplexe r that interfaces the sensors with the NOVA computer . 

Cooperative Programs 

BRW cooperated willi several groups on programs listed in tabl e 3. The 

following occurred duri ng 1982 : (1) the outside sampling platform, which 

houses several cooperative filter sampl ing programs and is lo cated approximately 30 m south of the main obs e rvatory building, was rewir ed; (2) an additional high-volume impactor wa s added to the LBL aeros ol sampling program; 

(3) during February, filters were expos ed on a second sampling system for URI; 

(4) a new pump was installed for the DOE high-volume filter system; (5) flask 

sample s were taken during three aircraft flights (two in May and one in August), and surface air samples were also taken, supporting the OGC project to 

determine the vertical distribution of halocarbons in the lower Arctic troposphere; and (6) the Unive rsity of Alaska so l ar radiatio n program was rei nstated in June. 

2 . 2.3 Arctic Haze Project 

From approximately mid-March through mid-May, a special intensive data 

gathering proj ect was undertaken to measure basic characteristics of th e Arctic haze . During the project, some existing programs were expanded and new 

ones were initiated. Additional solar radiation mea surements were taken using 

photometers and modified normal incidence pyrheliometers (GfICC and University 

of Alaska). Aerosol chemistry filter samp l es were obtained using a cascade 

impactor and a streaker for subsequent PIXE analysis. Halo ca rbon air sampl es 

were taken with increased frequency for OGC. An atmospheric bromine sampling 

program was initiated by NCAR . 

13 
2 . 3 Samoa 

2 . 3 . 1 Facilities 

No major changes in SMO facilities were made in 1982. Preliminary plans 

for installa tion of the PV sys t em were made, however. These plans involved 

ordering a replacement central air conditioner and designing duct modifications for the ICDAS room where t he PV system controller, inverter, and battery 

bank will be located. Structural timbers for the PV array supports were delivered in earl y December, and air- conditioning work will be completed earl y 

in 1983. In addition, the PV system batteries and scaffolding for use in 

erec ting the PV array supports and the PV array modul es were delivered in 

Decembe r. Co nstruction of the PV supports is sched ul ed to begin in early 

1983 . 

No changes were made in the GMCC remote sampling buildings at the point 

or on the ridge during 1982 . A contract was let to repair and paint the two 

GMCC housing uni ts. The most seri ous phase involved replacement of s hake 

shingles rotted by chronic shading from vegetation adjacent to the house 

roofs . Several trees were removed and over 1500 ft 2 of shingles were replaced. In addition, on one unit, rotted 2 x 6 tongue and groove planking was 

replaced under the shingles. The shade from a large tree kept the area moist, 

and rot had penetrated deepl y into the roof below the shingle layer. The 

units were also completely painted, resulting in co nsiderable improvement in 

their appearance. 

2.3 . 2 Programs 

All 1982 programs are summarized in table 4 . No additions to SHO G~ CC 

programs were made during 1982, however major disruption of all programs occurred on 28 Harch when lightning struck the top level of the remote sampling 

tower located on the ridge, approximately 100 m east of the main building . 

Downtime for damaged equipment ranged from a few days to a f ew months, but 

eventua lly everything was put back online after mu ch he lp from Bould er GHCC 

and considerable effort by R. Williams, the SMO electronic technician. 

Carbon Dioxide 

A URAS - 2T analyzer (SN 00 16), in continuous operation since February 

1978 , was upgraded in Septemb er by installation of a single IR source assembly. A se t of GHCC C02-in-air traveling sta ndard s arrived onsite in October 

and will remain while the regular GHCC standards are returned to Boulder for 

recalibration. The regular standards s hou ld return to SHO by mid- 1983. Period i c use of a GHCC CO 2 -in- air surveillance tank was also implemented duri ng 

October. It was s ubstitu ted for a working-gas t ank during the regular weekly 

ca libration . The G~ICC/SIO joint flask intercomparison continued all year . 

Ozone 

The SMO Dasibi ozone meter was damaged by the lightning strike, and was 

returned to Boulder a l ong with its recorder in late ~Iarch. An int erim instrument sent from Boul der was used until October when the SHO unit was returned 

after repair. Dobson operation using instrument no . 42 was uninterrupted all 

year. 

14 
Table 4.--Summary of sampling prog rams at SNO in 1982 

Program 

Gases 

--carbon dioxide 

Surfa ce ozone 

Total ozone 

CFC-l 1, eFC- 121 a nd N2 0 

Aerosols 

Condensation nuclei 

Optical proporties 

Solar Radiation 

Global irradiance 

Direct irradia nce 

Turbidity 

te orology 

Air temperature 

Soil temperature 

De\<,'point temperature 

Re l ative humidity 

Pressure 

Wind (speed and directi on) 

Precipitation 

Precipitation chemistry 

pH 

Conductivity 

Cooperative Programs 

Carbon dioxide (SID) 

ALE project, CFC-I I, CFC- 12 , 

N,O, CHCl " CCI , (OGC) 

CII" CO, CO, (OGC) 

CH, I , CII,CI, CH., CO (OGC) 

13C (USGS) 

Wet-dry deposition (NADP) 

Wet-dry deposition (ENL) 

Bulk deposi tion (E~IL ) 

Instrument 

URAS-2T i nfrared a nalyzer 

O.S-! gl ass flasks , p3 

0.5 - £ glass flasks, through analyzer 

5-£ evacuated glass flasks 

Dasi bi ozone meter 

ECC meter (terminated Sep 81) 

Dobson spectrop hot ometer no. 42 

300 -m! stainle ss steel flasks 

Pollak CNC 

G. E. CNC 

Four-wavelength nephelometer 

Eppley pyranometers with Q and RCB 

filters 

Eppley py r a nometers (2) with Q 

filt e rs on tilted mounts 

Eppley pyrheliometer wi th Q filter 

Eppl ey pyrheliometer wit h Q, OGI, 

RG2, and RG8 filters 

Sunphotometers wi th 380- , 500 - , 778-, 

and 862 -nm narr owba nd filters 

The rmistor 

Nax. -min. thermometers 

Jlygrothermograph 

The rmistor 

Dewpoi nt hygromete r 

Hyg r othermograph 

Sling psychrometer 

Ca pa citance lransducer 

~lic r oba rog raph 

~Iercurial barometer 

Bendix Aerovane 

Polyethylene funn e l, bott le 

Co rning model 125 meter with 

semim icro combina tion electrode 

Beckman model RC -16C meter 

5-£ evacuated gla ss flasks 

HP5840A gas c hroma t ograph 

Carle gas chromatograph 

Stainless steel flasks, 3 set-I 

10- £ stainless steel flasks 

HASL wet-dry co llector (ne\<,' 

Cheme trics, Dec 8 1) 

HASL \<"et-dry co ll ec t or (termi nated 

Nay 81) 

Plastic bu cke t 

15 

Sampling 

f r equency 

Conti nuous 

1 pair wk - 1 

1 pair wk- 1 

1 pair wk- 1 

Continuou s 

Continuous 

3 day-l 

1 pair wk- I 

Discrete 

Continuous 

Continuous 

Continuous 

Continuous 

Co ntinuous 

Discrete 

Discrete 

Continuous 

1 day - 1 

Continuous 

Co ntinuous 

Continuous 

Continuous 

Discrete 

Co nti nuous 

Co ntinu ous 

Dis c rete 

Continuous 

1 day-l 

day -I (G~ICC); 

I wk - 1 (NADP) 

day-I (GNCC); 

I wk - 1 (NADP) 

3 h- I 

1 wk- I 

2 pair mo- I 

\<"k-1.z. wet; 

2 mo I, dry mo- I 
Surface Aerosols 

The G.E. CNC was operational a l l year except for a few days after the 

lightni ng strike . As a result of the l ightni ng da mage, nephelometer operation 

was interrupted from late March to early June, Pollak CNC operation was interrupted for a few days while a replacement power supply was sent from Boulder, 

and the aerosol program chart recorder, which was also damaged, was returned 

to Boulder for repairs. 

Solar Radiation 

Quartz and RG8 pyranometers plus a tracking NIP and filter-wheel NIP were 

ope rational all year except for a period subsequent to the lightning strike . 

All the preamps were replaced and the damaged NIP was exchanged . 

~Ieteorology 

Normal operations prevailed until late March when all se nsors suffered 

l ightning damage. The Aerovane system, temperature sensors , pressure transducer, and all meteorology rack cards were damaged. Fortunately, a complete 

spa re Aerovane system, scheduled for installation at the point, was on hand 

and was used as a replacement. The dewpoint hygrometer and the pressure 

transducer were both returned to Boulder, and remained offline for the rest of 

the year. Temperature se ns ors were in operation again by mid-April. 

Precipitation Chemistry 

Collection protocols remained unchanged from 1981. A GMCC daily bulk 

sample, an NADP ,,'eekly wet-deposi tion sampl e, and a mon thly DOE bulk sample 

program were maintained . Onsite pH and conductivity measurements were performed on NADP and GMCC samples. 

ICDAS 

ICDAS operated normally 

March l ightning strike. The 

exchange of only one board. 

normal operation in mid-May, 

2 . 4 . 1 Facilities 

all year except for a few days s ub sequent to the 

NOVA computer suffered minor damage, requiring 

The mult iplexer-digiti zer was fi nally returned to 

after maj or problems were solved. 

2 .4 South Pole 

The G~ CC CAF at SPO underwent several changes during the 1982 season. The 

high-pressure compressor used for 14C sampling was moved from its skylab location to the CAF pump room and conne cted to an unused sampling stack through 

the ceiling. An automatic pressure s hutoff valve was co nnecte d into the system . While this move \,'as under way , the high-volume pumps loca ted in the 

cabinet in that room were removed, and the decaying decking was replaced with 

1/2-in plywood covered with rubber matting. During reinstallation of the 

pumps, the wiring was replaced and the PISSA ,,'ind controller was brought back 

on line. Figures 1 and 2 illustrate current CAF internal and roof arrangements. 

16 
Halocarbon 

GECNC 

Nephelometer 

CO2 Tanks 

Cryocool 

Go; 

Sampling Stacks 

Aerosol 

o 

Pollak 

Control 

Bo, 

U. of Az. U. 

Clean Clean 

0

Storag3 e "4~f§j~~H; ~d~H~ od~~~1 Folding Table & door Spare GMCC CO2 Tank 

o.&ommon a Storage 

08 a Shelves 

Storage 

DOb r:::::; 

r::----:-T-r-,,-.JL-I Dobson Room 

"=='===til!!!!!!o __ •. NDAA IGMCC 

SUNY 

Storage 

C14 Sphere 

Storage Keeling 

Flask 

Storage 

Solar 

Radiation 

Room 

(NOAA! 

File Desk 

GMCC) FW NIP 

=0 Table 

.,~---Grid Nor1h Keeling Flask 

C14 Sphere 

Storage 

Fi guce 1.--CAF flDDC plan at sPa, 1982. 

\

' _ ____ 17.1m 

GMCC 

Sampling Stacks 

«© u. 

OIA(r\~)"""d LBL 

High VOl ume 

Sampling Stacks 

E 

~ 

~ 

0 I R Hygrometer 

I 

D DOE 

Pump Enclosure 

OGl RGB 

{oJ {oJ (.) I 0 

Pyranometers 

D Dobson Hatch 

NWSNIP 

B ~G8 

::Lers 

11111111111 II , Grid North 

Figuce 2.--CAF coof plan at sPa, 1982 . 

17 

'I 
CAF wiring was reviewed and two remote outlets, one plugged into a wall 

outlet and the other plugged into ICDAS regulated power, were rewired through 

the circuit breaker box, CAF power distribution is illustrated in figs, 3 and 

4, The intake stacks for the various sampling programs were hea t-taped and 

insulated to prevent continuous buildup of ice on them, A complete inventory 

of CAF equipment and spare parts was made, This inventory was entered into 

the station computer and organized so that printouts are availab le by equip -

ment, part, and location , A procedure was a l so established for keeping the 

inventory current. 

CAF is plagued by large temperature fluctuations during the summer, apparently due to solar heating, A thermostatically controlled fa n was installed to help control these fluctuations, Another heat-related problem was 

water leaking into the building from the roof , This probably originated with 

spindrift that worked its way into the roof insulation during the winter , A 

special effort was made to keep the roof clear of snow to reduce this problem 

for the following summer, The heater l ocated behind the C02 analyzer caused 

problems for previo us crews, It was moved to a location near the humid ifier, 

During the summer, several researchers occupied CAI. Their relationship 

with GMCC personnel was remarkable for its spirit of cooperation. Their projects were S2558, S275A, and S279; detailed descriptions are contained in the 

NSF listing of Antarctic projects for 1981-1982 . During winter, Y. Latov from 

the Soviet Union maintained part of his magnetic field project in CAF . 

In the past, problems have been reported concerning human intrusion into 

the Clean Air Quadrant. This year, both the NSF representative and Station 

Manager worked closely with the GMCC Station Chiet. Each arriving scientist 

was briefed by the NSF representative and each arriving support person was 

briefeJ by the Station Manager, resulting in very few unauthorized intrusions 

into the area. 

During the first 2 months of 1982, several station power outages interrupted work at CAF . With normalization of the power plant, these interruptions ceased. The main station experienced t hree fires, one in the fuel arch 

in the primary fuel supply and two in the power plant . There were no serious 

consequences for CAF, however, as a result of these events . During the winter, a new survey of the entire spa complex including CAF was conducted . 

Figure 5 is derived from this new survey, representing the most recent available information . Also, the second spa winter airdrop, which occurred 

21 June , was on the coldest day on record with a minimum temperature of 

-83.2°C. 

2,4.2 Programs 

spa programs are listed in table 5 and are briefly described below, 

Carbon Dioxide 

The CO 2 system experienced a major breakdown . E. Green traveled to spa 

in January to install a new URAS-2T analyzer. Near season's end, the gas 

distribution piping became partially clogged, causing erratic readings for 

several days. With the relocation of the heater, which was formerly behind 

the analyzer, the zero-drift problem of previous years was solved . 

18 
,~ ... '5 ' .' S_~ S~ " ~ P"., ... t;:;-. ;/' .... ·600 600-~' ,'''' 

~::~ ~ ~rl'~';·;·~~ llillJ 

" lAo<o<' , _.,.c· N l<;"' 

" , ~-.... .,. 

.. - " ." -.. ,. " I .... G 

" .... ,. ,,- ll'" ,~ " N 1.<;'" f!!!' ".<0<0' CO 

XI r'o " ...... p;?-. ...,.,. =====illf " , Roco<' 

~ P,o., , 

'", iL ".-. 

'(]o ....... ". ,!. !l.". 

" ,....~_o<' 

, ,-.." 

N ;1..' 0,,,,. R.«<, A,,, • ~A«K' 

I 

:lQ r HU.,.' r ".,'.' I " I , .•.• 'o,~., 

10 r ....... , f!.!i" .... , "I "0 .... 

i'Q r:. ...... , P' .... ,.. nl 

10 \'-! ~~; ... , ~ ....... N r~M I.h: .. M "' '0 ...... 

" ;.1.,_ ... , 0. 0.""", 

n ~S< ••• '1'_"" s.,.-o s,..,· 

n " SOO". , ww' , .... ~ <av.: 

i> " 

" ~!m ........ ~~~~:.. n 1 

.., t-L C.· .. '" '. ',"".e, I ~, " r ~10' "- F~.';;' " , 10 p. ..... ~. l!.. .... .,.. " ~" .. " • n 1 I " !"'-" • ~ . , . , • ;,,.·E .. , 

" Ro<' 

n l'.OO( "

.... 

.0' H.I 

It ~ I 

-l- ICO>S , ,. ~;oo"::- '.0'''' N 

,-

f-------;I- r 

Figure 3.--CAF e l ec trical power c ircuit di agra m, 1982 . 

c, 

1 

0 (0000) 0,~B 000 0000 (0000) 

B' B12 B12 AIIO o QCg C, 0 0 

B7 0 C6 A13 

0 220V .. ET 0 Room 

B' 0 No. 2 0 

Shop A.O !l 0 0 

B" 0 A8 

B' 

0 u 0 

B' 

0 A8 B7 ~g Room 

NO. 1 0 0 B6 B'. 

Hall Room 

0 B6 BIO No. 7 

B' 0 fl 0 

B6 A22 A2<l BIO 

0 220VD OB6 0 DAIS 

,es!. Deck 

A32 Rool and Tower Oullels 

A26 A<' DoE Shaclo; Heater j I OA12 InOV) 

0 

A • 

0" 

[\ 

B'O 

0 

00 0 

A3 AH AI5 

Room 

NO. 3 

A30 

7 

0 

B8 0 Room B8 No. 6 

A19. All 

220V 

\ 

;; 0. 

0 

0 

B5 0 

B5 

A3 o Al3. A25 

220V 

Room 0 0 A3 B5 No. 4 

0 

B7 

0 

B5 

Room 

No "6 . 5 0 

0 

B8 88 Al<l B5 

A20D 0 

B8 

0 0 0 

0 Healer 120V unless 

01her w se spec.t·ea 

Figure 4 .--CAF elec tri cJl ro"er dislribuLion, 1982 . 

19 

I;:;. 

n 

" 

n 

" 

" 

n 

n 

-
> 

. 

w ! 

, 

~ I 

~ I 

:H 

II j ~ tf, :1 I' -'1 ; 

!t. 

! I i} I : II! ! j ! d; 

j i i l ; J ! } ! :,; ~ t 

I ! , 

t i , ' 

~ i 

'! 

Ii 

" " 

, 

~ 

~ 

9 

0 

, 

u 

> 

" ,I 

,i{ 

20 

" " 

I 

,f 1,1 

-::;~l : ,{ , / 

'.' 

I 

~j L_ ' w, __ ,_ 

~;~~ , 

" 

.-'-.-

" 

~ 

~ 

. 

~ 

~ 

--! i; ~ 

~ '" '" '" ~ 

~ 

'" '" 

:>, 

<U 

> 

.. 

::J 

'" 0 

'" U) 

" .- / .' on 

<U 

.. 

::J 

00 

..... 

~ 
Table 5 . --Summary of sampling programs a t SPO in 1982 

Program 

Gases 

-----carbon dioxide 

Surface ozone 

Total ozone 

CFC-II, CFC-I2, and N2 0 

Aerosols 

Condensation nuclei 

Optical properties 

Aerosol chemistry 

Solar radiation 

Global irradiance 

Direct irradiance 

Turbidity 

}\lbedo 

~leteorology 

Air temperature 

Sno .... ' temperature 

Room t emperature 

Water vapor density 

Pressure 

Wind (speed and direction ) 

Total precipitable ..... ater 

Cooperative Programs 

Carbon dioxide (SID) 

Total surface particulates 

(DOE) 

Total surface particulates 

(EPA) 

Aerosol chemistry (Univ . 

of aryland) 

Aerosol chemistry (Univ. 

of Arizona 

Aerosol physical properties 

(SUNYA) 

Carbon aerosol (LBL) 

Halocarbons (OGC) 

13e (USGS) 

I'e (NOAA/ARL) 

Drifting sno ..... (Univ. of 

Alaska) 

Instrument 

URAS- 2T infrared analyzer 

0.5-! glass f l asks, p3 

0.5-! glass flasks, through analyzer 

Dasibi ozone me t er 

Dobson spectrophotometer no. 80 

300 -m£ stainless steel flasks 

Pollak CNC 

G.E . CNC 

Four- wavelength nephelometer 

Sampling 

frequency 

Continuous 

1 pair wk - l 

1 pair wk- l 

Continuous 

3 day-l 

pairwk- l 

pair .... 'k- I 

austral summer 

Discrete 

Continuous 

Co nti nuous 

Streaker, Cascade impactor Discrete 

Eppley pyranometers with Q, OGI, and Continuous 

RG8 filters 

Eppley pyrheliometers with Q and RG8 Co ntinuous 

filters 

Eppley pyrheliometer ..... ith Q, OGI, RG2, Discrete 

and RG8 filters 

Sunphotometers wi th 380-, 500-, 778 - , Discrete 

and 862- nm narrowband filters 

Eppley pyranometers with Q, OGI, and Continuous 

RG8 filters 

Thermistor 

Thermistor 

Thermisto r 

Du Pont 303 moisture monitor 

Capacitance transducer 

Nicrobarograph 

Nercurial barometer 

Bendix Aerovane 

Infrared hygrometer 

5-! evacuated glass flasks 

lIigh-volume sampler 

High - volume sampler 

High-volume samplers 

High-volume samplers 

Pollak CNC ..... ith di ffusion baltery 

High-volume sampler 

5-! stainless steel flasks 

10-£ stainless steel cylinder 

3,000 psi spheres 

Sno .... ' crysta I counter 

21 

Continuous 

Continuous 

Con t inuous 

Continuous 

Continuous 

Continuous 

Discrete 

Co ntinuous 

Discrete 

2 mo- l (3 flasks 

sample- I) 

Co ntinuous 

(I filter wk - l ) 

Continuous (I filler wk - I) 

Continuous 

Co ntinuou s 

Discrete 

Continuous 

Twice mo- l 

(3 flasks 

sample - I) mo - l 

(2 cyl i nders 

sample - I) 

500 psi day - I, 

austral summer 

Con t inuous 

Remarks 

Jan 74-present 

(excl . Nov 78-

Nov 79) 

Jun 8I - present 

Nov 79 - present 

Jan 76-present 

Dec 63-present 

Ja n 77 -Dec 79 

Jan 80-present 

Jan 74-present 

Jan 74- present 

Jan 79-Dec 79; 

Jan 8I- present 

Jan-Dec 82 

Feb 74-present 

Oct 75 -present 

Jan 77-present 

Jan 74 -p resent 

Jan B2-present 

Har 77-present 

~Iar 77 -present 

Jul 78-p resent 

Nar 77 -p resent 

nec 75-present 

Feb 80 -p resent 

Jan 80 -p resent 

nec 75-present 

nec BI-Jan 82 

1957-present 

Nay 70-present 

Nay 70 - present 

Jan 79 -present 

Jan 82-present 

Jan 74 - present 

Jan 82-present 

I980-present 

Jan BI-present 

I972-present 

Jan 82 -present 
The p3 sampler was difficult t o operate during the co ld winter months . 

Two heat gun s were pointed continuously a t th e f lask valves to facilitate 

closing them when the temperature was lower than -SO·C. 

Ozone 

The surface ozone program continued t hrough the year with no major 

problems. 

Haloca rb ons 

Ha l ocarbon collection presented no problems this year. 

Surface Aerosols 

The main sources of trouble in the ae roso l program were the G.E . CNC and 

the Polla k CNC microammeter. The optical chambe r of the G.E. CNC flooded 

s hortly aft er reinstallation following its return to sPa . During the year 

this instrument drifted more than expec t ed probably becau se of a leak in the 

air intake path. The microammeter used for Pollak counter readi ngs failed in 

Ap ril, and a substitute was used un til the midwin t e r a irdrop in June . 

Solar Radiation 

Solar radiation was monitored without maj or probl ems . Du ring the·s ummer 

an IR hygrome t er meas ur ed discre te t ota l- co lumn water-vapor l eve l s several 

times a day. A new discrete and continuous a lb edo mea s uring system was installed this year . 

Meteorology 

The only major problem in the me teoro l ogy program was the failure of the 

Du Pont moistur e monitor , which prevented co llection of further moisture data. 

ICDAS 

ICDAS failed 24 times during 1982 . Four failures were related to the 

sta tion power - plant fires; one was because of opera t or erro r ; one occurred for 

no known reason; and the remaining were caused by erratic station-ge nerator 

gove rnors . A tape-transport problem delayed da ta collection for several days. 

This year, al l returned data tape s we r e sea led in meta lized pla s ti c 

Polyseal. 

Cooperative Programs 

No problems occurred with the SIO CO 2 flas k sampling program. The DOE 

aeroso l sampling sys t em lost only a few hours of da ta fr om a mechani ca l and an 

electrical failure during the year. No problems occurred with the OGC ha locarbon flask sa mp l ing program or the USGS 13C program. 

The University of Maryland and University of Arizona aeroso l chemistry 

sys t ems were not fully operational when the sta tion opened i n Novemb er 1981. 

The installation was electrically makes hi ft and physically deteriorated. The 

wind-s ector controller was nonfuncti ona l except as an on/off switc h for eac h 

22 
unit. The system was physically and electrically upgraded and the controller 

was repaired . The downpipes were heat-taped to prevent icing . During the 

winter, the r e were severa l pump fail ures . The University of Arizona system 

suffers from a design defect that allows the filter to be sucked up the intake 

pipe when the hol der is opened for filter r emoval . 

The newl y installed LBL carbon aerosol system consists of a r oof intake, 

flexible downpipe, filter hold er (IO-cm diameter), and another downp ipe co nnected to a pump. The pump exhau st flows through a continuously registering, 

accumu lating flow meter. The hard pipe between the filter and the pump broke 

as a result of vibration, and was replaced with a fl ex ible tube. The pump 

mo t or developed problems with the centrifuga l switch, which eventual ly was 

bypassed with a toggle switch. 

The newly installed snow crystal counting system turned out to be temperature sensitive and wo uld not function properly below -SooC. An electromag -

ne tic i nterfe rence problem with one of the other spa projects also affected 

the results of the system . 

23 
3 . CONTINUING GHCC PROGRAI'lS 

3 .1 Carbon Dioxide 

3 .1 . 1 Continuous CO 2 Heasurements 

Continuous measurement of atmospheric CO 2 by NDIR analysis conti nued in 

1982 at the four GNCC stations . Data acquisition and preliminary processing 

pro cedures remained as described in previous GtlCC Summary Reports (Peterson, 

1978, pp . 2D - 25 ; Nendonca, 1979, pp. 16-23) . The entire record of co ntinuous 

CO 2 measurements at each station has been recently corrected, conve rted to the 

X8 1 mole fraction scale, a nd edite d . The s e l e ction of these finalized sets 

for ba c kground conditions is now unde r way and should be compl eted by the end 

of 1983, in time for archival "ith \.Jl'1O and with the DOE Carbon Dioxide Information Center in Oak Ridge, Tenn . Provisional monthly mean values of background CD 2 con centration at the four observatories are presented in table 6, 

and plotted in fig . 6 . In this form, the val ues report ed are mu ch closer to 

fi nal than those given in previous GNCC Summa ry Reports, but must still be 

considered provisional. The ma jor episodes of line contamination and instrument malfunction have be e n excluded from the se records, and the previous problem of drifting CO 2 calibration standards (- D. l ppm yr 1) with respect to the 

Wl'10 sta ndards ma intained by C. Ke e ling at SIO ha s nOl' been resolved. 

Table 6.--Provisional sele c ted mont hly mea n CO 2 concentrations 

(ppm r e lative to dry air--X81 mole fra c tion scale) for continuous 

measurements at BRW , tlLO, StlD , and SPD 

Year J, " F,b Mar Ap' M,y J"" J"I Aug S,p D<l Nov Dec 

BRW 

1973 322 . 1 325 . 1 329. 4 333 .0 333.8 

1974 (336 . 2)* (337 .2F 336 . 7 337 . 2 336.9 335.9 330. I 324 . 7 325.8 329.1 332.2 335.3 

1975 336. 9 337.0 33 7. 2 337.8 338.3 335.3 328.6 324 . ] 325.2 329." 33t..8 336. 5 

1976 337 . 3 331.3 337.8 338 .1 337.8 336.8 330.1 324.0 325.6 330.3 33t..2 336.7 

1917 )36 . 9 336.9 338.3 339 . 2 )39.4 )37. 9 330. I 326 . 6 328.2 332.3 335.0 338.8 

1978 339 . 3 340.3 )41.6 341. 0 340.8 339.4 332 .0 )28.2 328. 7 )]2.9 338.9 339.5 

1979 340 . 2 341 . 4 342.5 342 . 4 342.9 342 . 0 333 . 2 328.5 330.t. 333.2 338.t. 3t.1.6 

1980 3t.2 . 0 342 . 5 343 . 4 3t.3 .3 3t. 3.3 3t.2.7 336.7 331 . 9 33 1.6 338.5 3t.0.7 3t.2.9 

1981 344. 4 345 . 6 344 . 6 345 . 8 346.9 344.1 336.8 331 . 8 333.7 339.0 342 .4 344.8 

1982 345 . 8 347.5 348 . 2 348 .4 348.0 345 . 8 339. I 332.8 334.2 338.5 342 . I 34t. .7 

MLD 

1974 333.0 332.1 331.0 329.1 327. t. 327.3 328. 3 329 . 5 

1975 330.7 33 1.5 332 . 1 333.3 333.8 333.9 331.8 330.0 328.5 328.3 329.3 330.5 

1976 33 1. 7 332 . 8 333.5 33t..9 33t..8 334.5 333.0 330.7 329.3 320.7 330.2 331. 4 

1977 332.0 332.3 33t. . 9 336.2 336.9 336 . 1 335.0 332 . 6 33 1.3 33\.3 332.3 333.6 

1978 335 .1 335 .4 336 . 8 337 . 8 338.1 338 . 0 336.5 334.5 332.t. 332. t. 333.8 33t..9 

197 9 336. 3 336. 8 338 . 3 338.9 339.3 339.1 337 . 6 335 . 5 333.8 33t..2 335 . 3 336 . 8 

1980 337 . 8 338. 4 340 . 0 340 . 9 341. 4 3t. l .3 339.5 337 . 3 336 . 0 336.1 337.3 338 . 4 

198 1 339 . 2 340.0 341 . 7 342. t. 343 . 1 342. ') 340.7 338.5 337. I 337.3 338.7 339.9 

1982 34 1. 2 341 .7 3t.2 . 7 343.8 34t..3 343.3 341.8 340 . 2 337.7 337.9 339 .1 340. 7 

5"D 

1 976 (330 . 7)t (330.6)t 33 1.3 331.2 330.6 331. 3 33\.1 331.1 33 1.3 331 . ') 33 1. 9 33 1.8 

19 77 331 . 7 332.0 332 . 2 332.2 332.8 333.7 333.2 333.1 332.8 (]32.9)t (333 .4 )t ( 333.7)t 

1978 

19 79 (334 .6)t (335 . 3)t (336. 0)t 335 . 6 335.9 336.0 336.4 336 . 3 336.3 336 . 6 336.6 336 . 9 

1980 337 . 5 33 7 .6 337.9 337 . 3 337 . 7 338 . 0 338.3 338. 3 338.2 338. 1 338.5 339.3 

198 1 339 . 0 339.3 338.8 339.6 338 . 9 339 .1 339.0 339 . 2 339 . 2 338.9 339 .5 339.8 

1982 340. 4 340.4 340 . 4 341.2 339 . 9 340.0 340.5 340 . t. 340.1 340.0 340 . 2 340.3 

SPO 

1975 328 . 2 328.3 328.5 328.3 328. 1 328.6 329.4 330 . 2 330.8 331.0 330 . 6 330.3 

1976 330 .1 329.8 329. 6 329.6 329.7 329 . 9 330.3 330 . 7 331.0 33 1.1 331 . \ 33 1.1 

1977 330.9 330.3 330 . 3 330.6 331 . 0 331 .4 331.8 332 . 2 332.7 333.0 333 . 0 332.7 

1978 33 2.6 332 . 4 332. 3 332 . 5 333 . 0 333 . 3 333.8 334.4 334. 9 335 . 0 33 4.9 034.6)t 

19 79 

1980 336.1 336.0 336 . 0 336 .2 336.6 336.9 337. t. 337.7 337.9 338 . 1 338 . 0 338.0 

198\ 337. 8 337.8 337.9 337.9 338. 1 338.3 338.7 339 . 0 339.2 339 . 1 338.9 338.2 

1982 338 . 5 (338.6)t 338.4 338.6 338.9 338.9 339.2 339 . 6 339.9 339.8 339.5 339.2 

," Less re l i ab l e dat a . 

tSubst itut ed flask data . 

24 
- .. 0 

" 

. " 

:., 

Figure 6 ,--Provisional selected 

monthly mean C02 concentrations from 

continuous measurements at BRW, MLO, 

SMO, and SPO . Values are in ppm 

with respect to dry air (X81 mole 

fraction scale) . 

Detailed r eports on the continuous C02 record at each s t ation are forthcoming, but some preliminary interpretations are already possible. Each of 

the four stations shows a CO 2 increase of nearly 9.0 ppm for 1976-1982, yielding a mean global growth rate for atmospheric CO 2 of 1 . 50 ± 0 . 02 ppm yr- 1 . 

From the data of Rotty (1983), the total industrial CO 2 production from fossil 

fuel combustion and cement manufacture for t his same interval may be estimated 

as -35 . 8 Gt of carbon or 16.8 ppm atmospheric CO 2 equivalent. The implied 

global average airborne fraction ~ ~ 0.54 for this period is virtually identical to the average (~ = 0.53) of the airborne fractions from the CO 2 observa -

tions by C. Keeling at MLO (~ = 0.55) and SPO (~ = 0.51) during the period 

1959-1978 (Bacastow and Keeling, 1981), Although there is some indication 

that the latitude dependence of the airborne fraction has weakened i n the last 

decade of slower fossil fuel CO 2 release, a mean value of ~ ~ 0.54 ± 0.02 

still seems appropriate for model projections of future atmospheric increases. 

A second conclusion based upon the data of table 6 is that the latitude 

gradient of CO 2 concentration from BRW to SPO has remained near 3 . 5 ppm during 

the last decade. Interannual variations of ±0 .5 ppm are probably related to 

the ENSO events of 1976, 1979, and 1982 (Bacastow et al., 1980). The magnitude of this gradient is directly related to the rate of release of fossil 

fuel C02 to the atmosphere at northern midlatitudes. That this gradient, 

which increased rapidly from - 1 ppm in 1960 to -3 ppm in the mid-1 970's 

(Keeling, 1983) is now nearly steady, is a direct consequence of the dramatic 

slowing in the rate of global production and consumption of fossil fue ls since 

the OPEC PEice increases of 1973. Fossil fuel growth rates have been less 

than 2% yr 1 since 1974, with zero or negative growth rates in 1980 -19 82, as 

compared with the mean growth rate of 4.6% yr- 1 in 1950-1973 (Rotty, 1983). 

A final comment on the continuous data concerns the stability of the CO 2 

seasonal amplitude over the last decade. Several recent studies of the SIO 

long time series CO 2 records from MLO, BRW, and SPO, as well as the shorter 

series from Station P, all suggest that the seasonal amplitude at the north ern 

midlatitude stations ha s increased by 0.6%-0.8% yr- 1 during the l ast two decades,_with a less certain indication of an even more rapid increase of ~2%-

3% yr 1 at SPO (Bacastow et al . , 1983; Cleveland et al . , 1983; Keeling, 1983; 

Pearman and Hyson, 1980, 1981) . Future studies of this type will more carefully define the cha nging seasonal amplitude in the GMCC flask and continuous 

data. See sec . 5 . 14 for a first, careful look at the MLO continuous record. 

However, even the simplest approach (i.e., examining the val ues in table 6 for 

the annual CO 2 growth rate on a month-by-month basis) suggests that the sea -

sonal amplitudes at both MLO and BRW have been increasing rapidly ( 1. 5%-

2% yr- 1 ) since 1975 . These results are consistent with previous studies of 

25 
the SIO data, which found lhat mos t o f the i nc reas e in seasonal amplitude ha s 

occurred since the mid-1 970 's. 

The same method applied to the GMCC flask and co ntinuous CO 2 records at 

SPO does not s how a pronounced increase in seasonal amplitude with time, but 

in fact suggests the reve rse. The gradual growth in Northern Hemisphere seasonality is most logically explained as a biospheric respons e to the enhanced 

atmospheric CO 2 levels, al though the rapid rate of increase is difficult to 

interpret in terms of known plant physiology . A second contribution is ex -

pected from increased heterotrophi c respiration, or rotting of soil organic 

matter under warm, wet weather conditions , probably more important at BRW than 

at MLO. Possible changes in the seasonality of the anthropogenic CO 2 release 

are probably not responsible for th e observed increase, but deserve furthe r 

study . 

3 .1.2 Flask Samp l e CO 2 Measurements 

The number of cooperating sites from which air samples were returned to 

G~ICC for CO 2 analysis in 1982 remained nearly unchanged from the 20 sites 

reporting in 1981. A complete list of flask stations in operation by the end 

of 1982 is given in table 7, and their locations around the globe are shown in 

fig. 7. De tailed station information for most of these locations has been 

reported in the GNCC Summary Reports for 1979 and 1980 (Herbert, 1980; DeLuisi , 

198 1) . A compl e t e description of the G~ICC fla s k network will appear in a 

forthcoming Imo special report. 

Table 7. --GNCC CO 2 flask network as of December 1982 

Code Station Latitude Longitude Elevatio n 

(deg) (deg) (m) 

MIS Ams te rdam I . 37 . 95S 77.53E 150 

ASC Asc ension I. 7.92S 14.42W 54 

AVI St. Croix, V.1. 17 . 75N 64 .7SW 3 

AZR Terceira I., Azores 38.75N 27 .08W 30 

BRW Barrow, Alaska 71 . 32N 156 . 60W 11 

CBA Cold Bay, Alaska 55.20N 162.72N 25 

CMO Cape Neares, Oreg. 45.00N 124.00N 30 

COS Cosmos, Peru 12.1 2S 75.33W 4600 

FLK Falkland Is. 51.75S 57.83W 5 1 

Gm Guam, Hariana Is. 13.43N 144.78E 2 

HBA Halley Bay, Ant. 75 . 00S 27.00W 0 

KEY Key Biscayne, Fla. 25.67N 80. 17W 3 

KPA Kitt Peak, Ariz. 32 .00N 11 2 .00W 2095 

KUN Cape Kumukahi, Hawaii 19 .52N 154.82W 3 

~lBC Nould Bay, Canada 76 . 23N 119.3311 15 

MLO Mauna Loa, Hawaii 19.53N 155.58W 3397 

NWR Niwot Ridge, Colo. 40.05N 105.63W 3749 

NZL New Zeala nd 43.83S 172.63E 3 

PSA Palmer Station, Ant . 64.92S 64.00W 10 

SEY Mahe' I., Seychelles 5 . 33S 55.17E 3 

S~IO Cape Matatula, Am. Samoa 14.25S 170.57W 30 

SPO South Pole, Ant. 89.98S 24.80W 2810 

SUI Station M 66.00N 2.00E 0 

26 
~. ~ 

" ., ... . .;, ~'.;~'''' ~- . . 

. - " , 

it .. :, • ...: ... 

.... "' . . 

".. 

[: '" 

"., 

.. 

., [ .. ,.. , 

Figure 7.--Locations of the cooperating flask sampling sites of the 

GHCC global CO 2 network. 

The hostilities between the British and Argentinians in the Falkland 

Islands (Code: FLK) terminated the C02 record there in February 1982 after 

barely 1 year of measurements , and all sampling equipment was lost or destroyed during the war. The reopening of this station is still und e r discussion, although the resupply logistics are now considerably more difficult and 

ci rcuitous. To fill the gap in latitude coverage created by the loss of FLK 

(51.75°S, 57.83°W), a cooperative sampling program was initiated with L. Heidt 

of NCAR at the project GHOST station near Christchur ch, New Zealand . The C02 

record at this site (designated NZL, located on Kiatorete Spit, 43.83°S, 

172.63°E) begins December 1982 . A second new station was established in 1982 

in cooperation with the British Antarctic Survey at their site at Hall ey Bay, 

Antarctica (75°S, 27°W). The first year of flask samples (December 1982-

December 1983) will arrive in Boulder for C02 analysis in April 1984 . 

Finally, to fill the gap between HLO (19.53°N) and Cold Bay, Alaska 

(55.20 0 N), a cooperative arrangement was reached with OGC to have C02 sampl es 

collected at their clean-air si t e at Cape Heares (45°N, 124°W) on the Oregon 

coas t. 

The CO 2 sampling site at Point Six Hountain, Hont . , was discontinued in 

1982, and replaced by a new sampling program at Kitt Peak National Observatory 

(32°N, 11 2°'.), near Tucson, Ariz. The Kitt Peak program, in cooperation with 

Battelle Laboratories, will relate the GHCC co ntinuous C02 meas urements at 

ground l evel to the total- co lumn CO 2 values obta ined simultaneously by the 

Battelle-Kitt Peak group using high-resolution Fourier transform spectroscopy 

on the HcHat h solar telescope. 

In 1982, 3167 0.5-2 flasks and 322 5-2 flasks were received and analyzed 

using the semiautomati c C02 analysis system described by Komhyr e t al. (1983). 

The only major cha nge s in the analytical procedure for CO 2 flask analysis made 

in 1982 were the cleaning of the flask pump-down vacuum rack and the co nversion from dry ice to liquid N2 in the cold trap of the vacuum line . Tank 

ca libration and flask analysis are now under the control of an HP-85 computer 

and an HP-6940B multiprogramme r. The conversion from silicone to Apiezon 

grease i n the flask stopcocks and the special cleaning of all silicone residue 

from the full flask inventory was completed in 1982. 

The provisionally edited flask data for 19 79 -1981 were reported in the 

G~ICC Summary Report for 1981 (Bod haine and Harris, 1982, pp. 21-29). Since 

that time the entire flask data set since 1968 has been corrected, converted 

27 
to the WHO X81 mole fraction scale, and edited for background conditions. 

Details of this process, the final flask data set, and data analysis results 

are presented by Komhyr et al . (1984) . The annual means are reported here in 

table 8. The background CO 2 values from the flask program have been archived 

with the DOE Carbon Dioxide Information Center in Oak Ridge, Tenn., with WHO, 

and with WOC-A. 

The 10,000 C02 flask measurements of the 20-site network from 1979-1982 

have been used to create the zonally averaged global C02 distribution and its 

variation in space and time (fig. 8). This surface is smoother than the 1981 

surface presented in last year's GMCC Summary Report (Bodhaine and Harris, 

1982, p. 28) because of more careful editing of the data for background conditions and a revised procedure of first fitting spline functions to the time 

series at each station and then using the smoother spline values in synthesizing the interpolated global concentration surface. Note the great repeatability in regular breathing of the global biosphere, dominated by the land plants 

of the Northern Hemisphere. 

The finer details of the interannual variations in the CO 2 seasonality 

and increase are better seen in a flat, two-dimensional projection of this 

concentration surface onto the time-latitude plane (fig. 9). These concentration contours represent the zonally averaged, mean CO 2 concentration at sea 

leve l with a resolution of 20 days and 10° latitude, so that particular features on smaller time and space scales (e.g., equatorial upwelling or the 

steep gradient at the ITCZ) will not be well represented. In generating the 

surface, only those sites of the network in remote marine locations (fig . 7) 

have been used, so that the inferred seasonal amplitudes are certainly minimum 

values that underestimate the much larger CO 2 seasonality expected for midcontinental locations. 

An important result of the flask network is the fine definition of the 

latitude dependence of the atmospheric C02 concentration on an annual basis 

since 1979 (fig . 10). The equatorial local maximum is mai ntained primarily by 

the upwelling and outgassing to the atmosphere of CO 2-supersaturated deep 

water in equatorial oceanic regions. The mean BRW to SPO difference of 

-3 .5 ppm is a result of fossil fuel combustion in the Northern Hemisphere. 

The nearly complete failure of the normal upwelling during the trade wind 

anomalies of the extreme ENSO event of 1982-1983 produced a marked reduction 

in this equatorial feature in the 1982 latitude gradient, as shown in fig. 10 

and discussed by Gammon and Komhyr (1983). The perturbation of the global 

carbon cycle by t he 1982-1983 ENSO was sufficient t o halt the atmospheric 

increase due to fossil fuel combustion for severa l months in the fall of 1982, 

which implies short-term changes in the natural CO 2 sources and sinks of 1 Gt 

(10 15 g) of carbon or more. 

A comparison of the flask and continuous CO 2 annual means for BRW, MLO, 

SMO, and SPO is presented in fig . 10. The mean difference between the flask 

and continuous values at each station over the period 1979-1982 is typically 

0.1 ppm (0.2 ppm for the mean of the absolute values of the differences). 

A second check on the reliability of the flask CO2 measurements is the 

ongoing program of flask comparisons with Keeling's laboratory at SIO, described in the G~ CC Summary Report for 1981 (Bodhaine and Harris, 1982, p . 27) . 

28 
Table 8.--Annual mea n CO2 

X81 mole fra ction s cale ) 

S t a . 1968 1969 1970 

MIS 

ASC 

AVI 

AZR 

BRI.' 

C8,\ 

eND 

FlK 

GNI 

KEY 

KU~I 

NBC 

NKO 

~I LO 322 . st 325.2 

1o'\,'R 323 . I 324 . 1 325 . 6 

PSA 

SEY 

S~IO 

SPO 

STC 324.0 326.4 

S'nl 

-:'-Numbec o f intecpo),lled points 

tlncomplete yeac. 

N 

a 

u 

" a. 

a. 

1971 1912 

327.4 330.2 

]25.2 326 . 3 

326.9 327.6 

~ 1/2 of total 

81 

~ 

atmosphe ric concentra tions (ppm CO 2 in air--

fo r the cooperating site s of the flask network 

1973 1974 1975 1976 1977 1978 1979 1980 1981 1982 

335 . 9"'- 337.8 339 . 3 339 . " 337.3t 338 .8 339 . 7 340.7 

337 . 1 339.6 340 . 4 340.9 

338 . 4 339.6 341.2 332 . 0 33].4 333 .0 333.9 335.0 336.6 337.7 340.2 341.5 342 . 7 

337.8 339.8 34 1 .3 341.9 

341.2 

339.7 

337 . 7 340.0 341.2 341. 0 330.7 333 .4t 332 . 7 335.2 336 .7 338 . 8 340.2" 3,+ 2.0 341.6 

332.3 334 . 4 335.7 337 . 4 339.3 340.4 341. 1 

340.3 341 . 9 342.5 

]37 . 3 

332. I 333.6 335 .2 336.7 338.9 340 . 4 341 . 0 

330.2 334 . at J32.1 334 .8 ]35.7 337.0 338 . 1 339 . 9 340 . 9 

333.9 335.2 337 S" 340 . 0 339.8 

339.3 340 . 1 340.5 

330.2t 330 .8 330 .7 331.5 332 .8 334.3 336.0 338. I 339.3 340.4 

329 . 4 330.2 331.5 333 . 7 335 .5 336.7 338 .5 339.3 

341.9 34 1.7 

numbec of points. 

8, 

Figure 8.--A three-dimensional perspective of the "pulse-of-the-planet," the 

variation of the global atmospheric CO 2 concentration in latitude and time 

based on flask measurements for 1979-1982. This zonally averaged surface has 

a resolution of 20 days and 10° in latitude and was synthesized from results 

of - 10,000 individual flask samples returned from the 15 remote sea-level 

sites shown in fig. 7. On 31 December 1982 the CO 2 concentration is 

339.5 ppm. 

29 
.'. 

.'. 

.'. 

. ', 

.', 

.'. 

"'. 

__ 3 10 3 10 __ 

1979 

CJI O---HO 

". ----- _____ --)10 .110 

------- = 

1980 

_}~ --- I~O __ _ __ _ 

JID -

", J...,,:--:::.~::- ,::-,,::,-,',,=,"-'C,, "'.,,--::-: ,, :-,,:---:7":::'-:;"r::--::<>n"::-"":-::-,--:::or:-'-:-:-:"--:':-:H:.-:':-":::' :-; ,,:::,:-:-::-'--::-:-'--:H"'. :-: ,,:-',,=,,,.....,=-"",c":- ",,,,, , 

1981 19112 

Figure 9.--A two-dimensional contour diagram, the projection of fig. 8 onto 

the latitude-time plane. The concentrations are zonally averaged, and 

strongly weighted toward remote, marine locations. The surface trends upward 

by 1.3-1. 5 ppm yr- 1 at all latitudes because of fossil fuel CO 2 emissions 

(-5 Gt of carbon yr- 1 ). 

Figure 11 shows the GMCC-SIO flask CO 2 concentration differences since the 

comparison began in mid-1981. With the exception of SMO, the scatter ha s been 

decreasing and the agreement improving, so that as of December 1982, the two 

programs have converged to the limiting error of sampling and analysis 

(-±0.1-0.2 ppm). 

Although the detailed description of the flask data and initial interpretations will appear in a future report, some of the longer time series of 

flask measurements finalized in 1982 are presented here. Figure 12 shows the 

selected flask data and fitted spline curves for BRW (1971-1982), NWR (1968-

1982), KEY (1973-1982), Killl (1976-1982), NLO (1975-1982), S~IO (1973-1982), and 

SPO (1974-1982). 

In 1982, mlcc began CO 2 samp ling on ships of opportunity, to assess the 

representativeness of our flask network and interpolated global distribution, 

and to observe finer features of the global distribution (e.g., ITCZ, equatorial upwelling, and longitudinal gradients). See sec. 4.12 for a report on the 

R/V DISCOVERER 1982 expedition in the North Pacific . 

30 
W 

..J 

a: 

u 

U1 

Z 

o 

H 

.... 

U 

a: 

'" "-

W 

..J 

o 

:E 

ID 

X 

:E 

"-"-

ru 

o 

u 

C02 LATITUDINAL GRADIENT 

'" 

'" 

341 

". 

'" _ :t/'f 34 1 ...... -t ' 

". , t I' l-----(' lSB I / i-_ 339 I i ... - ___ i' 

". 

". ""l ,_----t t Vi" * *, / '" I O'--_t' 19B0 

338 _-*----..... ," - '" 

". ""I -----* lA- V 'lil. " 337 " ,-. __ -f 1979 

'" .t_-----1 335 -,----

• 

SIN(LAT) 

-I 

19B1 19B2 1983 

"'" 

1981 !982 19B3 

;; 

Figure 10,--Latitude gradients of 

annual mean atmospheric CO2 concentrations at the flask network sites 

for 1979-1982 (*), The corresponding annual mean values from the 

continuous CO 2 mea surements at the 

four baseline stations are also 

shown for comparison (0), 

-, 

-3 , , ~ • " , , " • 0 " • , , ~ ... , J .. I 0 • D J , ~ . .. , , " I 0 • D 

19BI !982 1983 

w , :i: -: I ° ° 010. oo8 ,Ro0 Q,.<ool:tl 

~ ~ er----,..-",~iO,~ _",,"--,'0"", 8:':<,",~""'fI'~~ 5R: -I 0 v ° ° 0,', ~ --, ;; 

198 ! 1983 

Figure ll,--The differences between the measured atmospheric CO 2 concentrations in nearly simultaneous flask samples, as measured by GMCC (0,5 ~) and 

SIO (5.0 ~) since mid-1981 for BRW, MLO, KUM, and SMO, 

31 
2 j2~ 

Q 

Q 

z 

o 

BRW 71N 157\"_' _ -J 

I--- j 4 5 

U 

<! 

0:: j j 5 

o lj j 25 

o 

2 \~+-__ -. ____ .-__ -. ____ .-__ -r ____ .-__ -r ____ .-__ -, ____ .-__ -, __ -" ~,~"_, 'O~6~_ 

N 

8 "'j 

"'1 '" 

", 

~~~~ "

, '~ ~. J 

1968 1969 19 70 19 71 19 72 19 73 1974 1975 1976 1977 1978 19 79 1980 ·98· 1987 

--r ------,----------,-

~ 

jJoL' KUM 20N 155W 

J' ====~======~======~======~====~====== ======~====~~==== ======~ 

Q j!> O ~ . • 

Z j 4 0 • • 

o o ~ U jji) 

<! MlO 20N 156W '" 

W ~ J2 ~====== ==== ======~======~====~~==== ====== ======~==== ======~ --' J>O 

o 

Ou

2N 

:.:O:l~==:::==~~==:::==:::==~;::===:::= =:;: ,..o=:::;::: =:::.;::"' "'J~ _ : 0 ill; p~o" ... 

... ': \\l'~:'~T: ~ =. -r, 14 S 17 1V1 

~ , ~ 

:i J J2 ~------.-------.------.-------'------.------''------.~~-- ~~~r---

'~: .. , 

::o .w~ ~ ?9n 

:" -

"..,2Q 

-- 0 25W 

19 73 ·974 1975 1976 1977 19 78 1979 1980 198 1 1982 

Figure 12.--Final flask data for BRW (1971-1982), NWR (1968 - 1982), KEY (1973-

1982), Killl (1976-1982), MLO (1975- 1982), lO (1973-1982), and SPO (1974-1982). 

These records have been corrected, converted to X81 mole fraction scale, and 

edited for background conditions. The solid curve represents a spline fit to 

the background data O. Valid atmospheric samples not representing background 

conditions are denot ed +. Data synthesized to constrain the spline are denoted b,. 

32 
With proper latitude weighting, the estimated global annual C02 flask 

concentrations from the 20 cooperating sites are 337.2, 338.9, 340.2, and 

341.0 ppm for 1979, 1980, 1981, and 1982 respectively. These global means may 

be compared with the MLO annual means from the GMCC continuous CO 2 program 

because MLO has often been considered to be globally representative. Tables 6 

and 8 show that, in general, ~~O data lie 0.2-0.4 ppm below the global annual 

mean derived from the flask program. 

3.2 Total Ozone 

3.2.1 Observations 

Total ozone observations with Dobson spectrophotometers continued during 

1982 at 11 stations that constitute the U.S. total-ozone network (table 9). 

On 29 January 1982 the U.S. Army terminated operation of the Dobson station at 

White Sands, N. Mex., and Dobson spectrophotometer no. 86, which was operated 

there, was transferred to G~!CC. Plans are to relocate the instrument in the 

south central part of the United States. On 8 October 1982, Dobson measurements were terminated at BRW. The BRW instrument was returned to Boulder to 

be modified, recalibrated, and automated for Umkehr and total ozone observations planned for Poker Flat, Alaska (see sec. 4.3). In November 1982 Dobson 

spectrophotometer no. 94 was used to establish a west coast station at Fresno, 

Calif., but because of a shortage of personnel at the station, no observations 

were made during 1982. 

Table 9.--U.S. Dobson ozone spectrophotometer station network for 1982 

Station Period of record Instrument no ... ', Agency 

Wallops I., Va. 1 Jul 1967-present 38 NOAA-NASA 

SMO 19 Dec 1975-present 42 NOAA 

Tallahassee, Fla. 2 Jun 1973-present 58 NOAA 

Boulder, Colo. 1 Sep 1966-present 61 NOAA 

MLO 2 Jan 1964-present 63, 65t NOAA 

BRW 2 Aug 1973-8 Oct 1982 76 NOAA 

Nashville, Tenn. 1 Jan 1963-present 79 NOAA 

SPO 5 Dec 1963-present 80 NOAA-Army 

Huancayo, Peru 14 Feb 1964-present 87 NOAA-Huancayo 

Obs. 

1'Instrument used throughout 1982. 

tNo. 63, Jan-May 1982; no. 65, Jun-Dec 1982. 

3.2.2 Modernization and Calibration of Dobson Spectrophotometers 

In 1982 GMCC continued the program that began in 1977 to upgrade foreign 

Dobson spectrophotometers under the auspices of the WHO Global Ozone Research 

and Monitoring Project. In May, Manila Dobson instrument no. 52 was shipped 

33 
to Boulder, Colo., for repair and recalibration. An initial calibration indicated that the instrument was -8.9% out of calibration . Major repairs were 

then made, including installation of an "air-space" optical wedge, and the 

instrument was optically aligned. Following calibration by direct comparison 

with World Standard Dobson Instrument no. 83, instrument no. 52 was returned 

to the Philippines. 

3.2.3 Calibration Check of Dobson Spectrophotometers in the Global Network 

During the international intercomparison of Dobson ozone spectrophotometers held in Boulder, Colo., in 1977, a technique was devised to check the 

calibration level of Dobson instruments by means of special, calibrated lamps. 

Two lamps, UQl and UQ2, were calibrated using World Standard Dobson Instrument 

no. 83 . The calibration level of the World Standard was then transferred by 

means of lamp UQl to 14 instruments that had been calibrated previously by 

direct intercomparison with the \yorld Standard. Results of this work indicated that Dobson instruments, whose optics are properly aligned and have 

accurate wavelength-setting and optical-wedge calibrations, can be calibrated 

on an absolute scale with calibrated lamps Lo within about ±1% (Komhyr et al., 

1981). Conversely, such calibrated lamps can be used inexpensively to identify Dobson instruments requiring recalibration. Since the state of relative 

calibrations (.'avelength setting and optical wedge) of such instruments is 

unknown, the results of the lamp tests should not be used to correct the calibration levels of these instruments. In August 1981 the world Dobson instrument network was divided into seven regions, and a special calibration lamp 

unit was built for each region. After calibration with Standard Instrument 

no . 83, the lamp units were sent to each region where calibration checks were 

made on instruments within the region. 

Resul ts of the calibration checks shown in table 10 indicate that a number of instruments in the global total ozone network require recalibration . 

The data have been provided to \YI'IO as well as to the various institutions 

operating the instruments . The GMCC World Dobson Spectrophotometer Central 

Laboratory will continue to work with the Wl'IO Global Ozone Research and ~lonitoring Project to upgrade the calibrations of these instruments. 

3.2 . 4 Monthly Means 

Daily 1982 total ozone amounts (applicable to local apparent noon at each 

station) for all stations in the U. S. network have been submitted for publication on behalf of WHO and are available in Ozone Data for the World, published 

by the World Ozone Data Center, Atmospheric Environment Service, 4905 Dufferin 

Street, Downsview, Ontario M3H5T4 . Table 11 lists provisional monthly mean 

amounts of total ozone for 1982, for the GNCC observatories and cooperative 

stations. 

34 
Table 10 . --Pcovisional calibcation level of Dobson instcuments 

within the wocld Dobson netwock 

Station 

Region I--North America 

Toronto, Canada 

Resolute, Ca nada 

Churchill, Canada 

Goose Bay, Canada 

Edmonton, Canada 

Reykjavik, Iceland 

SPO 

Bis marck, N. Dak. 

Caribou, ~Iaine 

Wallops I., Va. 

Tallahassee, Fla. 

Nashville, Tenn. 

NLO 

StlO 

BRW 

Boulder, Colo. 

Boulder, Colo. 

Region 2--South America 

Mexico City, Mexico 

Huancayo, Peru 

Cachoeira Paulista, 

Brazil 

Natal, Brazil 

Buenos Aires , 

Argentina 

Buenos Aires, 

Argentina 

Region 3--Western Europe 

Bracknell, U.K. 

Bracknell, U.K. 

Halley Bay, U.K. 

Argentine Is., U.K. 

Seychelles, U.K. 

St. Helena I., U.K. 

King Edwa rd VII 

Point, U.K. 

Lerwic k, U.K. 

Arosa, Switzerland 

Arosa, Switzerland 

Hohenpeissenberg, 

F.R .G. 

Cologne, F.R.G. 

Oslo, Norway 

Oslo, Norway 

Troms¢, Norway 

Region 4--Western Europe 

Aarhus , Denmark 

Uccle , Belgium 

Biscarrosse, France 

Hagney-Les-Hameaux 

Dobson 

77 

59 

60 

62 

102 

50 

80 

33 

34 

38 

58 

79 

63 

42 

76 

61 

82 

98 

87 

114 

93 

97 

99 

41 

2 

32 

15 

101 

104 

56 

8 

14 

92 

40 

11 

85 

Per cent correc tion 

Lamp Lamp Lamp 

R11 

+0.00 

+0.59 

- 1 .76 

-0 . 1 

-0 . 44 

-0.44 

- I. 61 

- I. 47 

+1. 03 

+0 . 88 

-0.88 

-1.32 

+1. 03 

-0.73 

- I. 91 

+0.29 

-0.15 

R21 

-1.32 

-4.69 

+1.81 

+0.73 

+0.15 

+0.29 

R31 

+0.15 

+0.59 

-2.20 

+1. 03 

+0.15 

+6.90 

-0.29 

+0.88 

+1. 17 

R4 1 

-0.59 

- I. 17 

+2.49 

- 1 .91 

35 

R12 

+0.29 

+0.88 

- I. 47 

+0.15 

+0.29 

-0.15 

-I. 03 

+1. 47 

+1. 47 

-1. 32 

+0.44 

R22 

-1.32 

-4.99 

+3 .52 

+0.73 

+0.00 

-0.15 

R32 

+0.15 

+0.59 

-2.05 

+0.73 

+0.00 

+6.17 

-0.15 

+0.73 

+1. 17 

R42 

-0 . 88 

- I. 32 

+2.35 

- 2 .05 

RI3 

-0.29 

+1.03 

- 0.88 

-1.03 

-0.88 

0.44 

Nea n 

percent 

correc tion 

+0.15 

+0.74 

-1. 62 

:to.oo 

-0.08 

-0.30 

- I. 32 

-0.88 

+1. 25 

+0.96 

-0.88 

- I. 18 

+1. 25 

-0.81 

- I. 62 

+0.37 

-0. 30 

-\.32 

-4.84 

+3.67 

+0 . 73 

+0.08 

+0 . 07 

+0.15 

+0.59 

-2.13 

+0.88 

+0.08 

+6.54 

-0.22 

+0.81 

+1. 17 

- 0.74 

-1.25 

+2.42 

- I. 98 
Table lO.--Provisional calibration level of Dobson instruments 

within the world Dobson network--Continued 

Station Dobson 

Region 4--Western Europe (Cont.) 

Lisbon, Portugal 13 

El Arenosillo, Spain 120 

Vigna Di Valle, Italy 47 

Brindisi, Italy 46 

Sestola, Italy 48 

Cagliari/Elmas, Italy 113 

Casablanca, tloracco 

Cairo, Egypt 

Region 5--Eastern Europe, 

Leningrad, U.S.S.R. 

Belsk Duzy, Poland 

Hradec Kralove, 

Czechoslovakia 

Budapest-Larine, 

Hungary 

Bucharest, Romania 

Potsdam, G.D.R. 

Potsdam, G.D.R. 

Region 6--India 

New Delhi, India 

New Delhi, India 

Srinagar, India 

Varanasi, I ndia 

Ht. Abu, India 

Poona, India 

Kodaikanal, India 

Quetta , Pakistan 

Quetta, Pakistan 

Bangkok, Thailand 

Singapore (U.K.) 

U.S.S.R. 

108 

84 

74 

110 

121 

71 

64 

36 

112 

10 

55 

54 

39 

45 

43 

100 

90 

7 

Region 7--Australia and Japan 

Sapporo, Japan 

Sapporo, Japan 

Kagos hima, Japan 

Naha/Kagamizu, Japan 

Tateno, Japan 

Tateno, Japan 

Tateno, Japan 

Srinagar, China 

K'un-ming, China 

Aspendale, Australia 

Aspendale, Australia 

Perth, Australia 

Cairns, Australia 

Brisbane, Australia 

Hobart, Australia 

Macquarie I., Australia 

Invercargill, New 

Zealand 

5702 

5706 

5704 

5705 

116 

122 

5703 

75 

3 

105 

115 

111 

81 

6 

12 

78 

17 

Percent correction 

Lamp Lamp Lamp 

R41 

+0 . 29 

-0.44 

-0.44 

-3.23 

+0.15 

+ 1.32 

R51 

-0.29 

-1. 32 

+3.23 

+3.52 

-3.37 

-0 . 59 

+0.44 

R61 

-0.59 

+1. 61 

-1. 61 

+1.76 

-2.05 

-0.29 

-2.64 

-10.71 

R7I 

+0.29 

-1.76 

-4. 40 

+3.52 

-2.93 

-3.37 

+0.59 

to.OO 

+1.32 

-0.44 

-0.15 

+9.10 

-6.60 

+4.11 

+8.80 

+0.29 

-0.15 

36 

R42 

-0.15 

-0.88 

-0.44 

-3.37 

+0.00 

+1. 17 

R52 

-0.29 

-1 . 32 

+3.37 

+3.52 

-3.23 

-0.59 

+0.44 

R62 

-0.29 

+1.32 

-1. 91 

+1.47 

-2 . 49 

- 0.59 

-2.49 

-10.86 

R73 

+0.59 

-1.76 

-4.40 

+3.52 

-3.23 

+0.15 

-0.29 

+1. 61 

-0.73 

- 0.15 

R74 

+8.80 

+0.29 

-0.15 

tlean 

percent 

correction 

+0.07 

-0.66 

- 0.44 

-3 . 30 

+0.08 

+1. 25 

-0. 29 

-1. 32 

+3.30 

+3.52 

-3.30 

-0.59 

+0.44 

-0.44 

+ 1. 47 

-1.76 

+1. 62 

-2.27 

-0.44 

- 2.57 

-10.79 

+0.44 

-1.76 

-4 . 40 

+3.52 

-3.08 

-3.37 

+0.37 

-0.15 

+1. 47 

-0.59 

-0.15 

+8.95 

-6.60 

+4.1 1 

+8.80 

+0.29 

-0.1 5 
Table 11.--Provisional 1982 monthly mean total ozone amounts (milli-atm-cm) 

Sta tion Jan Feb Har Apr Hay Jun Jul Aug Sep Oct Nov 

Bisma rck, N. Dak . 375 399 392 405 377 362 340 310 296 291 312 

Ca ribou, Maine 399 420 420 427 386 376 359 376 334 323 326 

Wallops I., Va. 345 332 364 380 377 340 337 328 310 287 272 

SHO 257 258 259 257 253 251 25 1 252 259 258 265 

Tall aha ssee, Fla. 292 300 333 325 326 334 315 307 263 

Boulder, Co lo. 341 368 375 383 366 341 312 308 294 272 286 

HLO 256 252 285 29 0 288 28 1 272 267 256 247 238 

BRW 464 487 427 360 323 30 1 300 293 

Nashville, Tenn. 322 340 351 366 359 346 330 339 32 1 296 275 

SPO 304 284 239 264 

White Sands, N. Hex. 301 

Huancayo, Peru 265 269 271 263 265 263 269 273 272 271 262 

3.3 Ozone Vertical Distribution 

3.3. 1 Umkehr Observations 

Umkeh r observations continued in Boulder in 1982 with automated Dobson 

instrument no. 61 . Use of that instrument (see sec. 4.3) significantly increased the number of observations made compared wi th previous years . 

Dec 

329 

338 

283 

271 

268 

321 

236 

289 

336 

254 

After the eruption of the El Chi chon volcano in Mexico in April 1982, an 

intensive progra m of Umkehr observati ons was begun at MLO in Hay 1982. A 

classic set of data was obtained showing how vo l ca ni c stratosphe ric aerosols 

perturb ozone vertica l distributi ons de rived from Umkehr measurements . For 

co nventiona l Umkehr observati ons, the effec t is to diminish comp uted ozone 

amounts in the high stratosphere whi l e simultaneously accentuating tropospheric ozone val ues . This is illustrated in fig. 13a , which s hows a mean 

ozone profile derived from e i ght conventional Umkehr observations made in tlay 

1982 , about a month after the e ruption of El Chichon. Note t hat the deduced 

ozo ne amount in Umke hr layer 9 is negative. By December 1982, the stratospheric aerosol layer over MLO was conside r ably diminished, at which time 

conventional Umkehr observations yielde d more rea listic ozone amoun t s in the 

troposphere and stra tosphere (fig. 13b) . Short Umkehr meas urements (figs . 13c 

and 13d), on the other hand, appear to be less sensi tive to stratospheric 

aerosols. However , compared with vertical ozone distributi ons derived from 

ECC ozone soundings, t he a ltitude of maximum ozone concentration appears from 

the short Umkehr profiles to be about 4 km too low. 

3.3 . 2 ECC Ozone sonde Observa tions 

tlont hly ozone sonde flights were made in Bo ulde r throughout the year. All 

fl i ght s were made using type 4A ECC ozone sondes and 400-m3 thin-film plastic 

ba lloons . Balloon performance was excellent, with 39-km altitudes atta ined 

r egularl y . The sonde s appear to give reasonable ozone values to altitudes of 

-38-39 km. Above these altitudes the ozone signals falloff abruptly, ind icat i ng some instrument problem. All flights during 1982 were made wi th hypsometer type radiosondes that give greater confidence in measured altitudes than 

37 
2 

5 

10 

:0-

S 20 

w 

a: 

::0 

(j) 

ill 50 

a: 

"-

100 

200 

500 

STATION MAUNA LOA 

DATE 0582 TOTAL OZONE. 287 

UMKEHA. CONVENTIONAL (8) 

- 25 

-20 

-15 

- 10 

-5 

(a) 

l000 o ~ __ ~~50 100 ·2~~ ISO __ ~~~~ 200 250 ~ 300 

PARTIAL PRESSURE OF OZONE (nb) 

STAII ON:MAUNA LOA 

2 DATE: 05/82 TOTAL OZONE: 287 

UMKEHR: SHOAT (8) 

5 

10 

:0-

.s 20 

g'g 

W 

a: 

::0 

(j) 

(j) 

w 50 

a: 

"-

100 - 15 

200 

-10 

500 -5 

(e) 

1000 2 

0 50 100 150 200 250 300 

PARTIAL PRESSURE OF OZONE (nb) 

2 

5 

10 

:0-

S. 20 

w 

a: 

::0 

<J) 

ill 50 a: 

"-

100 

200 

500 

2 

5 

10 

:0-

.s 20 w 

a: 

::0 

(j) 

(j) 

w 50 

a: 

"-

100 

500 

1000 

0 

STATION:MAUN A LOA TOTAL OZON E FOR 

DATE: 12J82 ECC SONDES: 244 

ECC SONDE: (4) TOTAL OZONE FOR 

-40 UMKEHA: CQNV. (9) UM KEHAS: 238 

'0 

-15 

- 10 

-5 

(b) 

PARTIAL PRESSURE OF OZONE (nb) 

STATlON:MAUN A LOA TOTA L OZO NE FOR 

DATE: 12/82 ECC SONDES: 244 

ECC SONDE: (4) TOTAL OZO NE FOR 

UMKEHA: SHORT (11) UMKEHAS: 238 

0.1 ATM·e M 

'0 

20 j..I (JIg 

10 

-15 

-10 

-5 

(d) 

.2 

50 100 150 200 250 300 

PARTIAL PRESSURE OF OZONE (nb) 

Figure 13.--(a), (b) Nean conventional and (c), (d) mean short Umkehr profiles 

obtained at NLO in Nay and December 1982 . Dashed curves are ozone profiles 

derived from four ECC ozonesondes flown from Hilo, Hawaii, in December 1982. 

38 
do nonhypsometer radiosondes. A program of comparative measurements between 

the ECC ozonesondes and other high-altitude ozone-sounding instruments was 

carried out during the year. Results of these comparisons, made in Palestine, 

Tex., in June and October, are not available, pending completion of pump efficiency tests on the sondes . 

In conjunction with the Umkehr sounding program established at HLO, a 

program of high-altitude ECC ozone soundings was initiated at Hilo, Hawaii, in 

September 1982. Because NWS modified its balloon inflation shelter and because the shelter was unavailable for our use, the desired fr equency of soundings per month was not attained until December. Hean data for four soundings 

made at Hila during December are shown in fig . 13b. 

3.4 Surface Ozone 

3 .4.1 Operations 

Surface ozone was measured continuously at the four GtlCC observatories 

t hroughout the year with Dasibi ozone monitors. An attempt during 1981- 1982 

to use a second ozone monitor as a calibration standard at SPO does not appear 

to have improved significantly the certa inty with which a calibration level 

can be assigned to the station monitor. Therefore, the previous practice of 

assigning a calibration level based on an annual comparison with the network 

standard instrument has been resumed. Because of the pressure of other projects, it was not possible to assign a second ozone monitor to HLO as a calibration instrument during 1982. 

3 .4. 2 Data Analysis 

The year 1982 marked the tenth year of surface ozone observatio ns at BRW 

and HLO. Monthly mean surface ozone amounts for each of the four stations are 

s hown in fig. 14. A linear least-squares trend line, which ca nnot be distinguished at SMO and SPO from the series mean (also plotted as a straight line), 

is shown with the monthly data. The trend was also computed for the monthly 

anomalies (monthly values from whic h the long-term monthly mean has been 

removed). Since each station has a prominent seasonal cycle, use of the anomalies considerably reduces the scatter about the trend line . It also eliminates the effect upon the trend computation of beginning the series at midyear 

as was done for BRI, and tILO. This information is summarized in table 12 . The 

BRW 

NLO 

StlO 

SPO 

Table 12.--Linear least-squares trend analyses of the monthly means and 

anomalies of surface ozone partial pressure at BRW, MLO, SHO, and SPO 

tlonthli' mean tlonthli' anomali' 

Hean Trend Std. error Trend Std . error 

(nb) (% yr- 1 ) (% yr- 1 ) (% yr- 1 ) (% yr- 1 ) 

25.8 1. 58 2.36 1. 23 1. 16 

25.1 0.50 1. 99 0.59 1.11 

13.8 0.26 4.37 -0.88 1. 80 

20. 1 -0.08 2.11 -0 .52 1. 16 

39 
~,-----------------------------, 

" 

" 

~ N 75 ffl ~7 n ~ 00 81 ~ ~ 

Oa:e 

Figure 14.--Monthly mea n surface 

ozone amounts. A linear trend 

( thick) l i ne for the pe riod of observation is also shOlm . At SMO 

and SPO the trend line cannot be 

distinguished from the mean of the 

series also drawn as a straight 

(thin) line . 

trends are notable for their lack of significance, with none of the computed 

trends approaching the two-standard-error criterion for signifi cance at the 

95% level. 

Imp osed on the annual cycle seen in fig. 14 at all of the GfICC locations 

are large day-to-day variations in ozone . Daily surface ozone amounts for 

198 1 and 1982 are s hown in fig. 15. At BRW, during March-May, large daily 

excursions occur with both the highest and l owest daily va lues recorded during 

this period. At MLO large day-to-day varia tions charac t erize the entire yea r. 

At SMO large variations are spaced somewhat farther apart with high values 

appearing on a 2- to 3-week time scale . The smallest day-to-d ay variability 

is at SPO with the largest changes occurring during the ausLral s ummer . 

3.5 Stratospheric Ivater Vapor 

3.5.1 Operations 

After 1981, a year generally free from balloon performance problems, 

major difficulties with the balloons resurfaced in 1982. A new shipment of 

4,000-g neoprene balloons proved to be totally unreliable . This type of balloon was used s uccessfull y in 1981, but the manufacturer was apparently unable 

to maintain the same standard of performance. A 3,000-g natural rubber balloon was found that is capab l e of carrying the frost-point hygrometer to the 

desired 30-km altitude. Problems arose however , in getting this balloon to 

valve properly and to achieve an adeq uate descent profile required f or the 

40 
: 9:: . 

. '

~ ~ - J I I.! f! 

~;} .,," , ,'\ " II "I j' , . . • ' f ~ \ . "':;" ~'\ 1 I, 

, ~ I' I ,', i, 

I 

.. ,y' '. 

1," 

198i MAUNA LOP 

.q~ ~~ ~I~I~~I~I_"O~~= _~~~ W~~~· 

M, 

• '0 

~ . 

~ j • '.< 

.", 1 

'J '. .r ' .. "" I 'r :.'~" 

.9!:: 

-.... : .. -

. .1 ." ' ,I. ," 

...... -' !-; ',',: 

i , • 

-

, , 

. 

, · 

" 

~ , 

· 

:962 

.. ,.., ,"".".' , .. ,.""",,,",,,. "" W'''""". C", 

1982 MAU~A LOA 

.aq~ ~~.I~I~I~~~I~I"" 'O ~~""_~~""wa ",, ~ 

M' 

~:J,:' 

. 1,/, 

I I !' . " 

! .. .' , " 

.1 ' 

".1 

-I,"" ·1 I 

. ,. " .,. .- .. " } '" " ,. ", ...... ,,,,,,,.""-"""'. ""',>],,.,.,., ... . :~. 

Figure IS . --Daily surface ozone amounts f or 1981 and 1982 at the GflCC 

observatori es, 

41 
higlles l qua lit y da t a . Nea r tile e nd o f t ile yea r a t ec tltli que was ~or d Ollt 

us ing ~o of the 3 , 000 - g ba lloons . The i nstrument pa ckage a sce nds until a il e 

o f the balloons brea ks and then descelld s in a controll ed manner on the r edu ced 

li ft prov id ed by the r emaining ba lloon . This me thod proved t o be reasonabl y 

good, a lthough e fforts are continuing to r e fin e the t ec hnique . In any ca se , 

the rubber ba lloons have been mu ch mo re r e li able than the neoprene ones and 

cos t onl y ab out one-fourth as much. Although at least one sounding was att empted ea ch month, only six successful monthly flights were made in Boulder, 

primarily because of the problems with the neoprene balloons. 

3.5.2 Data Analysis 

The stratospheric portions of the six soundings for Bould e r are shown in 

fig. 16. The November sounding exhibits a water vapor profile somewhat different from that normally seen in the 80- to 10-mb region, increasing steadily 

from - 2 to 4 ppmm. This contrasts with the other flights in which the mixing 

ratio is generally consistent or increasing slightly above about the 60-mb 

leve l from 2.5 to 3 ppmm. A December balloon flight in Boulder and a September flight from Hila, Hawaii (both flights not shown), exhibited even more 

·,,---- ----------- - --r--, l~ ~'2 J() 

1-

'" 

'" 

>oc,}-;_., --='-,;_---___;---;__.--'--''' 

Figure 16.--Water vapor mass mixing 

ratio profiles for soundings at 

Boulder, Colo. 

drastic increases . It is possible that all t hree of t hese flights were affected by sulfuric acid droplets in the stratosphere resulting from the El Chichon eruption. Such droplets are thought to have been present in Hawaii and 

to have moved over Boulder in October . It is possible that these droplets 

were being deposited on the mirror of the frost-point hygrometer, thus indicating elevated wa t er vapor amounts. Because t he September and December flights 

gave erratic signals that did not meet the criteria for a properly performing 

instrument, these flights have not been included in the set of representative 

soundings. For the November flight, however, all of the in-flight checks 

appeared normal and no objective criteria were met for rejecting it. The 

possibility of contamination should be kept in mi nd, however, in interpreting 

this flight. 

A complete discussion of the water vapor time series at Boulder, Colo., 

and at Washington, D.C. , was presented by Mastenbrook and Oltmans (1983) . 

42 
3.6 Halocarbons and Nitrous Oxide 

3.6.1 Operations 

Air was collected weekly in paired stainless steel flasks at BRW, NWR, 

MLO, and SMO during 1982. Weekly flask pairs were collected only during Ja nuary, November, and December at SPO. Flasks were s hipped t o and from the 

stations in.small wooden boxes until April when the boxes were rep l aced by 

high-strength cardboard shipping containers. Also in April, an extra pair of 

flasks was shipped to BRW, MLO, and SMO to be added to the three pairs already 

being used at each station. This ensured that samples would be taken even if 

shipping time to and from Boulder increased. 

When flask samples reached the Boulder chromatographi c laboratory, they 

were analyzed for CFC-11 (CC1 3F), CFC- 12 (CC1 2F2 ), and nitrous oxide (N20). A 

new programmable integrating recorder that provides dire ct peak-height measurements and control of the analysis by a timetable was purchased in April. 

Computer programs were revised for speedy entry, reduction, and plotting of 

the data. 

At the Boulder laboratory, room-temperature fluctuations had been large 

and had degraded chromatographi c performance, until September when an air conditioner was insta lled. The stabil ized room temperature has resulted in more 

consistent results from the gas chromatograph. 

Only one change was made to equipment at the field stations: a PV array 

was installed at NWR to charge the batteries that run the sampling pump . 

Sample flasks normally used at SPO during t he February-October winterover period were kept in Boulder for special tests in 1982. Fifty flasks were 

purged and pressurized with high-purity ni trogen . After a few weeks, the 

f la sks were ana l yzed on the gas chromatograph for pressure loss and con t amination. After the problem flasks were made free of leaks, all flasks were taken 

to NWR and fi lled with air over a 4-h period . Again, after sitting for a few 

weeks, the flasks were analyzed. Inconsistent and contaminated flasks were 

baked at 180a C while being evacuated. This procedure e liminated flask problems. 

The samp ling instructions and background articles given to new station 

personnel for use in training were revised and upgraded this year. 

3 . 6.2 Calibration 

The calibration gas standard, tank 3072, was taken t o OGC in January for 

its routine stability check. CFC- 11 and NzO have not significantly cha nged 

since 1977 whereas CFC-12 has increased by 2.5 pptv yr- 1 . Howeve r , continued 

quarterly comparisons of tank 3072 with two other gas standards, tanks 3079 

and 3088, show no significant relative concentration changes in any of the 

three constituents. 

Two absolute ca libra tion systems, one for NzO/COz gas mixtures and the 

other for CFC- 11 /CFC-12/NzO mixtures, were built in February. Cal ibration 

data confirmed previous results that the correct NzO concentrations for tank 

3072 are 10% less than OGC originally reported. 

43 
When attempts were made to prepare CFC-ll and CFC-12 calibration mixtures 

using N20 as the internal standard, no GC response to N20 was seen. The elec -

tron capture detector's response to N20 increased as the CO 2 concentration 

increased. This anomalous behavior was confirmed by other laboratories. 

Tests are under way to ascertain the effect of CO 2 secular trends and annual 

cycles on the N20 fla s k data. 

3.6.3 Data Analyses 

Halocarbon and N20 selected data for 1982 have been combined with 5 years 

of previous data for statistical analyses and plotting. Figures 17, 18, and 

19 are plots of CFe-ll, CFC -1 2 , and N2 0 data respectively. BRW halocarbon 

data exhibit an annual cycle with highest concentrations during December and 

lowest values in June. No other station shows a statistically significant 

periodicity. SPO data continue to be the most variable. N20 data at BRW also 

have an a nnual cycle, but this could be due to variations in C02 that affect 

the measurements and will be corrected later. SMO N20 data show an unexplained increase in concentration all through 1982. 

Tentative mean concentrations for 1982 and first- and second-order leastsquares regression analyses on t he 6-yr halocarbon and N20 data sets are summarized in table 13. Only MLO continues t o show a statistically significant 

Table 13. --Mean mixing ratios for 1982, and result. of fir.t- "od secondorder regression analyses of CFC-ll, CFC-12, and N20 data for 1977-1982* 

No . of ean mixing ~Iix in g ratio Growt h ratet Growth rate 

Station obs . ratio for 1982 on 1 Jan 1977t changet 

CFC-11 (pptv) (pptv) (pptv yr- 1 ) (pptv yr- 2) 

BRill 258 214.9 154 . 1 ± 0.40 11 . 12 ± O. I 1 

NWR 268 210.5 150.1 ± 0.43 10.93 ± 0.12 

LO 26 1 206 .3 142.9 ± 0.68 13.38 ± 0.50 -0.32 ± 0 . 08 

SMO 269 202.2 134.7 ± 0.37 12. 10 ± 0.11 

SPO 85 214.9 134.6 ± 1. 96 12.70 ± 0.57 

CFC-12 (pptv) (pptv) (pptv yr - 1 ) (pptv yr -2) 

BRill 244 362.9 273 . 4 ± 1. 89 14. 15 ± 1. 26 0.38 ± O. 18 

NWR 228 356 .8 280.7 ± 2.23 II . 12 ± 1. 44 0.45 ± 0.2 1 

HLO 243 353 .8 268.5 ± 1. 03 15.67 ± 0.28 

S~IO 258 345 .8 245 . 3 ± 1 .28 15 . 30 ± 0.92 0.49 ± 0.14 

SPO 83 364 .5 242.8 ± 4.10 9.03 ± 2.70 2 . 09 ± 0.41 

N20 (ppbv) (ppbv) (ppbv yr- 1 ) (ppbv yr- 2) 

BRill 250 303.8 300 . 1 ± 0.20 0 .61 ± 0.05 

NWR 243 304 .8 299.1 ± 0.23 0.99 ± 0.06 

~ILO 250 304.0 298.3 ± 0.25 0.99 ± 0.07 

SMO 239 309 .3 299.1 ± 0.31 1. 59 ± 0.09 

SPO 105 302 . 2 297.5 ± 0.32 0.81 ± 0.09 

,"Coefficien ts are followed by their standard deviations, If a second-order 

coefficient was not significant, a first-order analysis was performed. 

t95% confidence interval. 

44 
L-~ ________________ ~ 

-r-------------------------, 

L---~----------------~~ 

" ,----------------------, ~ 

-

, 

'1 

f 

""1'0 I ~ .. 

.:;" " ':. ,', ;,;: 

'., '. 

"' '" -'I 110 III II~ 

-

~ 

: 

~ 

~ 

-

?: 

-

~ 

: 

" 

-

: 

,-

: 

~ 

• " 5 

?: 

: 

~ 

: 

" 

II 

\\\ B 

..... ,', .:-.... 

;-:po 

: 

" 

1 

'-, 

:'';'" .... >#>,-

....... 

'" "I B() III Il~ 

Figure 17.--CFC-ll data record , Figure 18.--CFC-12 data record. 

-

-

" 

J 

BH'\ -

-

• -, 

~ 

\ \\ Il -

: 

: 

-, 

: 

. 

- ' 11.0 -

~ 

~ 

~ 

~ 

: 

-

: oL-------------____________________________ -" 

g-~ I 

_ "'" '.'-',--', --i '~." ":" ,: ',J"_.:.:"'-': '.' .~.'" 

". "I lin 

Figure 19.--N20 data 

III U~ 

record. 

45 

1 
decrease in CFC-II growth rate, whereas it is the only station not showing an 

increasing growth rate in CFC-12. 

3.7 Stratospheric Aerosols--Lidar 

GMCC lidar activity at MLO came into national prominence on 28 January 

1982 when the Mystery Cloud was first detected and reported by T. DeFoor and 

K. Coulson. The commercial news media publicized the discovery and some commotion was raised because of the unknown origin of the cloud . The cloud 

spread northward rapidly and was detected by lidars located at higher latitudes. Interest in the cloud faded rapidly, as did the cloud. However, at 

the end of March and in early April, Mexico's El Chichon volcano erupted and 

produced a tremendous stratospheric dust cloud that persisted the entire summer as an annulus in an equatorial band between about 100S and 30 o N. 

Information on the El Chichon cloud was quickly relayed to the scientific 

community as a highly significant meteorological event. The El Chichon stratospheric cloud mass was about the same order of magnitude as the Agung stratospheric cloud in 1963. MLO lidar operators increased the observation rate 

from once Lo Lwice per week to obtain finer time resolution of changes in 

cloud-profile structure, and more than 50 observations were made. GMCC received numerous requests for MLO lidar data. Among applications of the data 

are investigations of satellite remote sensing errors, Umkehr remote-sensing 

errors, climate modeling, ozone photochemistry modeling, and stratospheric 

dynamics. In the annals of historical meteorology, the MLO lidar data will 

occupy an important position. A summary of the tlLO lidar data is given in 

sec. 4.8. 

3.8 Surface Aerosols 

The GMCC surface aerosol monitoring program during 1982 included continuous measurement of CN concentration and integrated light scatterring at BRW, 

tlLO, StlO, and SPO . All data were recorded as I-min and I-h means on magnetic 

tape and also on backup chart recorders . CN concentrations were measured 

using G.E. CNC's (catalog no. 112L428) with modifications suggested by 

N. Ahlquist of the University of Washington. Calibration points for the automatic CNe's were provided by daily Pollak CNC observations. Light scattering 

was measured using four-wavelength nephelometers that measure the scattering 

portion of aerosol extinction simultaneously at wavelengths of 450, 550, 700, 

and 850 nm . Calibrations of the nephelometers are performed at 2-mo intervals 

by filling them with CO 2 gas and adjusting the instrument outputs to the known 

scattering coefficients of CO 2 . 

3.8. 1 Barrow 

The BRW Pollak CNC operated properly throughout 1982 and provided daily 

observations for routine calibration checks of the G.E. automatic CNC. The 

G.E. CNC produced acceptable data for about 47% of the year. Other than downtime for routine maintenance and calibration, the major periods of downtime 

were DOY 1-12, 23-47, 49-53, 61-77, 124-140, 142-173, 251-265, 282-284, and 

314-316. 

The nephelometer produced acceptable data for about 76% of the year, with 

the only significant periods of downtime occurring during DOY 137-141, 219, 

46 
and 325-342 . The 325-342 data will be recovered from the ba ckup chart recorder. 

3.8 . 2 Hauna Loa 

The HLO Pollak CNC, which operated properly throughout 1982, provided 

daily observations for routine calibration checks of the G.E. automatic CNC . 

The G.E . CNC produced acceptable data for about 95% of the year. Other than 

downtime for routine maintenance and calibration, the major periods of downtime were DOY 1-4, 115-116, and 197-202. 

The nep helometer produced acceptable data for about 49% of the year . The 

major period of downtime was DOY 1-119 when the instrument was at the University of Washington for repair. Although two problems were repaired (the white 

object solenoid a nd photomultiplier), the signal-to-noise ratios of the 700-

and 850 -nm channels have been excessive so that Angstrom exponents calculated 

from 550 and 700 nm and from 700 and 850 nm are not as reliable as in previous 

years. However , lo ng-term averages of the data remain reliable. 

3 . 8 . 3 Samoa 

The SHO clean-air sampling building received a direct lightning strike at 

1500 LST on 28 Harc h (DOY 87). All aerosol i nstruments were damaged except 

the G.E. CNC. A new Pollak CNC po,,'er supply was mailed to SHO and was back 

online DOY 95. The Leeds and Northrup chart recorder was shipped to Boulder 

for repair and was returned to SHO and was back online DOY 148 . The nephelometer was repaired at the SHO site and was back online DOY 155. Since I CDAS was 

also damaged by the lightning, data were not available on magnetic tape un t il 

DOY 141. The lightning strike accounted [or the major periods of downtime for 

all aerosol instrumentatio n during 1982. 

The SHO Pollak CNC (SN 20) was operated until 7 Harch when it was re -

placed with Po l lak CNe SN 22 because of erra tic operation. Po l lak CNC SN 22 

was operated throughout the remainder of 1982. Daily observations of the 

Pollak counters provided routine ca libration checks for the G.E. CNC, which 

produced acceptable data for abo ut 82% of the year . Although the instrument 

itself was opera tional, data were l ost during DOY 87 -1 41 because no recording 

equipment was available. Routine calibration and maintenan ce accounted for 

t he remaining amount of downtime. 

The SHO nephelometer produced acceptable data for about 68% of the year. 

Other tha n downtime for ro utine calibrations, the significant periods of downtime were DOY 50-68 for repair of the filter wheel motor, DOY 88-154 for repair of damage ca used by the lightning strike, and DOY 160 for spare board 

repairs . 

3 . 8.4 South Pole 

The SPO Pollak CNC operated properly throughout 1982 . Daily observations 

from it provided routi ne calibration checks for the G. E. automatic CNC. A new 

Rawson-Lush mi croammeter (0-10 jJA) was included in the midwinter airdrop to 

replace a broken unit. The broken unit was sent for repair to Boulder on the 

opening flight. The G.E . CNC produced acceptable data fo r about 71% of the 

47 
year. Other than downtime for routine calibration and maintenance, the major 

periods of downtime were DOY 1-31 a nd 316-3 19 . A complete spare G.E. CNC was 

mailed to SPO at the end of the year. When problems occur with the G.E. CNC 

in the future, it can be replaced with the spare unit, and the inoperative 

unit can be repaired in Boulder during the austra l summer. 

The SPO nephelometer operated properly throughout 1982 and produced ac -

ceptable data for about 69% of the year . Downtime was caused by slow recovery 

of the instrument after calibrations , power outages, and times of extreme l y 

low aerosol concentra tion s that ca use d the instrument to drift off scale . 

3 .8.5 Data Ana l ysis 

Data analysis proceeded as described in the previous GtlCC Summary Reports. All observer notes and chart recorder data are examined upon receipt 

in Boulder to assure proper instrument performance. Aerosol data are stripped 

from the monthly tapes made available by the A&DtI group, and files of hourly 

means and 10-min graphics are produced. Missing data are then filled in, and 

necessary edi ting and calibration are applied . All aerosol data are available 

from GMCC in printout, microfiche, magnetic tape, or graphic form. 

3.8.6 Discussion of Selected Data 

Light-scattering and 

tables 14-17 and fig . 20 . 

CN data for the four stations are presented in 

All available data were used to calculate monthly 

Table 14.--BRW monthly geometric means of CN concentration (cm- 3 ) and 

light scatterIng (m 1 ) at 450, 550, 700 , and 850 nm, where values 

appear in a compact exponential format (5.68-6 = 5 . 68 x 10- 6 ) 

JAN '" ." ." '" '" '"' '" '" OC1 IOOV DEC 

1975 e N " 210 '" m '" " m 2}2 17~ " I€' 22< 

L 976 eN In 127 m 172 '" IO~ ." '" '" '" m 201 

b(~ ~DI 5 . 68 - 6 2 . 17-6 D~ -7 

bl SSO) <. \6-6 L 0-6 C 7\-7 

b(700) 1. 12-6 1. 08-6 L (;( - 7 

b ISSO) 2. 09-6 1 . 11-7 2 . 4(-7 

\971 eN '" I o ]6] '" 10' 

b( 4 50 I 1. 0 ':- 5 1 . 70-5 1 . 9 4- 5 I .': 7-5 " " ~. 21-6 '" 1. P 1" -6 6 . ( 9-6 " I.C9-~ " 1.~2-5 '" 

b(SS:!) J.e.:-s I . (9-5 65- 5 1.15-5 L 12-6 1 . 02-6 <. (-6 7 . (\- 6 l. 11 - 5 

b(7 00) 2 . 10-5 1 . 00 - 5 . 08-5 6 . 65-6 2 . 77 -6 2 . 76-E; .: . {'6-6 6 . 6C-6 I . (' .:- ~ 

b(SS O) 1.68-5 7.(5-6 7 . 90-6 <.H.-6 2 . 69 -6 2 . PO-6 ( . 62-6 6 . I ~-( 92-6 

1978 ~ '" "2 '" 1]8 10' '" )61 122 "2 b(45 0) L 32-5 1 . 22-5 1. 58 - 5 1 . 0-5 6 . S8 '" " M 6 1. H·6 2 • .'6-6 2 . ~9 -6 S. 0(.-6 7 . 97-6 (;. ~9 6 

b(550) 9 . 8J -6 1. 07 - 5 1 . 33 - 5 1 . 22-S 5 . 2<- 6 2 . 67 - 6 2 . :: ~- 6 2 . <:2-6 ~. 25-6 7 . lS-6 6 . I ~-( 

b(700) 9 . 1~-6 7 . 1<-6 8 . 70-6 7 . H-6 1. 19-6 l. H-6 1 . 9(-6 2 . :: 1-6 2.fO-~ ~S -6 <. ~O-6 

ble50) 8.85-6 5 . 25-6 6.23-6 5 . 19 M 6 2 . 19 - 6 e . ( 1-7 1. 71 - 6 \ . 9( -6 2 . r2 - 6 c 12 - 6 1. « _r 

1979 C~ ~ 17 '" ~66 272 "' 180 ", 199 " " 12S 227 

b(450) 6 . 69-6 9 . 63-6 2 . 16-5 1. 20-5 5 . 10 - 6 1.4,-6 1. 7,- 6 L 26-6 2 . 21-6 6 . 19 - 6 7 . ,2 - ( I . «(-5 

b(550 ) 6. 15-6 8 . 8\-6 2.01-5 I . C9-5 (. 26-6 l. \ 3- 6 !. \';-6 ·2 . 98-6 2. \ ,-6 C. 29-6 7 . \e-6 I. 0-5 

b (700) <.42-6 6 . 19-6 I . ( 2- 5 7 .( 6-6 2 . 66-6 6 . 77-7 2.05-6 2 . 21 - 6 1 . 73 -6 5 . C2-( 5 . 51-6 I . C5-5 

b(850) 3 . 35-6 (,60 -6 8.78-6 (.( \-6 1 . 65-6 (. 75-7 \ . (9-6 1 . 72-6 I. 3C-6 (. C \-6 C l 8 - 6 8 . (5-6 

1geo C~ m 305 300 '" " '" 99 '" 55 " " 3C~ 

b (50) 1. 05 -5 5 .46-6 7 . 13-6 8 . 99-6 1. \0-6 1. 26- 6 I . 11!-6 2 . 5(- 6 2 . ~5-6 2 . C7 -6 50-( I . 1~-~ 

b(550) 1. 0 4-5 5. 12 -6 6 . 86 -6 1.60-6 2 . 65-6 1 . 05-6 9 . 96-1 2 . ; (- 6 2 12-6 I. 8 3-6 (. P !-e. I.<f-~ 

b(700) 7 . 83-6 ], ~7-6 .;. (8-6 (. 96 -6 1.1\-6 6 . 2e - 7 6 . ( 5-7 I . n-6 I. ~9-6 1. 2C-f ; . 1~-6 8 . 7£'-C 

b(850) 5 . 98-6 2 . 57-6 3 . 0 6-6 3 . 36- 6 1. 10 -6 <. 30 - 7 (.56 - 7 I . ::5-6 I. 2\ -6 8 . 99 - 7 2 . 29-6 L 53-r 

1981 " '" ]" '" 217 '" 133 !6( '" 132 " 231 2V 

b«50) 1. 29 - 5 1. 22-5 1 . 07 - 5 1 . 0 ';- 5 ';. 15-6 1.78-6 2.(\-6 1 . 26 -6 2 £ 1-6 C~ 6 I . ~C-5 2.E ~ 

b(550) 1 . 25-5 1. 12 -5 9.89-6 '.l. C3 -6 3.62-6 I . (7-6 2 . 26 - 6 I. 1-'-6 2 ( 1-6 ( . ., '-10 \'-'~-5 2 . -\-5 

b(7 00) B.93-6 7 . 58-6 6.73-6 5 . (9-6 2 . \8-6 8 . 39 - 7 l. 7! - 6 8 . 6S - 7 , P6-6 ). \6-6 I . C6 -S 2 . C I-~ 

b(850) 6.73-6 5 . 5(-6 (.95-6 J . 57 - 6 \ . 3B-6 5 . 67 - 7 I. '6-C; 1 . 39 - 7 I. <1-6 .~ 6-6 7 . 82-6 I . ~5-~ 

1982 CN '" " 250 , .. " '" " " " 62 " 1\7 

b(450) 1.31-5 \.89-5 2 .6 3-5 2. 18-5 9 . 22-6 2.2(-6 2.82-6 <.6 7 -6 2 . 7<:-6 3- Jr-6 7 . 6(-6 I . H-S 

b (550) I. 20- 5 1.76-5 2 . 33 -5 1. 93 - 5 7 . 59-6 1.80-6 2 . ( 2 -6 .!. S6 - 6 2 . 55- £ 2 9; - 6 6 . 82 - 6 I . S5- 5 b(7 00) 8 . (2-6 1.26- 5 1 . 50- 5 1.24-5 (.57- 6 \ . \3-6 1 .6£ - 6 2.66 - 6 \.9\-6 2 06-6 4.70 -6 I . (2-5 

b (B50) 6 . H-6 9.40-6 1 . 05-5 8.78-6 l.06-6 ~2-7 I . -6 2.00 -6 I . ~-6 I. a- 6 l ~!> -6 I . (2-!> 

48 
Table 15.--MLO monthly geometric means of CN concentration (cm- 3 ) and 

light scattering (m 1) at 450, 550, 700, and 850 om, where values 

appear in a compact exponential format (5.68-6 = 5.68 x 10- 6 ) 

19H e N 

b( 4'>D) 

b15s0) 

b(700) 

blaSO) 

1975 eN 

tH 4 S0) 

b(550) 

b(70D) 

b l aSO) 

1976 

1977 

\978 

'" b( 450) 

b(550) 

b(700) 

b (SSC) 

'" b{ (SO) 

beS SO) 

bPOO) 

beaSOI 

'" b( ' SO) 

b(5S0) 

b(700) 

b ISSO) 

1919 e l: 

b( 4 S0) 

b(SSO) 

b(100) 

b18S0) 

1980 eN 

bl' 50) 

b15S0) 

b(700) 

b (850) 

1981 eN 

b(450) 

bC'>50) 

b(10D) 

b (850) 

1982 e N 

b1450) 

b(SSO) 

b(700) 

bl8S0 J 

J AN 

1. 15·6 

e . 69 - 7 6 . \ 9- 7 

) . 82-7 

J . 39-7 '"2 . 37 - 7 

L 66- 7 1.00- 7 

3. 98'" - 7 

2 . 54- 1 

\ . 58 - 7 

1.06- 7 

6.81-7 '" 5 . 53-7 

1. 5 4 -7 

-7 

175 

(. \3-6 

2 . e6-6 

1. 79 - 6 

1.2\-6 

>B. 6 . 7<-7 

4 . 40-1 

2 , (8-7 

1. 85-7 

7.41-7 '" S. L ~-7 

3.0(-7 

\ . 63-1 

4 . 68-7 '"1. 17-7 

1.82-7 

1. 17-7 

,,, 

'" 

1. 6 4- 6 

I . 27 - 6 

1. 0 4- 6 

7 . <7-7 

>0. 9 . 2l-7 

6 . 82-7 

5 . 0 4- 1 

J . 29-1 

m 6. 94- 7 

S. ell-' 

) . 29-7 

1. 57-7 

7. e2-' '"6 . e2-7 

4. 77-1 

3 . 24-1 

I. 1~-6 '" 11 . 18-1 

. 60-1 

3 . 1l-1 

9 . ::S-1 '"

. -1 

J.~ -1 

2 . -7 

I . C1-6 '" 7 . 57-7 

. 53-7 

2 . 54 -7 

1 • 56-7 '" I . ~0_7 

l.rO-7 

9 . n-8 

'" 

.-,AR 

2 . 86-6 0~ 1 

1. 88 - 6 . 83 - 7 

1.24 -6 4. 28 - 7 

7 . 90 - 1 2.95-7 

8 . 12-1 '"5 . 95-1 

L 38 - 1 

2. -1 

8 . 611'" - 7 

. 6 . 58-1 

C 27-1 

2. 88 - 1 

9 . 29'" - 1 

1 . 12 - 1 

~. 9J-7 

3. 51-1 

1 . 92-6 '" 1.37-6 

8 . 87-1 

6 . 15-7 

4. 51-6 '" .L -6 

2 . 21-6 

1. 55-6 

'" 2 . 16-6 

1. 5-6 

8.87-1 

-1 

I . J7-6 '"1.00_6 

9.27-1 

6 . 8 4 -1 

, .. 

'05 2.0<-6 

I . 6~ 6 

1. 2]- 6 

8 . 67 - 1 

230 1.64 - 6 

l. ~- 6 

8 . 70 - 7 

5 . 30 - 1 

m I . -6 

1 . 21 - 6 

8 . 26-7 

5 . 1\-7 

0~-6 '" ! . 89-6 

2 . 8~-6 

2 . 10 - 6 

on 3 . 40-6 

2 . 60-6 

I . U-6 

l. 39 - 6 

", 

3 . 01-6 

2 . 28-6 

\.59 - 6 

1. 22 - 6 

,., 1. 52-6 

I. 21-6 

8 . 89-1 

6 . 83 - 7 

"lAY 

I . ~6-6 

1 . 24- 6 

1. 0 4 - 6 

7 . 71-7 

,go 

2 . 11 - 6 

2 . 10- 6 

1. 8 4-6 

1 . 61 - 6 

1 . 82-6 '" I . ~- 6 

1 . 24- 6 

9 . 01 - 7 

1 . 0 4-'" 6 

9 . 16-1 

7 . 15- 7 

4. 89 - 7 

26S 2 . 20 - 6 

1.75-6 

I. j~ 6 

I . 10 - 6 

n, L 69 - 6 

2 . 93 - 6 

2 . 23-6 

1. 76 - 6 

1 . 9'" 4- 6 

1 . 55-6 

I . 14 -6 

8 . 6 6- 7 

2S? 

I . -6 

1. >0; - 6 

I . 19-6 

I . 11 - 6 

". 

2. 06-6 

1. 73-6 

1 .4 2-6 

9 . 11-7 

270 

7 . e9-7 

6 . 27 - 1 

4. 64 -1 

3 .40-7 

7 . 92-7 '" 6 . 23-7 

(.53- 7 

2 . 13-7 

9 . 23-7 '" 7 . 69-7 

5 . 78-7 

3. 77-7 

1 . 26-6 '" 1 . 02 - 6 

7 . 71-7 

5 . 05-7 

2 . 75'" - 6 

2 . 08-6 

1 . 52-6 

1. 24 -6 

3 . 97-6 '" 2 . 97-6 

2 . 09-6 

l. 5 1- 6 

2.98-6 '" 2 . 12-6 

I. l7-6 

9 . 19-7 

,go 

'" 7 . 95-1 

6.29-7 

5 . 05-1 

J. ( 9-1 

212 5 . 17-7 

J . 89 - 7 

2 . 72-7 

1 . 64 -7 

'26 7 . 08-7 

5 . 32-7 

3 .46-7 

l. 94-1 

4 .88-7 '" 3.67-7 

2 .34 -7 

1 . 60-7 

, .. 7 . 9 4 -7 

6 . 25-7 

J . 95-7 

2 . 54-7 

1. 10'" - 6 

8 . 53-7 

5 . 08-7 

],25-7 

,eo J . 10-6 

2 . 23-6 

1 . 51-6 

1 . 05-6 

9 . 68-7 '" 6 . 64-7 

3 . 76-7 

2 . 20-7 

'" 

1. 70-7 '"3.05-7 

2 . ~6-7 

I. '1-1 

'" 

no 5 . 18-7 

3.65-7 

2 . 49-7 

1 . 54-7 

5 .40'" - 7 

J . 99-7 

2 .48-7 

1 . 32-7 

232 

6.27-7 

4. 55-7 

2 . 17-1 

1.83-1 

5 . 54-7 '" 3 . 92-7 

2 . 18-7 

1 . 58-7 

1 . 14'" -6 

7 . 25-7 

4. 01'-7 

2 . 80-7 

230 

303 

I . ]3-6 

9 . 16-7 

5 . 68-7 

3 . 2]-7 

'91 

306 

4. 41-7 

L 4\ -7 

2 . 10-7 

1. 67-7 

7 . H'" - 7 

5 . 23 - 7 

J . 50- 7 

2 . 11 - 7 

280 J . 07-7 

2 . 01-7 

I . 18- 7 

7 . 21-B 

"2 8.14 - 7 

5 . S9-7 

3.63- 7 

2 . 44 - 7 

9 . 31-7 '" 5 . 70 - 7 

l. OC- 7 

2 . 10-7 

\. 14-6 '"7 . 29-7 

4. ::0- 7 

J . 15- 7 

9 . n-7 '" S.5P-7 

3. 1.,- 7 

2.00 - 7 

m I. 11-6 

'.60-7 

4. <3 - 7 

2 . B5 - 7 

30! 

4 . 02 - 7 

1.17-, 

2 . 59 - 7 

l.51-7 

m 3 . 2e-7 

2 . C6-7 

1 . 70 - 7 

1.07- 7 

m 2.4\-7 

1 . 51-7 

8 . 33-1' 

0~ B 

298 

3 . 11-7 

2 . 09-7 

I . 18-7 

9 . 5\-S 

'" 

1 . 75-6 '"

\. 15-6 

6.19-7 

4 . 85-' 

\. t3-6 '" 6.70-7 

3.68-7 

2.29-7 

277 

7 . ~1-7 

9~-7 

2 . 68-7 

1. 97-7 

<00 

!. U-7 

2 . fO-7 

2 . 19-7 

1 . 27-7 

3 . 76-7 '"2 . 61-7 

I . e6-' 

I . 19-7 

2 . <1-7 '" I . !e-7 

7 . 90-e 

5 . ec -p 

"0 J . 36-7 

2 . .,7-7 

1.80-7 

1.12 - 7 

'<0 

5.70-7 '" l. 32-' 

1 . 62-7 

I. 36 - ' 

6 . 'H-7 '" 4. 54-7 

2.45-' 

1 . 60-7 

,,, 4 . 6(-7 

1. 00-7 

1. 72-1 

t. 35-1 

27~ 

L (9-7 

J. IO-~ 

~~-­

I . ce-7 

2 . 91 '" - 7 

2 . 03-7 

I. <5-' 9 . 11 4-11 

2 . 71-7 '" 1 . 62 - 1 

9 . 68-1' 

6 . 10-1' 

1. 16'" - 1 

2 . le-7 

1. 46-7 

1. 24-' 

.. 36 

6 . 14-7 '" <. r 1- 7 [,96-7 

l. }J-7 

f. 6~'" 7 

5 . ~4-7 

2 . 79-7 

1 . 66-7 

~. e3-7 '" J . 01 -7 

1 . 14-7 

I . J9-7 

5 . 0J-7 '" 1. 9l-1 

! .C2-1 

I . P-6-7 

Table 16 .--SMO monthly geomet ric means of CN concentration (cm- 3 ) and 

light scattering (m 1) at 450, 550, 700, and 850 om, where values 

appear in a compact exponential format (5.68-6 = 5.68 x 10- 6 ) 

1<;76 Ct. 

1917 . 

lo{ ' SO) 

be 550) 

b(70C) 

b(E,)O) 

t 97E C N 

be ~SO) 

be ~ ')0) 

bP(CI 

bees( ) 

t ~79 Ct: 

be ~ ~O) 

l>e sse) bPOO) 

blBst) 

19H CN 

I ge I CN 

be( 50) 

be ')')0) 

b(7CO) 

b1E50} 

19B2 CI. 

bl 4 50 ) 

b(550) 

bUOO) 

b(8S0) 

J~ N 

'09 

2.0(-5 

I.el-,) 

I . es-s 2 . C4- 5 

121 

I . (2-~ '" I . 29- ~ 

1. 29-') 

l. !l!- 5 

'" 

." ' . 12-5 2.77-5 

2.B3-5 

l.C2-5 

'" 

2" 

1. 5t-5 '" !. ( !-S 

L 4 1-5 

!. 51-5 

'" 

'" 

229 

H' I . -5 

l.7t-S 

I . '1~-~ 

l. t:e-5 

1 . 57-5 '" I . c2-5 

1. 0-5 

l. C,0 - 5 

I . <8-5 '" I . (C-5 

1 . 50-5 

I . 6~-5 

n9 I. 8-5 

I . ~ 

I. 9-5 

I . e -5 

, eo 

2 ~., 

1. 28-5 '" I . OB-~ 

1. 07-5 

t. l(-S 

~82 

1 . 55 - 5 

I . 2-5 

I .H-S 

I . 'ie-5 

I . '" 5-5 

1 . e-5 

I . 2-5 

I . ( -5 

,,, 2 . 35 - 5 

2 . 0 4- 5 

2 . 12 - 5 

2 . 2P -S 

1 . 2')'" - 5 

1. 20-5 

L. 2B - 5 

t. 46 - 5 

1 . 22'" - 5 

I . 15 - ') 

I . 26 ~ 

I . !O - S 

JU),; 

'0> 

! ~5 

2. 11-5 

1.93- 5 

\.ge-5 

2 . 11-5 

26' I. 91 - " \.81-'i 

1 . 9(-') 

2 . 21-') 

~o ! 

2. 1)-5 

1.95- 5 

2 . 15-5 

2 . 75-5 

1. 2 '" !-S 

I. \7-5 

1. 21-5 

I. H-~ 

49 

,eo 

I . 3~-5 '" I. 12-5 

I. U p S 

I. 2<-5 

'96 1.99-5 

1. 89-5 

2 . 00-5 

2 . 16 ~ 

'69 2 . 66-5 

2 . 12-5 

2 . S5-,) 

3 . 27-5 

'" I. ! '" <-5 

I. 32-5 

I . '5-5 

t.6S-S 

,,, \. ~C S 

\. 2C-5 

\. 27 - 5 

I. 3e - 5 

1. 01-5 '" 2 . 71-5 

2 . 9'1-~ 

3 . lJ-5 

286 

1 . 91! - 5 

1. 1!0-5 

1 . 86-5 

1.99-5 

'" 

'9> 

1 . 0 4'" -5 

9 . '16 - 6 

1 . 02-5 

1. 12 - 5 

1 . 37-5 '" l. H-5 

I. ( 6-5 

1.6 l -5 

'" 

2 . 30-5 '" 1.97 - ') 

1. 9'1 - 5 

2 . 09 - 5 

202 

29 ~ 

2. 09 - 5 

2 . 1C, - 5 

2 . 31-5 

I . "'-'" 5 I . !6- 5 

I . ~I! S 

1 .49- 5 

~ 38 

1 .44- 5 

1 . 0 - 5 

1 . 50 - 5 

1.66- 5 

on 

3 . 02'" - 5 

2 . 64 - 5 

2 . 13 - 5 

2 . 95-5 

1.88-5 '" 1 . 72-5 

I . '9- 5 1 . 92-5 

m 1 . 69- 5 

1 . 59 - 5 

1 . 65-5 

1 . 79 - 5 

1. 27-5 '"1. 25 -5 

1.11 - 5 

1. 4 5-5 

," 

226 

2 . 61 -5 

2 . 36-5 

2.50-5 

2 . 76 - 5 

'" 

1O2 

m 9 . 55-6 

S . 96-6 

9 . 46 - 6 

1.05-5 

\.90-5 '"I. 9)- 5 

2.09 - 5 

2.H-S 

'" 

J. 0-5 '"J . II-5 

J . 31-5 

6~ 5 

2" 

'" 

'" 

«0 I . 10-5 

1. 05-5 

I. II ~ 

I. 24 -5 

2J2 

1. 23-5 

1.11 - 5 

1.26-5 

I. ~ 
Table 17.--SPO monthly geometric means of CN concentration (cm- 3 ) and 

light scattering (m 1) at 450, 550, 700, and 850 nm, where values 

appear in a compact exponential format (5.68 - 6 = 5.68 x 10- 6 ) 

\9H e N 

1975 e N 

1916 eN 

1977 ~ 

1978 eN 

1979 eN 

b( SO) 

bISSC) 

bPOO) 

b(650) 

ISoeo cr. 

19B I (I; 

be ~SC) 

t;( ~SC) 

bnCO) 

0(650) 

1ge2 C:' 

b« SO) 

b (S5C) 

b (7CC) 

~ (E50) 

" 

125 

12 ! 

10; 

III 

L 65- 1 

2 . 72-7 

\. 22-7 

5. 52 - 8 

1.31 

U9 

C 03--

2 . ?a.7 

L \7·-

6S-E 

'" 

" 

106 

136 

'" 

"e 

II! 

125 

'" 

9\ 

" 

" 

" 

II 

ISS I~! 50 

~.f; ~-7 2.~~-7 L!8-7 

3 . H-7 1. ~~-1 1.2 ~- 7 

1. ~- 7 1.~6-7 e . OC-f' 

9 . 1,-8 B. H - B ~~ e 

2C" 96 H 

;. 62-7 '" 2 Ce-1 

So . eE-~ 

£. lS - e 

". :,-7 " 1. ':~-7 

7 cs-e ~. 73-1! 

),26-7 "2 . ~C i 

I. 5~-­

lo2l-' 

!« e~ <\ 

3 . 11-72 . 86 - "' 2 . 79-7 2 . 21'-7 

2 . Ce-7 1.1'2-" 2 .IC- 7 1 . "'!-7 

I . OC ·" e. ss-£ 1. ;5-1 t.2!-' 6 , ],·£ 5 . 6,-8 1 .19 - 7 9 . !1-8 

~ \ 

21 

21 

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1.21"-1 

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l . C7-' " 2 . 1(-, 

1 . 59-7 

1.15-7 

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2.~9 1 

I . - i-7 

I . (\--

11 

~~ --" 2 . 93-7 

2 .29-7 

I . "2-7 

" 

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~.~--~ 

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2 . C£--

I . 2~-7 

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I;> 1 Z 2C 

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1.(~-7 2.-7_7 l.:C--

1.19- - z. ;:. " f'~

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'1 

., 

21 

;.2'-i " l. 1~_7 

2 . ~f·7 

I . £(-7 

}f 

OC1 

79 

ICi 

3 . ~(,-7 " 1. 7(-7 

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:~' (2 "IF-- (.n-7 

2 . 97-. 1 . • '_7 

C~-~ Llf--

~~ -- I . if--

~ --. . . :.;< . :--- '; f~-~ 

l. ,;.- ' . C-I 

NOV 

IS' 

'" 

IH 

I'? 

\ ~ 

S . H·c (. ((_7 

L PI-' 

' . cr-7 

I I ~ 

I I ~ 

II.! 

"' 

I,' 

:Lff-? E-~ 

~. 'E-~ (-

;I! 

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: . (_7 

, ... ~ --

~ ; 

:: \--

•. £:-7 

. :~-f 

7 . C(-f 

geomeLric mea ns, except for MLO, where only 0000-0800 LST data were used to 

avoid possible local contaminati on from the upslope wind. Linear leastsquares trend analyses similar Lo those given in the last two G~ICC Summary 

Reports (DeLuisi, 1981, p. 41; Bodhaine and Harris, 1982, p. 45) were appJi.ed 

t o the data sets shown in tables 14- 17 and fig. 20. The trend lines are superimposed on the data in fig. 20 and the trend analyses are given in table 18. 

Th e trend lines for light scattering were calculated in all cases from the 

550-nm data. 

Table 18.--Least-squares trend analysis of the common logarithms 

of the data give n in fig. 20* 

BRW a sp 

N 

ttLO 

a sp 

N 

StiO 

a sp 

N 

spO 

asp 

N 

Slope 

o 0003320 

- 0 0008493 

o 001119 

o 0009124 

- 0.003490 

o 001419 

o 00004082 

- 0 .0004128 

Intercept 

-5.293 

2.257 

- 6.236 

2.325 

-4 543 

2 . 354 

- 6.591 

.704 

S.E.t 

0.3968 

0.2783 

0.3456 

0 .1116 

0.1057 

o 09268 

0.1864 

0.4270 

o':T he scale of the abscissa in fig. 20 is such that January 19 74 = 1 and 

December 1982 = 108. 

tS. E. = standard error. 

50 

Trend yr- I 

o 92% 

-2.3% 

3 .1 % 

2.6% 

-9.2% 

4.0% 

0 .11% 

- 1. 1"4 
DARROW 

---r= ' 

~~- -~. " ~ \ .... { .".J - < 

sr~:"I,.~~ -_. ~ 

, "- .. < 

" -- -

-

E~ 

. .~ . I. .' ! - ~ ": ~t"""" " .~ :,--:: ~ 

.. ' I 

I \CAR 

\"EAR SOL TIt POL ~ 

~- ~ ... <~-- -

A " f 

YEAR 

Figure 20.-- Mo nt hly geometric means of light-scattering and CN data at BRW, 

MLO, SMO, and SPO. Only 0000-0800 LST data were used for MLO. For each sLation, CN concentration (bottom) is shown as a solid line. Light-scattering 

data (middle) are shown for 450 nm (dotted), 550 run (solid), 700 nm (dashed), 

and 850 nm (long-dashed). Angstrom exponents (top) were calculated from 450-

and 550-nm (dotted), 550 - and 700-nm (solid), and 700 - and 850-nm (dashed) 

light-scattering data. 

Long-term trends are generally less-pronounced in this year's analysis 

than in the previous analyses. For BRW lighL scattering in particular, the 

downward trend of previous years has reversed iLself because of the high winter 1982 and spring 1983 monthly me ans. All oLher trends remain c lose to 

previously determined trends, and in each cas e the change from the beginning 

to Lhe end of the data record is smaller than the standard error about the 

regression line. General discussions of the annual cycles and other features 

of the data shown in fig. 20 have appeared in Lhe last s everal G~ICC Summary 

Reports. 

Figure 21 gives a more detailed presentation of light-scattering and CN 

daLa for the GMCC stations during 1982. For each station (except MLO) daily 

51 
SARRO_ 

H' Jl L Al e; :;">;P OM '01 or('" 

~~ S -

_ 

1-...... -. ...,/"'0 "~ . 

'-~~ -

_"_ -•• 

" . - : -'- . - - -~. 

.1-

J •.• ~._. ;,..". • ~ .·i \ ~. 

__ ----4--....-_.:....:.....;,.. '. . \', ~ 

. \ , ; :; , ::J. _ 

Jj ~ '.I. F .' 

II I 'I 

II 

, , H' If:S IUR \PR \1\\ ;1' ~\G 

"~\Tll or Hlr II'IR 19!I.l 

s. oto. 

I: 

r: 

-. ~ c" 

1, -

~r 

t· 

Jl\ ITa WA R APR lUI Jl ' JlL Ale; !'fP CX"!" \0' DOC 

-

" ._-

~:l "'D;-~-: __ ~ -~ 

- - - ~ . 

" -

E . f---- _ .. 

j I. A,N.. orr 

1 .. _1. 1,..' 1'.-, 1 n.V: 

"'I .,' '.}). , . 

---'----'-' , 

j ' 

I 

,C ''.1 

. I" lA ' r[8 liAR APR lolA) Jl \ JlL Ale; 5[P OM '01 orr \lO\Tlt or TIlE )[AR 1981 

J. , 1"1:& liAR APR IIA) II" Il L H e; ~[P OM \01 01:(" 

'1- -~ 

:.,;, c, .'\-, .,j:;"" ~-:: c' ;::-:' t 

.:'; 

I . 

f" ,- '.\ .- ,',. I 

,' , :;' ; 1 - .. ' ,. I, . I ,. ',.\.' ,.I . !,.','.'" "t ,., 1 r .' ,'" !!.. "~'... . .:1'/ .' . 

! 

--- a\ HII .--'\I.!! I;M "~l -~~---~~-=-' ., 'X""' '01 lin 

\t:l\TH Of' ;m I 1'\11 ~ 

s:l\..TH POLE •• _ _ _ _ a. = ~ _ ~ ~ _ 

~ -...:..i':

., : -v'- ~ ·r - . - . . ~ . 

I" '\ . . 'I"' If I·::~· ~~:\:\ l' '". '.: .,. : 

I , ;-. ··r I 

I ' " . 'I,t .": .... I C" •• ; . • 

H ' n:& liAR APR \I n II' Ill. \Ie; ~f.P OC"T '01 JI 

\lO\liI 01' TIlE HIli 1911.1 

Figure 21 . --Daily geometric means of light-scattering and CN data, as in 

fig. 20. 

geometric means were calculated using all data . For HLO, only 0000-0800 LST 

data were again used to avoid contamination from the daytime upslope winds. 

3 .9 Solar Radiation 

3.9.1 Introduction 

The GHCC solar radiation program consists of many measurement and research efforts related to the interaction of solar radiation and climate. 

Long-term measurements of direct and global (direct plus diffuse) solar radiation are maintained to determine what effects th e changing atmospheric 

composition may have on the Earth's shortwave energy balance. Short-term 

measurement programs are carried out in conjunction with particular events to 

52 
answer specifi c sc i e ntific questions and t o s upplement th e monitoring data 

set . SOlne solar radiation measurelnents are us ed as t oo ls to e stimate the 

atmospheric quantity and radiative properties of certain constituents such as 

water vapor and aerosols. 

3.9 . 2 Monitoring Instrumentation 

Table 19 sho,'s the monitoring instruments online at the four GilCC observatories at the end of 1982. The filter designations, Q, GG22, DG1, RG2, and 

RG8, are the standard WiIO-recommended filters described in last year's GilCC 

SUllunary Report (Bodhaine and Harris, 1982, p. 50, table 14). Instruments 

first implemented during 1982 were the 778- and 862-nm sunphotometers and the 

SPO ,'ater vapor meter. The OGI and GG22 pyranometers at MLO went back online 

Table 19.--Solar radiation monitoring instruments, December 1982 

Instrumen t BRW ilLO SilO SPO Conunen ts 

Eppley pyranometer 

Q X X X X Continuous 

RG8 X X X X Continuous 

OGI X X X X Continuous 

Eppley pyrheliometer 

Q X X X X Continuous 

RG8 X Continuous 

Q X X X X Discrete 

OGI X X X X Discrete 

RG2 X X X X Discrete 

RG8 X X X X Discrete 

Sunp hotometer 

380 rull, narrowband X X X X Discrete 

500 run, narrowband X X X X Discrete 

778 nm, narrowband X X X X Discrete 

862 nm, na rrowband X X X X Discrete 

Shaded pyranometer X Continuous 

Solar IR hygrometer X X Continuous 

after being out of service for about 1 year. All pyranometers listed are 

operated in an upward-facing, level orientation. A complete history of the 

station instrument arrays is chronicled in the preceeding GMCC Summary Reports. 

The principal responsibility for maintaining the narrowband sunphotometers and 

handling the sunphotometer data has been returned to the NOAA Solar Radiation 

Facility in Boulder. Calibration and data acquisition details for most of the 

monitoring instruments were given in last year's GilCC Summary Report. 

3.9.3 Instrument Intercomparison 

The trave ling-standard quartz pyranometer and pyrheliometer (Eppley 

SN 12617 and SN 13909) were sent to all four stations and the intercomparisons 

53 
with them and the station instruments were performed as in past years. Although a preliminary analysis of some of the results was completed, the final 

analysis is not ready for presentation at this time. The traveling-standard 

pyranometer was calibrated at the So lar Radiation Facility on several occasions during the past 2 years, and the most recent calibration indicated a 

change in its calibration beyond the acceptable limits of tl.0%. Since the 

calibration standards of the Solar Radiation Facility were adjusted during the 

same time) we are investigating whether an actual change has occ urred in our 

traveling standard. 

3 . 9 .4 Monitoring Data 

Sunmlaries of pyranometer and pyrheliometer data for several years were 

given in last yea rls GMCC Summary Report . No new data are ready for inclusion 

in this report. 

3.9.5 Special Projects 

Solar radiation measurement activities were dominated during 1982 by the 

presence of two large stratospheric dust clouds. One cloud, of unknown origin, was first detected in January 1982. The other, from the flexican volcano 

El Chi chon, was first detected in early April . Because of the global extent 

and large concentration of these clouds, especially El Chichon, all GMCC solar 

radiation measurements may be affected. The magnitude of the El Chichon c l oud 

was so great and rare that it was considered by many as an event of the century. Certa inly the impact on the MLO solar measurements was by far the largest in 25 years . It therefore seemed prudent to concent rat e efforts on determining the radiative properties of the long-lived s tratospheric component of 

the volcanic clouds. However, several ongoi ng special projects that were 

planned or were being implemented prior to the detection of the volcanic cloud 

were also carried to completion during 1982 . 

A major effort was the establishment of an automated solar observatory at 

ILO consisting of an active, precision, solar-tracking spar; a computeroperated Ash Dome; and automated data acquisition. Instruments on the spar 

are a solar IR hygrometer , an automated multiwavelength narrowband SUIlphotometer, and an Eppley NIP . The automated observatory was put into operation in 

the old lidar dome during September 1982. Dome operation for the day is initiated when an observer determines that weather conditions are su itable . The 

observer activales the dome and acquisition computer, and documents the daily 

log. The dome aperture and active tra cking spa r locate the Sun and follow it 

for the rest of the day. The dome automatically closes in the event of rain 

but otherwise must be closed by an observer at the end of the day. After 

closing, the dome and spar reset to the s unrise position. The most important 

time for the observatory to operate is in the early morning before upslope 

conditions begin . It is therefore necessary that an observer be at the site 

shortly after sunrise . This requirement was met during most of 1982 and into 

1983, although it is not part of standa rd operating procedures at MLO. (The 

dome did not operate on weekends.) Further automation of the dome will allow 

it to sense weather conditi ons and to ope n and close for the day und e r computer control. 

A principal objective of the MLO automated solar observa tory is t o provide spectra l aerosol optical depth, which can best be derived from Langl ey 

54 
OftNl.S S ft(J 6 DftNl.S 7 fill B 

. 

.. 

......... =::------.... 

0000 0 

. 

" ~ ~. 

~" .. 

----------_ ... Z 

...J~ 

•. s ,., 4.' I.' ..s 

Rfl.Rf 1 Y[ A IRIRSS 

DfII€LS 9 fNJ 10 DftMl. " 

-f 

-

t--- " __ ~.; 00 0 

.; 

~ ~; :::====~ i::: .. 

Figure 22 .--Sample Langley plots from the seven-wa velength s unphotometer 

operating 1n the MLO automated so lar dome, where the natural logarithm 

of the voltage is plotted agai nst relative air ma ss . 

plots. Since several hours of nearly continuous observations are required to 

obtai n a single optical depth value from t he Langley plot, an automated observi ng system has definite advantages. Figu r e 22 shows the results of 

Langley plots from 1 day, using the seven-wavelength sunphotometer mounted in 

the dome. The plotted data have been edited and restricted to the air mass 

range of 1. 75-7.50 . The Langley plots are of superior quality, with the correlation coefficient often exceeding 0 . 9990 for unedited data and 0.99990 for 

ed ited data. 

A second sunphotometer intended for use at MLO has been designed and 

built. The new instrument, the PMOD triple sunphotometer, has three wavelengths, 380, 500, and 778 nm, and was designed to specifications and drawings 

supplied by ~~ . The instrument will be calibrated frequently at MLO and will 

be used as a standard reference instrument for GMCC sunphotometer calibrations. The PtlOD consists of three sunphotometers housed in a single unit that 

was precision machined to assure proper simullaneous alignment of all chan -

nels . The electronics, detectors, and filters are temperature controlled to 

within O.loC. 

In the spring of 1982 and of 1983 GMCC mad e supplemental measurements at 

BRW designed to de t ermine the optical properties of the Arctic haze aerosol. 

The me asurements included spectral optical thickness, albedo, the ratio of 

spectral global diffuse to globa l total solar flux, and the ratio of zenith 

sky diffuse to direct solar fl ux. Since the derived quantities result from 

instantaneous measureme nts of solar radiation at the Earth 's surface, the 

55 
aerosol optical properties are representative of the total vertically integrated aerosol. However, day-ta-day and year-ta-year changes in the measured 

quantities can be used to deternline the optical properties of individual components of the aerosol overburden . Analysis of the 1982 and 1983 BRW data is 

ongoing. 

Analysis results of some of the G~ICC solar monitoring data relative to 

El Chichon, principally for MLO, have been given by DeLuisi et al. ( 1983), 

DeLuisi (1982), and Dutton and DeLuisi (1983a) . These papers discuss the 

detection and the shortwave radiation effects of the debris cloud. In summary, the 500-nm optical depth of the cloud over MLO was initially near 0.7, 

but it varied grea t ly as the main original plume moved over the station. Four 

monLh s after the eruption, the 500-nm optical depth stabilized at about 0.25. 

At the same t ime, the daily integrals of direct-solar and clear-sky-global 

solar flux were reduced by nearly 30% and 7% respectively, relative to several 

previous years. Although nonspectral global diffuse flux at MLO increased by 

almost 300%-400% in J une and July 1982, this increase was not enough to be 

consistent with the large decrease in total flux, indicating unusually high 

backscattering and/or absorption by the volcanic cloud. 

Information on the El Chichon cloud is less abundant from the other GMCC 

stations because of their locations relative to the volcano and also because 

of observing conditions. Preliminary examination of spa filter wheel NIP and 

sunphotometer data for December 1982 indicate about 0 . 03 aerosol optical depth 

enhancement. However, a time series of the cloud evolution at SPO is not 

possible because of the 6-mo night. Normal optical depths at SMa are large 

compared with the expected El Chichon comp onent . As a result, preliminary 

examination of the S~IO optical data has not shown an obvious El Chichon signal, even though satellite measurements show the clo ud over the station. 

Direct solar measurements required for optical depth determination are only 

possible in the spring at BRW. 

3.10 Station Climatology 

3 .10.1 Instrumentation and Data Reporting 

The interpretation of l ocal meas uremen t s of trace gases, aerosols, and 

atmospheric turbidity requires accurate measurements of station pressure, air 

temperature, and moisture content. Surface winds must also be known to evaluate the potential influence of local pollution sources. Relatively standard 

off-the-shelf instrumentation was chosen for these measurements. Wherever 

possible, WNO-recommended standards for exposure were used. 

A propeller-type anemometer is used (Aerovane, no. 141, Bendix Inc., 

Environmental Science Division , Baltimore, ld. ) to measure the "lind speed and 

direction . A synchro-to-DC converter is used to translate the phase representation of direction to a DC voltage . Orthogonal components are used to average the wind . Station pressure is measured with a capacitance-type transducer 

(no. 1201C, Rosemount, Inc., Minneapolis, Minn.). The voltage output of the 

transducer is recorded without further processing. At BRW, MLO, and SMa the 

air temperature is measured with linearized thermistors (no. 44212, Ye llow 

Springs Instrument Co . , Yellow Springs, Ohio). The thermistors are encapsulated in stainless steel shells that are exposed in aspirated sun shields 

(no . 43404, R. M. Young Co., Traverse Ci ty, Mich . ) . A resistance-type thermometer, with a minimuml acceptable temperature of -85°C (no. 954PL, StQl,> 

56 
Labs . , Hudson, Haine) is mounted in a naturally ventilated radiation shield 

(no . 43103-A, R. H. Young Co., Traverse City, Hich . ) at SPO. Dewpoint hygrometers are used at all four stations (no. 911, EG&G Inc., Newton, Hass., at BRW 

and SHO; no. 1200ASP, General Eastern Instrwnent Co., \vatertown, Hass., at tlLO 

and SPO). 

Hourly average values, scaled in metric units, are processed and reported 

for each measurement listed above. The data are stored on microfiche and 

magnetic tape . 

and variable. 

3.10.2 Barrow 

The microfiche listings are organized by station, date, time, 

The files are available 6 months after the end of the year. 

A description of the BRW site and its local c limatology can be found in 

previous GtlCC Summary Reports. \.Jind roses of the hourly average resultant 

wind speed, in three speed ranges, as a function of direction for 1977 - 1981 

and for 1982, are in good agreement (fig . 23) . For 1977-1981, wind from the 

easterly sector occurred 62% of the time, and in 1982 wind from this sector 

occurred 60% of the time. For wind speeds of 10 m s-· or greater, the occurrence in 1982 was 80% compared with 85% over the past 5 years (Harris and 

Herbert, 1980). A major deviation from this pattern occurred in February when 

westerly winds prevailed for almost the entire month (easterlies occurred only 

23% of the time). Colder-than- normal t emperatures were also reported in February. Table 20 gives a monthly breakdown of average and extreme values of 

wind, air temperature, an'd station pressure. Recent comparisons \,li th NWS data 

from Barrow i ndicate that the station pressures reported for BRW are low by 

abOUL 2.5 mb. A study to be completed in 1983 will resolve this difference, 

and a correction will be applied. 

BARROW 

.2 

IV 

WISD SPEJ:D (II S) 

_ ~, ... ~ 

r:::=:J~i "S IO 

D .. SliD 

N 

• 

s '-1>:0 fREQ 

E 

BARROW 

77- 61 

WI SO SP[[O (II S) 

_ 5' · ;; ~ 

c::::::l5' ·S < IO 

=:::J WS i 10 

\ 

s lli1:-0 fREQ 

Figure 23.--Wind rose of surface winds for BRW for 1982 (left) and 1977-1981 

(right). The distributions of the resultant wind direction and speed are in 

units of percent occurre nce for the year and 5-yr period, respectively . Wind 

speed is s hown as a function of direction in three speed classes. 

57 
Table 20.--BRW 1982 monthly c limate summary;' 

Joo Fcb fla r Apr May Jun Jul Aug Sep Oct Nov Dcc 

Prevai I ing .. dod El'.'E WNl,.,' ENE NE E E E WSW ENE NIl ENE ENE 

directi o n 

Average ' .... ind 6.6 6.1 5 8 4.6 5.0 5 7 5 2 5. I 4.5 5.5 4.9 8.4 

speed (m 5- 1 ) 

Naximurn .... 'ind 16 19 12 12 II 14 II I D 14 14 16 16 

speedt (m 5- 1 ) 

Direction of max. 120 27D 95 255 85 95 255 235 60 305 60 50 

... ·i ndt (deg.) 

/\verage station iOI9 5 1021 .3 1016.0 1012 8 1014 4 IO} 1 . 7 1009.1 1011. 1010 8 1009. 5 10 16.9 1016 3 

pressure (mb) 

Haximum pressuret 10 38 1042 1027 1022 1025 1026 1019 1025 1026 1032 1027 1017 

(mb) 

Minimum pressuret 998 1003 1001 994 1007 994 996 987 1001 982 1009 1015 

(mb) 

Average air -24 -22 9 -25 3 -19 S -8.6 a 3 a 3.0 -I .1 -1 3.8 - 23 . - 23 2 

temperature (OC) 

tlaximum temperaturet - 7 - 7 2 4 13 15 16 5 -I ) - 6 

(0C) 

Nlnimum temperaturet - 38 -45 -42 -33 - 24 -4 -2 - 3 -6 -25 -30 - 34 

("e) 

"':Instrument heigh t s: .... 'ind, 16 m; pressure, 9.5 m (NSL); air and dcwpoint temperature, 3 m. Wind and temperature 

inst ruments are on a l o\,'e r located 2S m northeast of lhe main building . 

t Naximum and minimum values are hourly averages. 

3 . 10. 3 Mauna Loa 

A de scription of the MLO si te and its l oca l climatology ca n be f ound i n 

previous GtlCC Summary Reports . The combined wi nd distribution for 1977 -1 98 1 

in fig. 24 s hows a mu ch hi gher occurrence of wi nd s with a southerly comp one nt 

than does a l arge -scale trajectory ana l ysis . Although the synoptic-scale flow 

pattern is more easterly or westerly, the e ffprt of Mauna Loa Mou ntain is t o 

redirec t stronger winds from al oft down the slope, with a more southe rly component. The departure from symmetry in the distribution of the southe rly 

wind s is t o the south - southwest, the direction of t he s ummit of Mauna Loa. 

Higher wind s peeds 10 m s -1 ) occur most commonly (80% of the time) with 

MA UNA LOA 

82 

IV 

WISO SPEED (II 5) 

_ $' ~ 

r:::::.:J$ 5 WS <IO 

o WSllO s WI~ O fREQ 

!-.lAUNA LOA 

77 - 8\ 

IV 

WI SO SPEED (II SJ 

- $ ~ ' S < ~ 

c.::::::l~"S<IO 

o "'~IO s 

Fi gure 24 . --Wind rose for MLO f or 1982 (l e ft) and 197 7-1981 (right ). See 

l egend for fig . 23 . 

58 
Table 21. --NLO 1982 monthly climate summa ry'" 

J.n Feb M" Apr M.y Jun Jul Au g Sep Oct Nov Dec 

Prevai ling Io.'ind SSW SW SW WSW SSE SSE SSE SSE SSE S SSE SSE 

d i rection 

Ave rage I·d od 4. 7. 4 0 4.6 3 . 3 7 5. 3 4 .4 3.8 3.5 5 3 5. 8 s peed (m s - ') 

tlaximurn I<.' i nd 16 25 14 16 9 11 13 IS IS 10 17 17 

speedt (m s - 1) 

Direc t ion of max. 235 220 185 240 30 200 210 165 ISS 165 205 215 

l.-indt (deg.) 

Ave rage sta tion 679 2 677 6 679 2 680 . 680.9 681. 68 1 .9 682 . I 681. 5 680 .8 680 . 8 681 .3 

pressure (mb) 

rn um pressu ret 683 685 683 684 683 684 685 685 685 683 684 685 

(mb) 

Nin imum pressu rc t 675 669 675 676 678 678 677 680 679 679 676 675 

(mb) 

Average air 4. 4. I 4.0 5.8 7.5 9. 9. I 8 7.8 8.2 8 3 6 

tempera t ure (Oe) 

Naximum tempera t uret IS IS 12 16 18 18 18 16 IS 17 16 18 

(0C) 

Minimum l empe raturet -3 - 3 -2 - I 3 3 0 2 0 

(Oe) 

Precipi tati on (mm) 198 257 317 56 16 16 120 141 35 9 43 34 

"'Ins trument heights: I.'i nd, 10 m; pressure , 3399 m HISL); air and de l<o'Po i nt tempe rature , 2 m. !'h nd . nd tempe ra tu re 

sensors are l ocated app roximately 15 m soulhlo'est of the mai n buildi ng on a towe r. Pressure sensors are l oca t ed in 

the obse rva t o ry bui Iding . 

tNaximum and minimum val ue s are hour ly ave rages . 

stormy periods and are almost exclusively confined to the southerly directions . Of pa rti cular interest is the relative ly large frequen cy of oc currence 

of winds greater than 10 m s-1 from the south-southeast. The upslopedowns lope winds are gene rally repres e nted by speeds of 5 m s-1 or less, con -

ditions which oc cur approximately 62% of the time. Calm conditions (wind 

spe ed <0.5 m S-I ) occur 3% of the time on the basis of the 5-yr average. 

Monthly mean and extreme values for wind, pre ssure, and temperature are given 

in table 21. Precipitation amounts have been added this year. 

The surfa ce wind s at NLO in February we re considerably stronger than 

usual and relatively void of upslope-downslope influence for the entire month. 

Sixty-six percent of the time the wind blew from the southwesterly quadrant 

with speeds in excess of 5 m s-l. For almost 42% of the month, the wind blew 

from the southwesterly direction alone . A peak wind speed of 25 m s-1 from 

220· was repo rted. The lowest pressure in th e last 5 years, 669 mb, was also 

r eported . No rtheasterly winds oc curred less than 10% of the month. 

3. 10.4 Samoa 

6 

The expo s ure of the instrumentation at SMO is considerably different from 

that at the other GNCC stations. Since February 1977, the anemometer has been 

located at a he ight of 14 m on a sampling towe r atop Lauagae Ridge. In this 

location there are no major obstacles to the wind flow from the westerly direction, but the shape of the bluff displaces the wind from easterly directions . 

Temperature is measured at a height of 7 m on the same tower. Oewpoint temperature is measured from air samples drawn from the sampling stack. Station 

pressure is measured in the main building located about 100 m west of the 

sampling tower. On 28 ar h 1982 lightning hit the sampli ng tower causing 

damage to most instruments located on top of the ridge as well as to some in 

the station building. Some sensors could be repaired, but the wind and pressure sensors required replacement. A significant part of the pressure and 

humidity record is missing as a r e sult of this lightning strike . 

59 
S,..,\IO,\ 

82 

111"0 SPEED (liS) 

_ S"' _s ~ 

~ ~~ S 10 

lIS l 10 

'\ 

s 11"1\0 fREQ 

S'\ ~IOA 

77 81 

IV 

"I \0 5P[EO (I( Sj 

_ .lo~ 1fS $ 

!::=l $ " . S ~ ID 

_5 ~ 10 

'\ 

s 11 1\0 rRr.:Q 

----

Fi gure 25 . --Wind rose fo r SMO f or 1982 (l e ft) and 1977- 198 1 (ri ght) . See 

l egend for f i g. 23. 

So ut heasterly wind prevai l ed 66% of t he time in 1982 as comp ared with 61% 

du r ing the prev i ous 5 yea r s (f ig . 25) . No parti cul arly st ro ng evidence exists 

of a si gni f i ca nt wind s hi f t a ssocia t ed wi th t he onse t of the El ~o during 

t he second half of t he yea r. The on l y noticeab l e s hi ft i n t he wind direction 

distribution is a s l ight i n c r pasp in t he percent occu rrence of northeasterly 

winds a t t he expense of northwest e r lies . Typica l ly the northeast erlies occur 

about 8% of t he t ime and northwest erl ies 12%. I n 1982 northeast erlies occurred 

13% and northwesterlies 6%. Seasona l variations of all other meteorological 

Table 22. --SflO 1982 monthly climate s umma r y'" 

--------;:-:-~;:-----;;=--;:c:--_;;::::-___;:_:=____;_c_;_-,._,__-_,_:_:_ --;;--:---c,--- --- Jan Feb Har Apr flay Jun luI ,\ug Sep Oct No v nee 

Prevailing wind 

direction 

Ave r age wind 

speed (m s - I ) 

Maximum I..'i nd 

speedt (m s - I) 

Direction of max. 

windt (deg.) 

I\verage station 

pressure (mb) 

}Iaximum pressuret 

(mb) 

NNE SSE SE Nt~' SE SSE SSE SSE -s"s::,;---Cs"s",;---'s"s",;---'S:':sc:,-

Ninimum pressuret 

(mb) 

3 .5 4 8 4.5 3 2 3 .9 4 4 

II 16 13 9 10 

355 350 345 350 100 Ito 

999 6 998 2 999 6 1000 5 1001. 1001 .6 

1005 1005 1005 1004 1005 1004 

996 990 991 99) 996 99) 

Average air 27 . 5 27.0 27.9 27.8 26 26.8 

temperature (OC) 

Naximum temp eraturet 3 1 31 32 34 31 31 

(0C) 

~linimum temperaturet 23 22 24 23 23 23 

("e) 

~recipitation (mm) 244 357 225 26 203 8) 

4.6 5 3 5 8 5.3 ).9 4 4 

14 12 10 13 13 8 

ISO 165 170 170 1 )0 165 

26.5 25.9 25 26 3 25 6 26 2 

31 29 30 31 28 30 

23 23 22 24 22 24 

77 329 89'-_--"-54 115 91 

':"Ins trument heights: ""ind and de""point temperature, 14 m; pressure, 30 m (HSL); air templ.:rature, 7 m. \.lInd and 

temperature sensors are located atop I.auagae Ridge, a distance 11 0 m northeast of the station. Pressure Sf'nsors 

are l ocaterl i n the station . 

tMaximum and minimum va lues are hourly averages. 

60 
variables are small compared with other GMCC stations (table 22). Only slightly higher winds and cooler temperatures occur in winter than in summer. The 

monthly variation in precipitation was surprisingly large, with April the 

driest month. The winds were unusual as well: the maximum s peed was only 

7 m s-l, and winds greater than 5 m s-1 occurred only 5% of the time as compared with an expected frequency of 40% based on the previous 5 years . 

3 .10.5 South Pole 

Figure 26 displays, in polar coordinates, the distribution of the wind as 

a function of speed and direction. The most prevalent direc tion on 1982 was 

north-northeasterly as in previous years. For the second successive year l a 

marked increase was observed in the percentage of stronger winds (~10 m s 1) 

I SOUTH POLE 

62 

IV 

1'1 so SPEED (Il 51 

_ ~~ I' S 

r:=::l S Ii '-9 < 10 

CJ S~10 

\ 

s 1'1 SO rR~ 

c 

SOUTH POLE 

77 61 

IV 

WI so SP!:£D (It S) 

$li ~ 

c:::::J$~ LO 

0 · 9110 s 1'1\0 fREQ 

Figure 26.--Wind rose for SPO for 1982 (left) and 1977-1981 (right). See 

legend for fig. 23. 

that are predominantly from the north. During the previous 5 years, wind 

speeds 10 m s-' occurred 3% of the time. In 1982 wind speeds ~10 m s-1 occurred 7% of the time. Calm conditions (wind speeds <0 .5 m s-l) occurred 

<0.1% of the time. 

The full extent of the austral winter on the Antarctic plateau is shown 

in the eight monthly average air temperatures that are below the annual average of -49.2°C (see table 23). The maximum hourly average temperature in 1982 

was -18. 3°C (DOY 001) and the minimum temperature was -82 .5°C (DOY 173). This 

was a new record low temperature for SPO . 

61 
Table 23 .--SPO 1982 monthly climate summary'-' 

Jan Feb a r Apr ily Joe Jul Aug Sep On Nov Dec 

Preva iling ... ·ind E £};1: ENE , Nt: , ).,'NE KE /';'},'E N N NNE 

di rceLlon 

.-\verage Io.'ind 4 2 4 6 5 2 6 2 6. 6 0 7.5 6.5 6.0 8 3 6.9 4 5 

speed (m 5- 1) 

~Ia)(imum ' • .-ind 10 7 9 10 13 " 16 12 12 17 17 9 

speed-;- (m s' I) 

Direction of max. J50 345 320 20 20 5 290 325 320 325 30 100 

lOindt (deg.) 

,\ve rage stalion 686 5 680 4 670 5 672 6 672 6 668 5 674 . 669 2 667.0 673. 683.8 690 . 

pressure (mb) 

laximum pressure+ 694 691 687 691 685 688 690 679 681 690 696 700 

(mb) 

~lin imum pr('ssuret 673 672 655 651 655 645 658 651 655 655 668 677 

(mb) 

Average air - 26 8 - 39.9 - 54.0 - 54. - 56 4 -60 3 - 57 . 9 -61 •• - 61 .4 -49 6 - 37 6 -30 3 

temperature (·C) 

~laximum temper.1lUre+ - 18 - 22 -38 - 34 - 38 - 39 - 34 - 38 -35 - 30 - 29 - 20 

(0e) 

~linimum tt>mper.lluret -33 - 55 -68 - 75 - 77 - 83 - 73 - 75 -77 - 64 - 46 - 37 

(0C) 

·· .. Instrument heights: .... ·ind, 10 m; pressure, 2850 m UISL) ; air temperature, 2 m. The anemometer and thermometer arc 

located on it mast 30 m grid north of CAf. Pressure measurements arc made ins i de CAF. t~lax imum and minimum values are hourly .werages . 

3. 11 Precipitation Chemistry 

The precipitation chemistry program co ntinu ed with little change during 

1982 at the 10 regional and 2 baseline NADP sites (see table 24). The sites 

located at Bishop, Calif., and Pendleton, Oreg., closed in July. Snow samples 

were analyze tl fur BRIV antl SPO, and special studies continued at rlLO using the 

ion chromatograph. The IVashington, D.C., network continued to operate with 

six observers . 

3 . 11 . 1 Baseline leasur nts 

The five-site special network on the islafld of Hawaii and a sixth site on 

Kauai continued to operate on a daily or biweekly schedule . Site locations 

were discussed in previ ous GMCC Summary Reports. As seen in fig. 27, the 

Table 24.--Annual weighted-avera ge ion concentrati on (~eq Q-') at 

NADP regional a nd baseline sites from January to December 1982 

\;110 5i te H+ S04= ~0 Cl 

Alamosa, Co l o . 2 .21 26. 1~ 14.23 3 81 

Bishop, alif. '~ 2 .36 12 .79 6.53 1 .i7 

Caribou, ~aine 18. 97 21. 76 9.16 2 .61 

Huron. S. Dak. 3 .25 27.64 21.89 2 .94 

:1eridian, ~is~ . ~C. 78 36.94 12.93 10. 43 

Pendleton, Oreg. .. 1.46 17 .05 9.14 4. 76 

Washington Crossing. ~.J. 42. 11 53 . 43 22.21 7. 75 

Ral e igh, ;..r.C. 36 . 06 37.49 15 .77 5 . 74 

Salem, Ill. 36 .57 47. 03 17 . 2 7 4 50 

~;icto ria , Tex. 8 .5 9 21. 84 8.51 19 .30 

('Ito;' 4 .32 5. 16 .15 1 .38 

S'IOt ) . 27 27 .30 (6.0b)' O. !.O 15 i 86 (3 .20 )§ 

'C l o sed Ju ly 1982; values as~d on January -June data. 

-;- Baseline site 

§Yalues 1n parentheses represent the non-seasalt contnbut1011. 

62 
70 70 

MLO KUlAN I MAUKA 60 ' .2 

60f 

4 .2 

" " ~ 40 .. :j 4 .' 

: · · , . 30 . , < < 

20 .., j 2, 

4.1 

10 5.' 10· 5.' 

• • •• • ••• " A " A S 0 N 0 M A M A S 0 N 0 

70 70 

1.

2 

22 MI IIALAI Hill 60 .2 60t 

" "r ... ... 4 .' 

• < · · , 

"I . 

= 1 '.1 :1 

20 r 

~j~/\ 4.1 

'J ~~ 5.' '] .. • F M A M A 5 0 N 0 • •• F M A M A S • •• 0 N 0 

70 70 

KAUAI KU~IUKAHI 60 '.2 .. ' .2 

" ,. ... • •• ~ 40 4.' 

. ,.I . , . • ~ 30 < 

20[ 

< '--- ~ t, ' .1 20 

.0. 5.' '1 ~~ 5.' 

6.0 ••• F " A .. A S 0 N D F .. A .. J A S 0 N 0 

Figure 27 . -- ~Ionthly precipitation weig¥ted means for six sites on the islands 

of Hawaii and Kauai during 1982 (+ = H ; n = S04-)' The sites in order of 

increasing elevation are Kumukahi, Kauai, Halai Hill , 22 ~Ii , Kulani Nauka, and 

tILO. 

acidity increase with elevation is still quite evident, as in past years. An 

opposite trend, a decrease of sulfate with increasing elevation, is also evident. Removal of the seawater sulfate comp onent (not shown), howeve r, gives 

sulfate concentrations comparable with those observed at NLO. Agreement at 

Halai and Kauai, two sites with approximately the same elevation a nd orienta -

tion to the trade winds, is not as good as in past years. 

tlonthly weighted hydrogen ion and sulfa te values for tlLO and StlO NADP 

sites are shown in fig. 28 . Annual weighted means are s hown in table 24 where 

the values in parentheses for SNO were adjusted using Na to remove the sea salt 

c 0nt ri hut.ion. Snow samp le da ta for BRW and SPO are shown in fig. 29. 

63 
. 

, 

BO60-

20' 

'" 

'0 

,,-

20-

S ALEM 

I 

I 

;-

~ 

CARIBOU 

, 

/ 

/ 

F M A 1>1 

, 

, 

\ 

/. 

II - 4.2 

I 

J \ A s o N () 

r .. , 

'.2 60 ~~~~~~~~~~~~~~~ ~~ 

ALA~IOSA 

'.7 J ... 

'.7 

A SON D M A M A SON D 

Figure 28.--Monthly precipitation ,eighted m~ans for five regi onal and baseline NADP sites during 1982 (+ = H ; 6 = 504-)' 

3.11.2 Regional Measurements 

Annual weighted ion means for the 10 NADP regional sites are shown in 

table 24 . Selected monthly weighted hydroge n ion and sulfate means are s hown 

in fig. 28. A more extensive analysis has been compl eted for the Caribou, 

Maine, site; figs. 30 and 31 indicate the amount and quality of data available . Changes in quality assurance, quality control, and collec tion protocol 

since 1980 ha ve increased the reproducibility of the data. 

3 .11 . 3 Washington, D.C . , Netwo rk 

The data for the Washington, D.C., network are s hown i n fig. 32. 

BARROW SOUTH POLE 

,,, 

[" 

Figure 29 . --Snow sample ion concentrations for BRW and SPO during 1982. 

64 
T 

0 0.,,'· 

' : 

J '0 ;/' / ------------- Figure 30.--Hon t h ly precipitation 

weighted means f or Caribou, Ia ine, 

f or 1980 -1 982 . 

1 

., , , 

"r J',U :;'l.1~ t .. n. 

~~ [3 . ' ., 

'r 

or 

'.i- /0 

'r 

• 

" 

06 .. '" " .. .. W • .1 " " " 10.., It 

Figure 31.--Annual precipitation 

weighted means for Caribou , Maine, 

over the existing data record. 

Figure 32.--Honthly precipitation 

weighted hydrogen ion concentration 

for the Ivashington, D.C., area . The 

cente r bars highlight the summer 

data . Each annual mean i s noted at 

the top of its co lumn. 

3 .1 2 Data Hanagement 

3. 12. 1 I CDAS 

For over 6 ye a rs the A&DH group has oversee n the a utoma ti c co llection of 

continuous data by ICDAS at the f our GHCC observa t ories . This mini computer 

system records meteorological, aerosol, CO 2 , 03 , and solar radiation data on 

magn etic tape in the form of minute voltages and hourly sca l ed values . The 

ove rall performan ce of ICDAS was good agai n this year with a 95% average data 

recovery fo r the four stations. The breakdown by station during 1982 is 99% 

at SPO, 97% at SHO, 96% at HLO, and 88% at BRW. ICDAS performance statistics 

by st ation and ye ar fo r 1977- 19 82 are s hown in fig . 33 . If 19 77 is discarded 

for HLO, whe n the station was rebuilt, ICDAS has operated over the entire 

period for 97% of the time at SPO, 95% at SHO , 97% at HLO, a nd 92% at BRW. 

3.12.2 Redu c tion Facility 

Successful data transfer from th e GHCC stations to the CDC 750 computer 

in Boulder req uires a comp l ete rewriting of the data tapes. This is performed 

in the GMCC reduc tion laboratory. In 1981 both the hardware and software used 

for rewriting we re upgraded. A faster NOVA 4 "'ith a hard"'are multiply-divide 

function and a Winchester disk were installed . The larger disk allowed the 

use of the Data General RDOS . All software used for processing was converted 

to FORTRAN . This system operated without extensive downtime in 1982 . By the 

end of the year 30% of the disk was used for permanent software files. 

65 
Figure 33.--ICDAS performan ce statisti cs by station and year for 

1977 -1982. 

The DECtape II (TV-58) cartridge drive was used throughout the year t o 

ex tra ct special sola r radiation measu rements recorded at tILO. Tape -reading 

problems occurred and in most cases were traced t o fau lty hardware. In only 

one case was a tape failu re detected. This project will continue into 1983 . 

Al l TV-58 cartridges recorded on IICMIS boxes wi ll be processed through th is 

syst em. Software is being prepared to print su~nary reports of the tapes and 

to make backup recordings of the contents on larger tape reels . This software 

wi ll be completed well in advance of the deployment of IICMIS. 

3 .12. 3 IICAMS Development a nd Testing 

Significant adva nces wprp marlp in the development and testing of IICA , 

which will replace ICDAS i n 1984 . Component testing was given t op priority, 

and for the most part the final complemen t of subcomponents was eva luated. A 

prototype data logger was constru c t ed and installed at MLO to record signals 

from a set of sola r radi ation senso r s . The performance of this system was 

satisfactory in mo st respects . Discussions wi th sta tion staff and project 

leaders indicated that a printer would be a necessa r y part of eac h system. 

Thus, access to a common printer will be provided f or each IICMIS dat a re -

corder. 

The config urati on of IICMIS i nclude s a CPV (MDX-CPV)), programmable memo ry (MDX - VMC), battery-powered memory (MDX-BRAM) , se ri al input- output boards 

(MDX-S10 2) , a ba ttery-powe r ed c l oc k (MDX-BCLK), and a di gi t al input-output 

board (MDX-DI0Bl). The boards and the card cage in whic h they reside (MD -

CCI2) are manufactured by Moste k, Inc. Sensor vo ltages are a cquired with an 

a nalog-to-di gita l converter (Data Tran slation DT 2742). The clock and random 

access memory are battery powered and are maintaine d f or 5 days or more . The 

software resides in PROM so that the system will restart automatically after a 

power failure. Data are recorded on preformatted cartridge tap es (DEC, 

TV-58) . Operation control is provided by a se t of function switches and a 

nume ric pad in a modular fr ont panel terminal (Burr-Brown, TtI-76). An Epson 

MX80FT printer will be used to print results . All comp onents except the 

printer reside in an enclosure built in-house. 

Specifications were prepared for the IICMIS CO 2 software after a series 

of me e tings and discussions with the CO 2 staff . This is a complex pac kage and 

a significant amount of testing will be necessa ry. Specifications [or a n 

lI eN-IS that "'ill r ecord the so l ar radia tion, ae rosol , sllrface ozone, a nrl meteo rologi ca l si gna ls will be prepared ea rl y in 1983 . Software wi ll be wr iLLe n 

66 
in the summer of 1983, and testing will follow in the fall . Installation will 

be done station by station beginning in 1984. The plan calls for the construction of 24 IICAMS units to replace ICDAS at the four GMCC stations. 

3 . 12.4 Archiving 

The mag netic data tapes listed in table 25 were added to the inventory of 

GMCC data archived at \,1J)C-A in Asheville, N.C. There are now 34 G~ICC data 

tapes in the archive . A list of the data archived prior to 1982 can be found 

in the GMCC Summary Report, No. 10 (Bodhaine and Harris, 1982, p. 70). 

Copies of the tapes can be obtained from User Services Branch, £/CC423, 

National Climatic Center, Asheville, NC 28801 (FTS 672-0682 or 704-258-2850, 

ext. 682) . Planned new numbers are 672-6682 and 704-257-6682. GMCC archive 

tapes are located in tape deck no. 9708. GMCC also archived all available 

1979 CO 2 flask data from stalions in the CO2 flask network (NESDIS, 1983). 

Table 25. --G~ICC data tapes sent to WDC-A in 1982 

Tape Date of Period 

name issue Pa rameter Station of da ta 

A82225 8/16/ 82 Solar irradiance BR\4 1981 

(Research Cooperator format) 

A82226 8/16/82 Sol~r irradiance tlLO 1981 

(Research Cooperator format) 

A82227 8/16/82 Solar irradiance SMO 1981 

(Research Cooperator format) 

A82228 8/ 16/82 Solar irradjance SPO 1981 

(Research Cooperator format) 

3.13 Atmospheric Trajectories 

3.13.1 Introduction 

Development of the GMCC atmospheric trajectory program continued in 1982. 

There are no,,' three versi.ons of the program. The first, called GMIBITI, has 

been operational for well over a year. GAMBIT1, originally developed from the 

ARL trajectory model (Heffter and Taylor, 1975), produces backward isobari c 

trajectories for the Northern Hemisphere. Analyzed u and v willds for the 

Northern Hemisphere are tI,e primary input. The wind data are produced by 

mlC's operational model and are suppl ied t o cncc by NCAR. A complete des c ription of Lhis version of lh~ trajecLory program as well as examples of output 

plots were presented by lIarris (1982) dlld Bodhaille and Ha rris (1982, Pl'. 71-

74 ) . 

The se c ond version, GA~IBIT2, is simiJar to the firsl, excepL it can produce trajectories for the elilire globe. The input dala are in the form of u 

67 
Table 26. --Description of mlc data purchased from NCAR 

Dates 

Parameters 

Levels 

Program 

Northern Hemisphere 

65 x 65 grids 

1975-Aug 1982 

u, v , z, T 

1000-100 mb (mandatory 

levels) 

GAI'!BITl, GAl'lBIT3 

2 .5 0 global grids 

1977, 1979, 1980 

u ,v,z ,T 

1000-100 mb (mandatory 

levels) 

GAl'lBIT2 

and v analyzed wi nd s for every 2.5 0 of latitude and longitude. The program 

can operate in three modes : (1) Northern Hemisp here only, (2) Southern Hemisp here only, or (3) both hemispheres. In the last mode, grids from the Northern Hemisphere a nd the Southern Hem isphere data tapes are spliced together 

al l owing the compu tation of cross- equatorial trajectories. This program produced the SNO trajectories used in the case study in sec . 3. 13 . 3. A disadvantage of GANBIT2 is t he added comput er costs inc urred when dea ling with the 

larger global data set . 

The third version of the trajectory program, GAtIBIT3 , produces i sentropi c 

trajectories that trace paths determined by the wind field on surfaces of con -

s tant potential temperature. Detai.ls of t he computati onal method for GAl'IBIT3 

and a case study are i n sec . 3.13.4. 

Table 26 gives a description of t he NNC data , purchased from 

se rve as input for the three versi ons of the trajectory program . 

years ha ve been ordered and should be obtained this year . 

NCAR, that 

The missing 

The quality of the 1982 data set decreased dramatically over previous 

years because of the amount of dat a missi ng. Following are the breaks in the 

1982 da t a up to 31 August : 

12-1 9 Jan 

22 - 26 Feb 

03-11 Jul 

27-31 Jul 

09-16 Aug 

Breaks create a problem because trajectories ca nnot be comput ed f or times when 

there are no data. Also, breaks prevent the program from being run in its 

most efficient mode; i.e., instead of computi ng trajectories for an entire 

month, the program mu st start or stop at breaks . 

Next year the possibility of a more direct link to the data will be investigated . If found, this could prevent excessive loss of da ta and wo uld 

give more rapid access to the data . When the data are obtained through NCAR 

t here is a t least a 6-mo delay. 

3 .1 3 . 2 GANBITl 

Last year as part of the process of valida ting GAl'IBIT1, two spec ial products were developed. An example of the first is given in fig. 34 , which s hows 

a plot of the gridded wi nd s used as input to the trajectory program . Here the 

68 
NMC CRID WINDS FOR 700 MB n" 19 OZ 

Figure 34 .--NNC grid winds for 

19 April 197 7 at 0000 Z in the region around Bermuda. The direction 

of the main vec t ors is the same as 

wind direction (i.e . , wind flowing 

toward s dots). Wind speed is proportional to the l ength of the main 

vectors , 

winds are plotted on a map as vec t ors pointing in the direction of the wind 

and proportional in l ength t o the wind speed. Since t hese vectors show a 

" snapshot" of the wind at one time (in this case for 19 April 1977 at 0000 Z) 

and traj ec tories trace air flow over a finite period of time, the traj ectories 

were checked by examin ing wind speeds and directions from a series of wind 

vector plots. This validation procedure, though somewhat inexact, gave further evidence of the reliabiliLy of the GA1'IBIT I program . 

Figures 35 and 36 s how trajectori es arrivi ng at nine desti nati ons in the 

HLO region. This second type of specia l plot s hows how trajectories are afrected ~y a . ,"all change in destination. The nine destinations, spaced )0 

apart, form a cross with HLO i n the ce nter . Figur e 35 shows remarkable agreement among the nine independently computed traje ct o ri es , suggesting that the 

wind field was fairly homogeneous at 500 mb on 1 Hay 1979 . Several days earlier on 25 April (fig. 36) , a 3° difference in the destination made a significa nt differe nce in the airflow pattern . The relationships among these trajectories are consist ent with a ridge bei ng present to the north of Hawaii on 

this day . The progression from south and west to north and east results in a 

continuousl y larger deformation of the trajectories to the north. 

.' 

- "'. 

l>D' [ • 

~ .Iot8 TRAJEX"I'ORIC;: ARR I\I \ G 79121 5 1 79 AT OZ 

, 

r 

.,' [ 

",' ,, -

.J " ,~, 

.', 

, ', 

~ '\ 

" 

.', 

~-

,,~', 

.', ,i!j" 

Figure 35 .--Trajectories arriving 

at nine destinations near Hawaii on 

1 Hay 1979 at the 500- mb level. 

69 

!IOO liB TRAJ!X'TORI~ ARRI\I \ C 79115 ~ l'> 79 IT fTl 

" 

.', 

.J 

,', 

.~" > '. , 

'>D' [ • .liO', 

,,,,', ,,,,' , ,, ', '0" ,.,' [ 

Figure 36.--Trajectories arrivlng 

at nine desti nations near Hawaii on 

25 April 1979 at the 500-mb level. 
3. 13.3 GAI'IBIT2 

This year the global trajectory mod el, GAI'IBIT2, produ ced G~IC C's first 

trajectories for SHOo Trajectories for 1977 at the 1000- and 850 -mb l evels 

were compu ted in the dual-hemisphere mode so that airfl ow from SHO co uld be 

traced across the Equator from the Northern Hemisphere if necessary . The case 

study presented here is for Har ch 1977 . During the first part of the mon th, 

air flowed to StlO from the ea st (fig . 37). The predominant sou theasterl y 

trade winds at SHO res ult from counterclockwise flow around the So uth Pacific 

s ubtropi cal hi gh. Figure 38 is an exampl e of trajectories during the middl e 

of Harch when a tra nsition from easterly to westerly winds occurred . At this 

time some of the 10-day trajectories to SHO originated in t he Northern Hemisphere . The NHC s urface map for 17 Harch (fi g . 39) shows tropica l storm 

Norman to the west of SHO o During the l ast part of Harch west erly winds 

driven c l ockwise around this storm are see n in the trajectories in f ig. 40. 

"' ~ ...... U1O~L&" . ... "'" noooo > n 

~ on H)OO WI "n 1000 "' 

•. , ~ _____ ---':':':.:':~:::: "_:.' .::n.:~:.:.=- . ______ -, 

,. 

•. , 

"J' E 100' • 1100" ' 0' • 

Figure 37 .-- SHO trajectories arriving on 1 Harch 1977 at the 1000- and 

850 -mb l evels. 

3 . 13 .4 GAMBIT3 

r IUI"""W. 

~,~--------.:.:~~~'= .=-="~------, 

,. 

. .. 

'00' E tOO' • tOO' • " 0" 

Figure 38 .--StlO trajectories arriving on 17 Har ch 1977 at the 1000-

and 850-mb l eve l s. 

In an attempt to improve the accuracy of t he trajecto ries , a procedure 

for computing ki nemati c trajectories on isentropic surfaces , GAHBIT3 , was 

developed. Testing and comparison with the is obaric mod el continues. Becaus e 

of its added complexity and cost of operation, GAHBIT3 is r un on a ca se-study 

basis. Some prel im inary results are presented below. 

The computational method was determined i n part by limitations on computer memory and costs . Rat her than dynamic isentropic traj ecto ri es , the 

model produces simpl er kinematic traj ec tories, but even these require a mult i -

s tep process involving mor e than a half dozen programs. The first st e p is to 

choose a potential temperature (8 ) for the isentropi c surface on which tra -

jectories will be constructed. This is accompl is hed by compu ti ng 8 from ra -

winsonde da ta at or ne ar the desired trajectory destination, or from analyzed 

gridded data. Once the desired 8 is determined, a seri es of 8 surfaces are 

computed on an ap propriate subgrid of the NtlC 65 x 65 Northern Hemis phere 

grid. One s uch 8 surface is shown in fig. 41 over the subgrid us ed for HLO . 

Note t he characteristic rise of the isentropic s urface toward the pole. Plots 

70 
Fi gure 39 . --NNe surface analysis for 17 arc h 1977 . SNO is marked 

*' 

of i se ntropic surfaces are used to det e rmine the app roximate heights of the 

surfaces at the de stina t ion. In this case t he he ight of the surface at e = 

310 K (the 310-K surface) is about 3 km a t NLO. If the e value chosen is too 

l ow , these pl ots wo uld s how that the surface is not defined at MLO . In the 

latter case , the isentropic surface would intersec t the earth before reaching 

NLO, indicating tha t air arriving there did not travel along that surface . To 

be examined is the possibility that there are day-to-day variations in e large 

enough that wo ul d require frequen t adju stments t o the e surface bri ngi ng ajr 

t o the station . In the examples presented her e e = 310 K was close to the 

700 -mb level and 0 = 32S K was c l ose to the SOO-mb l evel at NLO . 

•. ,,-------_._--------, 

,...,ftA.r'"""' .... ""'~'...,." ,it> .... • ",,,,(,,,. , r ,n , 000 o • 

.... _u 0'''' ...... 

o· 

.', 

'00· • , . ' , ,,,,,", ,d ' 

71 

Figur e 40.--SNO trajectories arriving on 22 Nar ch 1977 at the 1000-

and 8S0-mb levels. 
6 

S 

4 

:; 

2 

o 

Figure 41.--The 310-K isentropic surface for 25 April 1979 at 0000 Z overlaying the NLO subgrid of the NNe Northern Hemisphere 65 x 65 grid. 

Given t he desired potential temperature B., the program that computes the 

isentropic surface uses Duquet's (1964) ethod~ described also in Haa genson 

and Shapiro (1979), to transform the data from mlc standard levels to the B 

s urface . Input data for this program are temperature, height, and u and v 

wind components reported at nine levels (850, 700, 500, 400, 300, 250, 200, 

150, and 100 mb). On a gridpoint-by-gridpoint basis, the two pressure l evels, 

i and i+l, that bracket B. are found. Assuming that temperature varies linearly as pK, then J 

where 

B = 

K B. (T. - B P. ) 

T. = J 1 1 

J B. - B 1000K 

J 

Ti +1 - T. 

1 R 

K = K K c 

Pi+1 P. P 1 

..,. 0.286; 

R is the gas constant; and c is the specific heat of air at constant pressure. p 

72 
Knowing T

j and 8

j , and from the definition of 8, 

JOOO 

Pj= ' 

Wind is assumed to vary linearly with height. 

u and v on the 8. s urfa ce, z. must be found by J J 

equation from the lower pressure level: 

Before interpolating to find 

integrating the hydrostatic 

c [(T.n. - T.n.) n. 

z. = z. + -.I'. _=,1 "'1'---_----rn",I.--=1- J 1 g n. 

In 1 rr 

J 

+ T. 1 

J 1 

( P )K where g is the acceleration of gravity, and n =, 1000 . 

(1) 

Once T, P, z, u, and v are determined for each grid point on the chosen 

isentropic surface, the data are recorded on magnetic tape and the same computations are performed on data reported for 12 hours later. This process 

continues until a sufficient number of isentropic grids are available for the 

computation of trajectories. GAMBIT3 is similar to GANBITl (Harris, 1982) except that the input wind data are on isentropic rather than isobaric s urface s. 

Th e other parameters, T, P, and z, are not used in determining the trajectories but are reported along with the trajectory segment endpoints as additional information characterizing the history of the air ma sses . Figur e 42 

sho,,'s how the isentropic trajectories are displayed on a map. A symbol (an 

identifying letter or numeral) marks every 12 hours along the trajectory. The 

numera l s show days of travel to the desti nation. Table 27 is an examp le of 

the additional information that accompanies the plotted trajectories . The 

isentropic trajectories in fig . 42 are compared with the isobaric trajectories 

for the same day (fig . 43) when this case is discuss ed in detail later. 

Additional study is needed to determine the validity of the GANBIT3 pro -

cedure . The greatest weaknesses are probably those related to the i nput data. 

For example, as is true for the isobaric procedures, real data coverage over 

much of the ocean and polar regions is sparse . Both the isentropic and isobari c procedures are also limited by the coa rse mes h of the NNC Northern Hemisphere grid, about 200 km per grid unit at the Equator to 400 km per grid unit 

at the pole. Further inaccuracies may be introduced into the isentropic trajectories by t he fact that, although significant levels are used i n the computation of heights by NNC, only the mandatory levels are provided. Thus, the 

hydrostatic equation may at times be inconsistent when us ed between mandatory 

levels as in ( 1) . 

A comparison between isentropic and isobaric trajectories for NLO during 

April and ay 1979 yielded some interesting results. Figure 44 shows 310 -K 

is entropic trajectories that are comparable with the 700-mb isobaric trajectories in fig. 45. Good agreement was also found between the 325-K isentropic 

traj ectories in fig. 46 and t he 500-mb isobaric trajectories in fig . 47. In 

cases like these, where good agreement is found, wind flow is approximately 

zonal so that height and pressure of the isentropic surface do not change 

significantly . The trajectories in fig . 42 arriving at HLO on the 310-K surface show better agreement with the 500- rather than the 700-mb trajectories 

in fig . 43, even though the 310-K trajectories arrive at HLO near the 700-mb 

73 
\ 

---~ .. ,oo". 

Figure 42.--MLO t r ajectories arriving on 25 April 1979 on the 310 -K 

isentropic surface . 

, ..... 

..... ....... E1tIO I • .all .. ,"" .... ,. " . , .", 

.. .. >0:0 ... ~ .. >0:0 ... " .. ...,w. 

.', 

wi. 11/ , wi . .... ~' . , ... 

Figure 43.--MLO t r ajectories arriving on 25 April 1979 at the 700- and 

500-mb levels. 

Table 27.--Location , pressure, temperature, and height of the air mass 

at 12- h intervals along the isentropic t ra j ectories s hown in fig. 42 

" L.O H • 25 0 11 o.~ 

Nn. "RS ~'C" L. AT I TLJO~ LONGITUO~ PRESSURE TEMPERATURE H!lGNT 

0 tq:~1 _155;5~ 70.;2 281;0 2 .. b : 12 21 ... 6' _)5b.81 b64 .. 5 215.8 151 •• Z. 2S.1n _tS8 .. 22 b1Q.l 270.1 40b2. 

36 10.~6 -157.~6 511.5 Z"" .. ct ~60b. 

~8 15.IS .155.7~ 521~7 251,1 H07, 

60 31.LtI§ .11§2. q , .QOb.G 253.7 5n2. 1~ 38.00 _150&86 560.4 262.7 4856. 8~ 40.~8 _lSO.OIli 511. a 2"4., 4733, o. "3.74 .14'.76 522.0 251.~ 5~11. 

108 40.61 _143.~n ~n.o 250.2 6 tie. 

120 5b.04 .143 .. '0 463,2 2Q8.~ b21Q. i 12 '.57.6~ .1Sq.31 "57,0 2 a1.1 613 4 ; 

144 45.~7 17Q.Q, 50S.4 255.0 SlH, 

IS6 38&12 16b.'''' 54b;3 2bO.S UlO. 

168 3':.4~ 1.0.2~ a~5.8 252.0 51H. 

180 41.,o~ 121:00 ql~ O lal;1 bU1. 

102 lIb.4t I 12 . 8. 3U.0 H2.5 11H. ~oa 50:bl Q,:oa 361.0 HI: I HH. 

"L.a 70 a 25 12 310.0 

NO. "RS 8ACK L ATITUo~ LONGITLJOf PRESSURE TEMPERATURE MEU"! 

n tQ:'51 _155;58 b19:2 211;5 lJ!3, 

IZ 21.,-A _155.oS b0 2." no.o 320 I, 24 2°.24 _156.1. &40,2 212." 181,. 36 ZS.~b _153 •• , 518.0 25.,6 5101. ae ~2.'--; .1 0q .,1' 518, I 2560. 5316. 

60 36,5! .146.=,30 SIO , I Z56~. 5aH. 

12 42.:\7 .t U2.3b 410 .. 0 240.0 7n81, 

H 48.02 _130.18 103,. 231.4 n.8. 

Ob 1)6.15n .t24.4'7' 360 .0 ZlI,4 100b. 

lOS &l.~l -118.50 UOI.4 238.1' 11 .Z. 

'ZO 5q.,~ .1';Q.,Q4 400~Q 210,1 6.12 • 132 45.,11 .I't~~~ 102.8 211. I HU. 

14. 3A.Ii~ l'7a'~ • 76,5 250,6 5.6S • 156 36 .. 1)'- lb~ .. 4" 'il'.5.Cil 2~6.4 5]74. 

IbS 37 .. 16 1ll e.Ot a65.7 20Q .. O &001. 

ISO Ql.D' 128.7q 424,3 24Z." &7&1. 

I·Z a!i.2~ 114 .. 0e 40'7,6 2]0,5 7071 • 104 51.1. .S.85 3&a.0 n2.Z 1188. 

74 
Figure 44.--HLO trajectories arriving on 12 April 1979 on the 310-K 

isentropic surface. 

. I . . ... 

,,' ',;;; 

W1D .....,"""'..,. .uN'_' ''',," . • " '" 

c,"'_u 

p .n _'" 

~--':!,A!:~ \~ .. 

, .. '. -~,;; •. --,~ •. --=,c.: . ,--;;'."" 

, .... 

Figure 45.--HLO trajectories arriving on 12 April 1979 at the 700- and 

500 -mb l evels . 

pressure surface (see table 27). Within 2 days back a l ong the trajectories 

shown in fig. 42, the northerly tracks locate the air ma sses higher up the 

isentropic "mountain" shown in fig. 41, approaching the 500-mb level. At its 

most northern location, track B (1200 Z) is close to 8 km in height (360 mb). 

Earlier in their journey to HLO (6-7 days back) both trajectories are farther 

south, henc e at lower elevations. Poor agreeme nt wa s found be tween isentropic 

and isobaric trajectories when, as in this case, wind flow was north and 

south, or when winds were light and variable. 

In the future, case studies comparing isentropic with isobaric trajectories may r eveal more conditions of agreement. Under favorable conditions isobaric trajectories may then be judged adequate, whereas the isentropic model 

could be used for case studies where isobaric results are uncertain. The 

benefits and practicality of a dynamic rather than kinematic isentropic model 

will be investigated next year. When opportunities arise, GHCC trajectories 

will be compared with those of other organizations. Verification with rea l 

wind observations will be attempted whenever possible. 

. ', 

. ', 

( 

! 10"·1 

. .,,-- - ~ 

. , 

, 

~ . > • 

-;~ . 

Figure 46.--HLO trajectories arriving on 2 Hay 1979 on the 325 -K isentropic surface . 

75 

• • __ I 

~'. 

Figure 47.--HLO trajectories arriving on 2 Hay 1979 at the 700- and 

500-mb levels . 
4. SPECIAL PROJECTS 

4.1 CO 2 Modeling 

4.1.1 Introduction 

This section is a progress report on the development of a COz model designed to interact with data from the GMCC COz flask and continuous sampling 

program. Large-scale features of the COz data can imply physical mechanisms 

to be included in the global carbon cycle model. Discrepancies between modelcalculated COz va lues and the data may point to problems with flask sampling 

or the model. 

The model is an adaptation of Machta's (1974) two-dimensional global 

diffusion model. It simulates transport of atmospheric COz vertically and 

latitudinally; COz flux into, out of, and within the ocean; and transport of 

COz into and out of the biosphere. Output of the model is atmospheric COz 

concentration as a function of latitude, altitude, and time. Rotty's (1982) 

values for anthropogenic CO 2 release are used and an ocean simulation having a 

mixed layer and a thermocline layer is included . Data for oceanic alkalinity, 

salinity, and total dissolved inorganic carbon were obtained from Takahashi et 

al. (1981). Partial pressure of COz (pCO z ) was calculated by assuming that 

alkalinity remains constant and by solving the alkalinity and total absorbed 

inorganic carbon equations . Figure 48 shows pCOz vs. time and latitude. 

A model by Kerman (1980) expressing COz flux as a function of difference 

of pCO z in ocean water and volume mixing ratio of COz in air, of wind friction 

velocity, and of temperature was used to simulate the air-sea exchange of COz. 

The flux of COz can also be expressed as a speed or "piston velocity" times 

- J ". , o 

-0 

Figure 48 . --Partial pressure of COz 

dissolved in the mixed layer of the 

ocean as a function of latitude and 

DOY . 

76 

Figure 49.--Piston velocities for 

COz air-sea exchange as a function 

of latitude and DOY. 
the concentration difference; that expression is used here (fig . 49). 

velocities are in reasonable agreement wi th the values of Peng et al. 

These 

(1979). 

Work is continuing with E. Box of t he University of Georgia on a model of 

the biospheric fluxes of CO 2 , The net flux (NEP) for a given latitude band 

( lat) and time (T) is expressed by 

NEP(lat ,T) = NPP(l at ) [R( lat,T) - U(lat ,T)] , 

where NPP is net primary productivity, and R (release) and U ( uptake) are the 

fractions of the carbon liberated fr om and taken into the biosph e re, respec -

tively, as a f un ction of time . The NPP va lues were taken from Box's data by 

R. Sc hne ll (personal communication; NOAA/GtICC; 1982) a l ong with the values for 

seasonal fract ional upt a ke of CO 2 by phot osynth esi s. The rel ease fractions 

were obtai ned by fitting the model to th e data. Later, Box ' s dec ay values 

will be used to give these numbers. Fractional ice cover of the ocea n was 

calculated by averaging sea -i ce data for 5 years from the World Data Ce n ter. 

The average ice fraction vs . DOY a nd l atitud e is shown in fig. 50. 

4.1.2 Results 

A three -dimens iona l de pi ction of mode l r esu lts is s hown in fig. 5 1. In 

general, the model accurate l y reproduces l arge - sca le features of atmosphe ri c 

CO 2 change with time and latitude. Figur e 52 shows a map of mea n a nd RHS 

differences between the model CO 2 concentrations a nd those of the flask sampling network. The mea n differences reflect agreement i n predi c tion of the 

annua l mea n CO 2 value , whereas t hp R~IS differences reflect agreement in the 

Figure 50 .--Frac tion of sea surface 

covered by i ce as a function of 

latitude and DOY. 

77 

Figure 51 . Hodel prediction of the 

concentration of atmos pheri c CO 2 at 

the Earth's surface as a fun ction of 

latitude and DOY. 
(b) 

• - I.\lO _ KUM 

GM\ 

. SMO 

• SPO 

Figure 52.--(a) Ne a n difference and (b) RtIS difference between model and obse rved CO 2 concentrations (p pm ) at locations of sampling. 

details of th e annual cyc l e . In general, the annual mean agreement is good 

excep t at the Azores . The RNS di ffe r e nces of model and flask results a re l ess 

tha n 4 ppm for 12 of the 18 locations . So uth ern Hemisphere fla sk CO 2 results 

are examined i n sec . 4 . 2 . Only a t the Equator was there a n obvious annual 

cycle phase difference in the time series of CO 2 concentrations for two lo ca -

tions having about th e same latitude. Other cases of l ongi tudina l differences 

were more subtle. 

4.1.3 Co nclusion 

Th e a bove comp arison of dat a vs . model CO 2 va lues shows that a twodi mensi ona l (al titude-latitude) model of CO 2 exc ha nge ca n exp lain a l arge 

proportion of the variabi l ity of CO 2 change in the course of I yea r. The 

model i s intended for interactive use fo r evaluation o f dala and estimation of 

gl oba l car bon cycle f luxe s . The prediction of globa l atmospheric CO 2 increase 

following a n E1 i~ o event is a possible future application. 

4.2 A Preliminary Examinatio n of CO 2 Data in the High Latitudes 

of th e So uth er n Hemis phere 

As part of t he CO 2 flask sampl ing program, evaluation of the re s ults of 

networ k sampling is i mp or tant t o see how th e objectives of the program are 

being me t. This brief report describes the beg innin g of s uc h a n e ffort 1n 

whi ch seve ral hi gh -latitude Souther n Hemispheric samp ling locations are 

examined . 

In an earlier examination of s ix sets of flask data for 3 yea rs, Gi lle tte 

and Hans on ( 1983) r emarked t hat data from high-latitude so uthern locations 

seemed t o have less yea r-to- year vari ab i lity a nd possibly mo re spatial corr ela tion than data from northern locations. Because in the Southern Hemisphere the annual CO 2 cyc l e is smaller, flask sampling errors tend to obscure 

78 
Lhe a IlI1 II ,1 I cyel p mo re Lhere th<111 they do at northern locaLions . Thus, an 

(>.]rly eX lll1inatioll o f SOllLilerll flask s<'1lllpling locations \,"(1S undertaken Lo gain 

experienc(' [or slIch analyses and to guide the sLraLegy Lo obtai n the best data 

I. o ssible [or carbon cycle modeling. P. Fraser of CSIRO is cooperating in this 

examination of daLa and has provided data for Cape Grim, Australia. For this 

prelimjnary analysis, conLinuolls data [or 1980 frolll SPO and Cape Grim, and 

flask data [or 1981 from Amsterdam Island, Falkland Island, Palmer Station, 

and SPO are used. 

EquaLions were written that expressed concentration of C02 at one location as a linear [unction of CO 2 co ncentration at SPO (continuous) or Cape 

Gri ln or botll, Lo test the data for illdependent illformaLioll at tile sanlpling 

sites. The equaLions expressing CO 2 flask co ncentrations at location i and 

day j are 

x. = ,\ I . + A2i XSPOj + E .. 1J I. 1J (2) 

X

SPOj = D1 + D2 \Gj + E. 

J 

(3) 

h'here [\] i' A2i' D], and D2 are constanLs to be uetermincrl; Ei] and Ej are residuals; and CG refers to the Cape Grim data. Data [or 1981 ,,'ere used in (2) 

.nd data [or 1980 ,,'ere used iu (3). Residuals E. and E. "ere tested for 

1J J 

independence by the Kolnlogorov - Slnirllov white-noise tesL as described by Box 

al.d Jellkins (1976) . 

50111(' results are sho\,"n in Lable 28. AmsL e rdam Is land COL values s hov," independence from spa daLa. Palmer Station cOllcentrations can best be expressed 

as a linear fllncLion of spa cOllce ll trations. Til e allnllal cycles are practically 

the same, but Palmer data are aho ut 1.7 pplll higher then SPO data for 1981; 

Lhis is possibly an oceallIc elt.ect. Fa1kland Ts]a nd data shov, illtiepelidelllt:" 

[rom SPO data, but shO\,' a decreasing lr<.>nd near the end of the year that Illay 

indicate questio llahle data at that time. SPO and Cape Grim C02 data presenLed 

LIl fjg" 53 h'ere l.ikeh'i se shO\,' 11 to have sOl11e -indepelldence ap parcntJy ovC'r time 

periods o[ several monLhs for 1980. 

Table 28. --Resul ts of CO 2 data tests 

Loca ti 011 

AlliS Le rdam I. 

Falkland Is. 

Pa]lner StaLion--PSA 

SPO (flasks) 

79 

ResIIJLs 

IndepelldenL illforlnaLiol1 

Questionable 

XpSAj = 1.005 XSPOj 

E .. 2 = 0 .514 ; white lIaise 

LJ 

XSPOj = 0 .9 997 hSPOj 

E .. 2 = 0 . 444; white noise 

IJ 
,,,sf . ':"':'':'''~~'::'.''::::':7:~:' 1 ~ 3J.6- ' ,... ..... •• :::- 0" 

....... '0. . ....... 

.., '.0· •. 0 .. -= ••. 0 ........ . :!: •• 0 •• 0 , 

S 33.1 '-

1.17 110 

Oay of Year (1980) 

• Cope G"m 

• Soulh Pole i 

2" 

Figure 53 .--C0 2 data for SPO and 

Cape Grim i n 1980. Data are presented on the 1974 SIO scale. 

Since onl y 1 year of data was available f o r analysis , a cross- spectrum 

a nalysis was do ne for the SPO a nd Ca pe Grim sites for periods of up t o 

4 mOlltil S . TillIe series we re ljllear l y delrended and a si nu so i d hav illg a 1-y r 

period \,'a s removed [rom the data . For the 1980 data, no coherence was round 

for peri ods up t o 4 mo nths, possibly because o[ the mont h-l ong data g ap in the 

Cape Grim dala. 

Th e [ o 1101,-i ng concl usi ons ca n be drawn from this s tud y : (1) Amsterdam 

l s l. alld ha s a CO 2 cOJlcentration Lime se ri. es tha t ca nnot be h'riLLen as a linea r 

function o [ the SPO time se ri es ; (2) Palmer St a ti on ha s a n e l evation of CO 2 

co ncentrations but the sa me ann ual cycle as SPO; (3) Falkland Island has questionable CO 2 data; (4) the SPO a nil Cape GrilD CO 2 re co rds are s ignificantly 

different f o r 1980 a nd t here is no cohere nce [or [luctuations o[ periods less 

Lhan 3 mo nlh s . 

4. 3 Dobson Spectrophotometer Automation and Establishment of the 

Gl oba l Umk e Ilr Observat i on Network 

fu ndi ng was rece ived early in 1982 from EPA, CtIA, a nd 11J'10 [ or a utomation 

of s ix Dobso n ozo ne s peclropholome Le rs [ o r Umkehr observaLions, h'hich yield 

da ta on the ve rti cal distribution of atmos pher i c ozo ne, a t a select global 

npl ~o rk of stal i ons . Dala fr oln l il e networ k a re expec l ed to provide informa -

tion on poss ihle long-lerm ozo ll e des trucli on (e.g., by hal ocarbo ll s) nea r 

40 kill, <"Ind Lo se rve as comparisons f o r s aLe ] -] iLe ozo ne obs erva lions. 

Stati oll s tentatively seject e d for the Umk ehr obse r vatio ns are tILO; Poker 

Ftal, Ala s ka; Haul e Prove nce , France; Pretoria , Soul h Africa; lIu ancayo , Peru; 

alll! Pertll, Allslr.l1 i_.1. BOlllder, Co .l o ., h'ill constiluLe the sevenlh stalion of 

th e nelh'o rk, using Dobson i ns Lrume nt fl O. 61, \\'hl e h h'as aulomaled in ]981. 

Wil h use of an aUlomated Dobson inslrument, th e obse rver is replaced by 

all HP99 15A comput e r a nd an llP2240A meas ur eme nt ond contro l processo r. Stepper 

nlolors se l ecL wavelellglhs 0 11 wiljc h obse rvalions a re mari e , alld co ntrol the 

positi on o f th e inslrume nl' s o pti ca] \\'edge during obse rva ti ons . Temperature 

se nsors loca t ed \h thin the instrument aUlomalical l y compensate [or t e mp e rature 

e[[ects . \'o ltage on th e photomultiplier tube is co ntro ll ed digitally . A 

baltery- backed c l ock provides an acc urate real -time base f o r compute r opera -

lion. 

Obse rva l o ries ho using th e au t onlated DobsOl1 instruments wj l l have a ul o -

mated shutte rs that a llO\ .. ' Umk ehr o bservati o lls lo be made, beginning a t su nr-i se 

80 
and ending at sunset, without the presence of an observer . Precipitation 

detectors will keep the shutters closed during adverse weather conditions . 

Rotatable instrument chassis will track the Sun during observations, to minimi ze measurement-degrading polarization effects. 

Al though Umkehr observa tions "'ill be fully automa tic, measurements of 

total ozone will be semiautomatic. After positioning the Sun director on the 

instrument's light inlet window and orienting the instrument correctl y with 

respect to the Sun, the operator will merely activate a switch to initiate the 

t otal ozone measurement. About 2 minutes later the computer "'ill yield the 

total ozone amount. 

The Umkehr observation network using automated Dobson spectrophotometers 

is expected to be fully operational by the sunmler of 1984 . 

4.4 Studies of Winter CO 2 Variability at HRW 

4.4.1 Introduction 

As part of a series of studi es on va riabi lity of CO 2 co ncentration at 

HRW, the relation between anthropogenic aerosol and CO 2 in the Arctic was 

examined to gain a better understanding of the variations in CO 2 co ncentration 

of up to 3 ppm that occur over periods of 1-7 days during winter . Kelley and 

Gosink (1979) made measurements suggesting a CO 2 source in the Arctic Ocean 

during winter; Rahn (1981) discussed transport pathways of pollution aerosol 

from mid1atitude industrial centers to the Arcti c; Shaw (1981) suggest ed a 

synoptic-scale eddy diffusion of pollution aerosols into the Arctic; Shaw 

(1982) presented evidence of direct transport of pollutants into the Alaskan 

Arctic by atmos phe ric mean flow; and Barrie et al. (1981) discussed periodic 

injections of pollution aerosol into the Arctic from lower latitudes and the 

accumulation during winter of these pollutants in a horizontally mixed reservoir. 

In the present study, continuous CO 2 analyzer data, meteorological data, 

and the results of aerosol chemistry filter samples, the last furnished by 

K. Rahn of URI, for December 1979-March 1980, were examined to determine 

whether these factors have some bearing on CO 2 measurements at BRW and, if so, 

to assess the relative co ntributions of these factors to CO 2 variabi lity. 

4.4.2 Analysis and Results 

Daily averages of CO 2 and the pollution aerosol indicators, excess (noncrustal) sulfate (XS0 4 ) and vanadium (XV), are plotted in fig. 54 . The cubic 

spline best-fit curve provided a reference for calculating departures of C02 

co ncentrati on . Three approaches were used to study CO 2 variability . 

The first approach involved weather map classification. Examination of 

8S0-mb constant pressure charts identified three main atmospheric flow regimes 

affecting BRW for the study period: (1) northerly flow from the Arctic Ocean, 

(2) so utherl y fl ow from the Pacific region, and (3) easterly flow from the 

Canadian Arctic. These patterns accounted for 36%, 30%, and 11%, respectively, of all twice-daily 8S0-mb maps for the study period. CO 2 and aerosol 

81 
Figure 54.--Daily averages of C02 

concentration and sample averages of 

noncrustal sulfate (XS04 ) and vanadium (XV) at BRW for December 19 79-

March 1980. The dashed line is a 

cubic spline best-fit curve to the 

CO 2 data based on hourly averages. 

CO 2 concentrations are given in t he 

SIO 1959 Index scale . 

chemistry data were partitioned according to the corresponding flow regime. 

The means for CO 2 departure, XV, and XS0 4 for the Arctic Ocean flow pattern 

were significantly greater (by the Student's t test) than those for the Pac ific region flow pattern. Except for XS0 4 , t he means for the Arctic Ocean fl ow 

pattern were also significantly greater than those for the Canadian Arctic 

flow pattern . The standard deviations within map types were, however, quite 

large. For CO 2 , this was a reflection of a few departures in both Arctic 

Ocean and Pacific region flow patterns that had an opposite sign from the 

mean. 

The second approach was to consider the correlation of CO 2 concentration 

with meteorological variables and pollution aerosol . Correlation coefficients 

of CO 2 concentration with meteorological variables were low but of the sign 

expected from the results of previous studies (Peterso n et al., 1980; Ha lter 

and Harris, 1981), suggesting higher CO 2 with northerly flow and colder, drier 

air masses than with warmer, moister southerly air. In contrast to the co nsiderable variability of CO 2 departure within a particular atmospheric flow 

regime and the weak correlation with meteorologica l variables, the linear 

correlation of CO 2 with pollution aerosol indicators was considerably stronger, +0.7 for XV . This fairly high positive correlation refl ects the correspondence of peaks and valleys in dai l y CO 2 and pollution aerosol indicator 

levels plotted in fig. 54. 

In the third approach, CO 2 concentration as a function of air mass origin 

was determined. A division of the Arctic into sectors similar to those of 

Miller (198 1b ) was made. The origin sectors of all (twice-daily) 10-day, 

850-mb back trajectories during the study period and the corresponding average 

daily CO 2 departures were noted. The significance of the difference between 

sector CO 2 means was tested by usi ng t tests at the 0.05 confiden ce level . 

The results of this analysis, shown in fig. 55, indicate that average CO 2 departures associated with trajectory origins over mu ch of the Arctic (sectors A 

and B) were slightly negative and were not signifi cantly different from ave rage CO 2 departures in the Pacific region. Anot her important result is that in 

moving from sector B t o E and from E to H, average CO 2 departures become pos itive and increase significantly. In his study of low-level back trajectories 

to BRW, Miller (198lb) found a sharp April decline in the freq uen cy of trajectory origins in the region corresponding to sectors E and H. Rahn (1982) 

demonstrated a corresponding decrease in XV leve l s. Although the level of CO 2 

82 
I 

-.38 

(26) 

Figure 55.--Average CO 2 departure as 

a function of a 10-day, 850-mb trajectory origin. The signed numbers 

are average CO 2 departures (SIO 1959 

Ind ex) . The tallies of daily averages used in calculating the sector 

averages are in parentheses . 

during these events does not decrease correspondingly, variability in CO 2 does 

de crease markedly. 

4.4.3 Discussion and Conclusions 

The pre cedi ng evidence regarding winter C02 variability at BRW provides a 

basis for assessing the relative importance of the three possible causes: (I) 

a natural source in the Arctic Ocean, (2) a homogeneous Arctic air reservoir 

of midlatitude industrial CO 2 gradually accumulating during winter , and (3) 

transport of industrial C02 directly from source regions. 

The first possibility is supported by the winter-spring supersaturation 

of CO 2 in Arcti c Ocean water with respect to the atmosphere. The second possibility is supported by the positive average CO 2 departure for northerly 

Arctic flow, the negative average departure for Pacific region flow, and the 

oscillation between these two patterns being a major feature of the winter 

atmospheric circulation over the Alaskan Arctic. In contrast, the third possible ca use is strongly evidenced by the greater predictive ability of pollution indicators (XV and XS0 4 ) than meteorologi ca l factors regarding CO 2 departure. The first and second possibilities seem less likely than the third 

for the following reasons. Some C02 departures with the Arctic Ocean flow 

pattern are negative . Also, the trajectory study suggests that much of the 

Arctic is not a CO 2 source. Furthermore , the spatial heterogeneity in the 

Arctic implied by that study does not seem in accord with a homogeneous, well -

mi xed Arctic air reservoir, A cas e in which a major positive CO 2 departure 

and pollution indicator peak occurred with a Pacific region flow pattern leads 

83 
to the s uspicion that CO z variabili t y is related to direct trans port from 

specific ind ustrial regions and that air ma ss or map type may be more coi ncidental than ca usal. 

The trajectory study rei nforces the third possibility as the most important factor contributing to s hort-term C02 variabi l ity. Additional evidence 

is furnished by the coincidence in April of a marked decline in the frequency 

of trajectory origi ns i n sectors E a nd H, which a r e associated with the greatest positive depar tures in CO z ; the onset of a 2-mo period of relative ly 

s teady CO z ; and a rap id dec line in XV. Therefore , ba sed on the evidence presented here for the three possible causes, relatively direct transport of CO z 

from industrial regions ma kes the grea t est contribution to sho rt-term (periods 

of a few days) winter variability in CO z concentrati on at BRW. This variability appears as fluctuations of up to ±3 ppm superimp osed on the annual trend. 

A discussion of short- term CO z variability has implications conce rn i ng 

the represen tativene ss of the data. Thus , CO 2 departures determined in this 

study are not necess arily depa rtures from background; they are departures from 

a cubic sp line best-fit curve to the data. The trajectory origin analysis 

shows that, for the winter of 19 79 -1 980, average CO z departures associated 

with 10-day trajectory origi ns over a large area surrounding BRW were not 

statist ically different. 

The implied homogeneous distribution of CO z in the region centered a t BRW 

1S consiste nt with the co ncept of regional background. If this regi onal average CO 2 concentrati on is accepted as background, then the traje ctory origi n 

analysis is consi stent with the idea t hat perturbations from regi onal bac kground co ncentration are the result of rapid transport from areas ou t side of 

the region. For example, the 1- to 7- day episodes of large positive CO 2 departure are produced most ofte n by transport of anthropogenic C02 from the 

vici nity of Europe and central Asia . Comparable periods of negative CO z depar tur e reflecL a return to c leane r conditions. 

A co ntr as ting idea i s t hat these period s of negative CO 2 represent pe rlurbations [rom characteristic Alaskan Arctic levels rather than a return to 

regional background. The latitudinal gradien t in CO z co nce ntration during 

winter (Bod haine and Harris, 1982 , pp. 21- 22) s uggest s that arr ival of air 

from the Pacific region south of 55°N should result in reduced CO 2 concentra -

tions at HRW (Pete rson et al., 1980). Our trajectory study ag rees with this 

idea whereby t he greaLest negat i ve CO 2 de partures at BRW were associated with 

t rajectory origi ns over the s ubtropi cal Pacific Ocean. 

Thu s , transport of air relatively l ow in CO 2 from the Pacific region may 

be involved in the s hort-term winter variability at BRW i n additi on to direct 

transport of i ndu strially derived CO z . Perhaps the application of the trajectory-origin vs. COz - departure analysis to a larger se t of BRW data would c larify th e ro l e of long-range transport from the Pacific region. The r esulting 

distributi on o f CO 2 de parture as a fun ction of trajectory origin might then 

provide the basis for usin g trajectori es Lo i dentify bac kgr ound and nonba c kground samplin g co nditions in the data se l ec lioll process . 

4 . 5 Measurements o f Skylight Polarization at MLO 

The we ll-known sensitivity of the polariza tion of light from the s unlit 

sky to the effec ts of dust, haze, and ot her particles in the atmosphere, in 

84 
90,-------------,--------------, 

~80 

i 

~70 

~ 

~60 

0: 

.. 

..J 

050 

a. 

Le 

0 40 

'" '" 0: 

"'30 

'" " 

20 

10 

C LEAR ........ 

4123 

_ -...1. ....... - 1"""-

,- I '\ 

I \ 

--.-1r-"----" 

~'- ' 

:f\ , " ", ... , \ \ 

I' " , , \ 

, ... \ 

:1 

, ! I 

: I 

, I 511~ 

4111--

I 

I 

I 

NP 

0~~6~~4~~~~~~~~~~~ 

SUN ELEVATION (0) 

Figure 56.--Degree of polarization 

at 700 nm, as a function of Sun 

elevation, observed under the El 

Chichon stratospheric cloud at MLO. 

A curve typical of clear atmospheric 

conditi ons is given for comparison . 

(NP = neutral pOint.) 

conjunction with the appearance of the volcanic cloud from El Chichon in the 

stratosphere over Hawaii in Apri l 1982, provided strong olotivations for continuing and expanding the measurements of skylight polarization at tlLO. Of 

most interest are measurements in the red and near-IR spectral regions made 

during the morning twilight period at the 3 . 4-km altitude of the observatory. 

neasurements at these \,18velengths are useful for detecting and characterizing 

atmosp heri c aerosols be cause the radiation is less subj ect to multiple scattering by ord inary oxygen and nitrogen molecules of the atmosphere than at 

shorter wavelengths . Measurements during morning twilight are preferable to 

those during evening twilight because of less interference from clouds in the 

morning. 

The degree of polarization of light from the zenith sky, mea s ured during 

twilight and in the immediate postsunrise period at MLO soon after the appearance of the volcanic cloud over Hawaii in April and May 1982, is shown as a 

function of Sun eleva tion in fig. 56 . A curve for the average clear atmospher e , as observed under the clean stra t ospheric conditions of 1977, is given 

for comparison. Lidar observations at MLO showed the cloud to be markedly 

variable in density and height in its early stages. For instance, on 11 April 

the clo ud was of sufficiently high density to cause a virtual reconfiguration 

of the polariza tion field, particularly in the inunediate su nrise and postsunrise periods. The clo ud top, however, was restricted at that tinle to an altitud e of about 26 km so that the data during twilight were not transformed to 

the extent shown by later measurements . By 14 May, the cloud top had risen to 

at least 35 km, presumably by a process of gas-to-particle conversion in its 

upper levels. This increased c l oud thickness caused not only a further de -

crease of polarization magnitude and the appearance of an anomalous neutral 

point afte r sunr i se , but also the deve l opment of a definite presunrise polarization minimum that continued to exist through the remainder of the year. The 

cloud became very thin and tenuous on 23 April, as indicated by the tendency 

of the polarization field to return t o normal . 

85 
90 

80 

70 

60 

~ 

is''' 

\:i 

N 

it: 40 .. 

-' 0 

Q. 

30 "-0 

"' "' 20 a: 

C> 

"' " 10 

0 

8 

CLEAR _ 

/;\ 

( ~ 

~2!~ ____ / / \ 

1/ 

/1 

, I 

~2~8~ __ .... /1 I 

6 

I 

4 2 0 -2 

SUN ELEVATION (0) 

\ 

\ 

, 

I 

, 

I 

, 

, 

,---

I ,......_ ..... 

, ,I 

\..J I 'J 

- 4 ·6 ·8 

Figure 57.--Degree of po larization 

at 700 nm, as a function of Sun 

elevation, observed on various dates 

following th e appearance of the El 

Chi chon cloud ove r Hawaii . A curve 

t ypica l of clear atmospheric conditions is given for comparison. 

MeasuremenLs ma de later in 1982 and on 12 May 1983 (about 13 months after 

the clo ud reached Hawaii) are shown i n fi g . 57 . A t e nden cy to return to normal i s evi dent in the data, but the twili ght configurati on 1S s urprisingly 

persistent in s pi te of decreasing cloud den sity and height as indi ca t e d by 

lidar measurements a t MLO. 

The polarization meas urements will be continued to doc ument as completely 

as possible the effects of volcanic material on the polarization field, as 

well as to develop the polarization method of detecting and characterizing 

stratospheri c aerosols i n the future . 

4.6 Arctic Haze and AGASP 

4.6.1 Introduction 

Haze over the Arctic ice cap was first exte nsively document ed by Mitche ll 

(1957) . He no t ed that th e haze was generally observed during periods of otherwise clea n air, extended over a ltitudes from near the ground to 300 mb, and 

exte nded over air routes up t o 1,000 km long . On the basis of a range of 

optical and physical evide nce, Mit c he ll suggested that the haz e was composed 

of non-ice parti c les ha ving diameters smaller than 2 ~m. Two decades later 

his suggesti ons were co nfirmed. Beginning in the mid seventies, research re -

sults from several groups confirmed the pr esence o f mu ch higher concentrations 

of aerosols in the Arctic atmosphere than one would ex pec t in a remote and 

s upposedly pristine environment. 

A virtual explosion o f informa Lion on Arctic haz e followed the aerosol 

chemis try measurements of Rahn et al. (1977) , and a n entire issue of Atmo -

spheric Environment (vo l. 15, no . 8, 1981 ) was devot ed t o Arcti c air chemistry. A consensus of these and other papers s uggests that ( I) Arctic ha ze is 

a widespread phe nomenon hav ing a ma j or concentration peak in Mar ch-April; 

86 
(2) horizontal and slant visual ranges in Arctic haze may be restricted to 

5-8 km by the haze; (3) wintertime Arctic haze has a large pollution-derived 

component of probable Eurasian origin; (4) the_~ollution component ~f the 

aerosol is dominated by sulfates (up to 2 ~g m ), organics (1 ~g m 3), and 

black carbon (0.3-0.5 ~g m- 3 ); (5) the haze is well aged, as evidenced by its 

high secondary/primary ratio and by peak concentrations in the low submicron 

range (accumulation mode). 

4.6.2 Possible Climatic Effects of Arctic Haze 

Elevated levels of aerosol concentrations in Arctic haze such as those 

measured at BRW have been shown to contain a large black carbon component. 

This component can attain a concentration of up to 40% of the total carbon 

content of the aerosol, which approaches that observed in urban atmospheres . 

Radiative-transfer modeling studies indicate that average local atmospheric 

heating by solar absorption from a thick layer of carbon aerosol in the Arctic 

haze may be comparable with that from doubling atmospheric CO 2 concentrations 

(Porch and HacCracken, 1982). These effects are most pronounced in the high 

Arctic latitudes, partly because of the high surface albedo of large and persistent areas of snow and ice. 

4.6 . 3 The Arctic Gas and Aerosol Sampling Program 

A multilaboratory NOAA group \"as formed in tlarch 1982 to organize and 

direct an airborne study (AGASP) of the phenomenon of Arctic haze; flights 

were conducted from mid-tlarch through mid-April 1983. The NOAA WP-3D Orion 

aircraft used in this study is a modern, highly versatile and efficient research platform. The aircraft has a range in excess of 3,000 runi with a complement of up to 18 crew and scientists. An international cadre of government 

and university scientists joined the NOAA group in this unique undertaking. 

A list of the principal investigators and their programs is presented in 

table 29. A more detailed description of the AGASP project is g.ven by 

Schnell (1983), and an up-to-date discussion of Arctic haze is given by Hileman (1983). 

AGASP had these central measurement objectives: (1) to determine the 

distribution, trajectories, and chemical composition of Arctic haze aerosols; 

(2) to determine the concentration and distribution of trace gases, mainly 

anthropogenic, such as halocarbons; (3) to determine the concentration, flux, 

and gradients of atmospheric CO 2 in relation to important Arctic sources and 

sinks; (4) to measure the in situ radiative effects of the haze; and (5) to 

document the existence of, and conduct gas and aerosol measurements in, polar 

tropopause folds. AGASP allows the comparison of measurements, theory, and 

modeling of the climatic effects of Arctic haze. 

The measurements were conducted during 120 research flight hours in the 

Arctic atmosphere, which included profiles above and upwind of surface stations (such as at BRW) in the international Arctic Air-Sampling Network. 

Coordinated aircraft operations were conducted from Spitzbergen by NIAR (one 

aircraft) and by the tlax-Planck Institute for Chemistry, Hainz, Germany (two 

aircraft). In addition, the DOE 1-'13-57 flew above the NOAA WP-3D during the 

Alaskan flights to conduct complementary stratospheric measurements. Approximate flight tracks for the NOAA WP-3D are shown in fig. 58. Dropwindsondes 

87 
Project 

leader 

R. Schnell 

S. Naegle 

B. Bodhaine 

K. Rahn 

W. Zoller 

H. Rosen 

K. layaweera 

W. Berg 

A. Lazrus 

R. Borys 

G. Grams 

G. Sha,,' 

f'. Pa rungo 

A. Hogan 

S. Oltmans 

R. Rasmussen 

G. Bingham 

R. Gammon 

L. Heidt 

G. Herbert 

R. Gilmer 

J. Harris 

Cooperating 

fl. Shapiro 

A. Kruger 

R. Lie fer 

P. Guthals 

II. Raatz 

P. Crutzen 

T. Cahill 

A. CIa rke 

J. DeLuisl 

T. Ackerman 

F. Vallero 

B. Nendonca 

II. Rodhe 

B. Otta r 

R. lIoff 

S. Rossby 

J. DuGranrut 

Table 29.--AGASP management and scientists 

Institution 

CIRES 

CIRES 

NOAA/GfiCC 

URI 

Univ. of fld. 

LBL 

Uoiv. of Alaska 

NCAR 

NCAR 

CSU 

Georgia Inst. of 

Tech. 

Univ. of Alaska 

NOAA OWR~I 

SUNYA 

NOAA/ GtICC 

OGC 

LLI 

NOAA/ GNCC 

NCAR 

Exchange 

NOAA/GNCC 

NOAA/G~ICC 

NOAA/GNCC 

Aircraft/Satellite 

NOAA/WPL 

NASA/Goddard 

DOE/New York 

Los Alamos Na tl. 

Univ. of Alaska 

Responsibility 

Administration 

Overall project management 

Data manager 

Aerosols 

Gases 

Integrating nephelometer, PIXE, CNC 

Trace elements, organics 

SO , IfN031 H2S, Hg, trace elements 

Cafbon 

Spores , bacteria 

Cl, 8r, I, Na, K, V, Mil 

SO. 

Aerosol size distributions 

Polar nephelometer 

Aerosol size distributions 

Aerosol composition 

Aerosol size distributions and 

composition 

Ozone 

Trace gases 

CO 2 flux/concentration 

CO 2 concentration and source-sinks 

Halogens 

Processes/Trajectories 

Energy-C02 fluxes 

NOAA gus t probe 

Air mass trajectories 

tleasurements/Meteorological Analyses Programs 

Lab. 

Tropopause folding events 

TONS satellite ozone data 

HASP \oiB-S7 Flights 

Max-Planck lnst., 

tiainz, FRG 

HASP aerosol chemistry analysis 

Arctic meteorological analyses 

German aircraft measurements 

Carbon/Radiation 

Univ. of Calif., 

Univ. of Wash . 

NOAA/GNCC 

NASA/Ames 

NASA/ funes 

tleasurements/Climate Modeling 

Davis Carbon optical properties 

Aerosol light absorption 

Su rface radiation measurements 

Arctic haze modeling 

Net radiation flux/airborne 

measuremenLs 

Surface Measurements 

NOAA/G~ICC 

Uoiv. of Stoc kh olm 

NIAR, Norway 

AES, Canada 

NOAA/RFC 

NOAA/RFC 

NOAA WP-3D 

BRW operations 

Swedis h stations 

Non.,'egian measurements 

Canadian measurements 

Research Aircraft 

88 

RFC Project Director 

RFC Project Engineer 
Figure 58.--Approximate NOAA WP-3D 

flight tracks during AGASP . 

were released from the WP-3D in remote locations, including over the North 

Pole, to study the vertical structure of t he atmosphere. Fl ight patterns were 

designed to transect all major pathways of Arctic haze precursors into the 

Arctic basin. 

Initial data reduction and preliminary analysis indicated that AGASP was 

a very successful field experiment . Results \,'ill be summarized in next year's 

G~ CC Summary Report. 

4.7 Light Scattering, Condensation Nuclei, and Air Hass Trajectories 

at Whiteface Hountain 

4.7.1 Introduction 

A cloud chemistry and radiation experiment was jointly conducted by ASRC 

and G~ CC at \,HI duri ng the summ ers of 1981 and 1982. HHI, operated by ASRC of 

SUNYA, is ideally located (44.39°N, 73.86°\;) as a continental site, intermediate between an ur ban area and a background site such as a GHCC observatory. 

The experiment was designed to investigate possible changes in ti,e interaction between clouds and solar radiation caused by aerosol scave rlging in t ile 

clo ud. Since anthropogenic aerosols can alter cloud droplet sizes, it follows 

that t he radiative scattering and absorptioll properties of clouds could be 

affected by the aerosols dispersed within the clouds. The objectives of the 

experiment were ( 1) to collect cloud water and ana l yze the residue f or optical 

absorption, (2) to identify the residue chemically, (3) La measure the optical 

properties of the free aerosol, (4) to calculate the modified cloud optical 

properties, and (5) to estimate the enhanced absorption of the cloud caused by 

absorbing anthropoge nic aerosols . 

4.7 . 2 Ins t rumentation 

The instruments supplied by GtICC for installation at \,HI were a Gardner 

CNC, a G.E. automatic CNC, a four - wavelength nephelometer, a one-wavelength 

nephe l ometer, an HP data acquisition system, and a Leeds and Northr up mul tichannel chart recorder. All instruments were installed and operating on 

89 
'Ill 'ntUOC1tIRJES AllllIVISC 62I!1O - ~/lO/82 .1lI nuJOCTDlIlES AIIRJVISC 62ISJ - 6/ 1/ 82 

A.O'Z ae.oV9 C In ae.oVB A.O'Z &60 VB c-In MOVB 

9 O'Z lOOV9 II In lOOV9 B0'Z1OOVB DlnlOO vB 

.nI nuJOC1tIRJt:> A!tRIVING 62162' 1/ 1/ 82 'N 'ntUOC1tIIUES ARIIIVI.'iG 62IM _ ' / 11/ 82 

A O'Zae.o V9 Clnae.o V9 A.O'Zae.oIlB CI2%MO II9 

eO'ZlOO V9 Dln1OO V9 90'Z1OOV9 D_ln1OO 1iB 

\ 

Figure 59 .--Exa mples of ai r ma ss trajectories from the sou th (u pper left), 

east ( upper right), nort h (lower left), and wes t (lower r i ght ) at 850 and 

700 mb on DOY 150, 157, 182, and 198 res pec tively . 

22 Ma y 1982 (DOY 142), a nd the experimen t was terminated on 19 August 1982 

(DOY 231). 

4 . 7 . 3 Discussion of Se le cted Data 

All data for the s ummer of 1982 at W'HI " ere presented by Bodhaine e t aI. 

( 1983). This report gi v e s a ll li ght-scattering and eN da ta in graphi c f orm 

with both 10-min and I-h time re so lutio n, and in tabular form with l-h and 

I-d ay geometric mean s . In additi on, t "ice- daily (0000 and 1200 GtIT) 10-da y 

back trajectories, calculated at the 850 - and 700 -mb levels "ith W'HI as the 

end point, are pres ented. These traje c torie s we re ca lculated as desc ribed by 

Harris ( 1982). 

Examinati on of the 1982 W'HI data showed that a va ri e ty of me teorological 

conditions existed with air mass trajectories arriving fr om all directions. 

Four trajectory c lasses were exami ned: ( 1) those from the west with paths over 

90 
- -

A ~-- . 

~ 3::; --.J: ~ -, _~_. 

.. I '\ " '; - r - , J - '- • - . I ,,,j 

~~--' -~ ----. 

~:;=:;=..;::::::===-== ~- ---= : 

j--.....,--r---- -- --~~ , -

' --' ----'-

- ~ - ---=-,~ - --r , .r . \ -... I.: 

~ + '-:;:::::- __ ---"".~ ... --,-, - - !. --- " 

t .+' /"";.... 0- J' ~' r 

j---+'''-~ --~~- - .-

------.--

" ! .. ~~~ ,rl"~'~~ " ; " -

~ ______ --"'P"" ~ .QL1lI ... I -.ltALlVIR- ... ~ __ 

- -_ 

:-----==--== 

I 

+--:-------- - --. ";. II. ._. __ _ ! I I 

", ~ bJ, -' ""V" r· r' i ". • ",ft '. or----. c "- -.-- -----;r __ ., . 

, -. . r I ,'. ,.,.. . • • • . '·' r i , 

, , .'" I , 

~ __ ~ ___ ... ... .. "" -"[)I.LJILI"H£ U a R '!If\? 

Figure 60.--Selected 10-day periods of aerosol data at \.JFN. Each frame shows 

Angstrom exponent (upper), light scattering (m iddl e) , and CN concentration 

(lower). Light-scattering data are f or 450 - (do tted ), 550- (solid) , 700 -

(dashed) , 850 - (long-dashed), and 525 -nm (chain-dashed ) wavelengths . Angstrom 

exponents "'ere calcu l ated from the 450 - and 550 -run (dott ed), 550- a nd 700 -nm 

(so lid), and 700- and 850 -nm (da s hed ) light-scattering data. 

the Great Lakes region, (2) those from the east with a maritime orlgin, 

(3) those from the south with a southern U. S. continental origin , and 

(4) those from the nort h with a Canadia n continental origin. One exampl e from 

each c la ss is shown in f ig . 59. Each of these days is in cluded in the t i me 

series of CN, light-scattering, a nd Angstrom exponent data shown in fig. 60. 

Table 30 gives the daily geometric mea ns of these data for the four example s 

given in fig. 59. 

DaY 198 exhibited the highest light-scattering values of the entire summer. The weather pattern during the time period DaY 194-198 recurred throughout the s ummer, and consisted of increasing atmospheric pressure and hazy, 

polluted conditions that generally worsened until a front pa ssed the station 

91 
Table 30.--Daily geometric mea ns of light scattering,* Angstrom exponent, and 

CN concentrati on at WHI for days selected to illustrate trajectories 

arriving from the four different directions shown in fig. 59 

Sou th East North West 

DOY 150 DOY 157 DOY 182 DOY 198 

a (450) m- 1 6.55-6 1. 74-6 1.67-6 4.91-4 

sp 

m- 1 a (550) 4 . 66-6 1. 18-6 1. 11-6 3 .59-4 

s p Ill-I a (770) 2.97-6 7.08- 7 7.49-7 2 .32-4 

sp 

m- 1 a (850) 2.00 -6 3.53-7 4.73-7 1.69-4 

sp 

a(450,550) 1. 7 1.9 2 .0 1.6 

a(550,700) 1.9 2 . 1 1.6 1.8 

a(700,850) 2 .0 3.6 2.4 1. 8 

CN cm- 3 385 1413 84 1 

*Values appear in a compact exponential format (6.55 - 6 = 6.55 x 10- 6 ). 

early on DOY 199. Trajectories were from the west during that time period. 

The peak hourly mean light-scattering values were 9.4 x 10- 4 , 7.2 x 10- 4 , 

4.8 x 10- 4 , and 3.5 x 10- 4 m-', In order of increaSIng wavelength at 1700 EST 

on DOY 198. The peak CN concentration of 1400 cm- 3 occurred 3 hours later. 

Table 30 shows that light scattering (or haziness) was about 2 orders of 

magnitude greater when traj ec tories were from the west than when trajectories 

were from other directions. Trajectories from the west were mo st common, 

followed by those fr om the north, south, and east . 

4.7 . 4 Conclusions 

Wh en trajectories arrived from the west aft er having passed over the 

Great Lakes industrial region, generally hazy conditions were observed in the 

vicinity of WHI and light-scattering values of nearl y 10- 3 m- 1 were recorded . 

Trajectories arriving from the north or the south were representative of continental background conditions and gave light-scattering values of about 

10- 6 m-I. Trajectories from the east, having a maritime origin, were repre -

sentative of the cleanest conditions and gave light-scattering values below 

10- 6 m -1 During this study, the majority of trajectories arrived at WHI from 

the west, accompanied by polluted atmospheric conditions. 

4.8 Lidar Observations of El Chichon Stratospheric Dust 

More than 50 lidar observations of strato spheri c dust were made at MLO 

during 1982. These observations captured the essence of the time changes of 

92 
verLical profile shape and optical depth of the Mystery Cloud and the El Chichon cloud described in detail in sec. 2.1.2. 

Figure 61 shOl,·s monthly average profiles o f El Chichon dust for 2.5-km 

intervals starting in April and ending in December. These profiles are scaled 

to unity at the profile maximum. The number above each profi le is a scaler 

multiplier that gives the absolute optical depth of dust when multiplied by 

the i ntegral of the r espective profile. Some interesting features seen in 

this figure are the altitud e rise i n the profile maximum from 24 to 28 km that 

occu rred between April and May , f ollowed by • slow descent from 28 km in May 

to 2 1 km in De cember. Another feature of interest is that the altitudes of 

the Ilalf-maximum points on the profile seem La displa y a cons tanL difference 

of about 5 km for the entire 9 months. 

April May June July August September October November December 

40r---'---'---r--'r--'---'---'~-'---T---'---'---'---'---r---'---'---'--, 

0.Q38 0.046 0.040 0.037 0.032 0.027 0.029 0.022 0.011 

_ 30 

E 

"-

~ 

'" "' ~ 

" 20 

10~-7~~~~--~-'~-'~-77-~~~-'~--~-'~-'~~~~~~-'~~ o 0.5 110 0.5 1'0 0.5 110 0.5 110 0.5 1/0 0.5 1' 0 0.5 110 0.5 110 0.5 

Relative Extinction (km .1) 

Figure 61.--Monthly averages of lidar observations aL MLO in 1982, in terms o f 

backscatLer rat io (Rayleigh + Mi el/Raylei gh. Vertical reso lution is 2.5 km. 

Th e profiles have been normalized so that the maximum _has a value of I. The 

scalar number given on each curve is i n units o f 4 km I, whjch when nlultiplied 

by the integral of the profile, gives th e optical de pth of the sLra to sp he ri c 

cloud. 

Figure 62 s hows a comparison between lidar- derived optical depth and 

sunphotomeLer monthly ave rage optical depth. The period Jalluary through March 

was marked by e nhanced s tratospheric dust from the Mystery Cloud. Note the 

hori zo nta l line labeled "Ave rage for 1980 - 81 Above 19 58 - 62 Background." The 

histori ca l MLO mea surements s how Lhe cleanest stratospher e during this background pe riod. 

To comput e scattering optical depth from the lidar meas urements, a value 

of 50 ~as used for Lhe total-scatter-to-backscatter ratio. A va lue of 56 was 

calculaLed from size distrib'ltiolls dedu ced from specLral optical depth inversions. If this value "'ere used, the lidar-scatLering optical depth would be 

l ower by aboul 15%. 

93 
-Udar 

• Sun Photometer 

0.1 

E 

0 

~ 

a> 

~ 

... 

0.01 

Average for 1980-61 

Above 1958-62 Background 

0.00 1 L_=--:-;-~~:-:--,--,--:--=-,--;:-'-c::-'--:c---;;--' JFMAMJJASOND 

Month 

Figure 62.-- Lidar-derived optical 

depth (small dots connected by 

lines) vs. s unphotometer ( large 

dots) month ly average optical depth 

at the 694 -nm wave length, al MLO in 

1982. 

4.9 Umkehr Ozo ne Profile Erro r Caused by El Chichon SLratosp he ric Dust 

Pa st theo r e tical i llves tigaLjons have indi ca ted a linear rel a tionship 

be Lwee n s tratosp heri c dust o pti ca l depth and amo unt o f error in the Umke llr 

ozo ne pro fil e . Umkehr and s tratos pheri c dust opLical depth meas uremeIlls were 

r o u tinely mad e aL tlLO s h ort"!y follol,odng the Harch-April 19 82 erupt i o n o f £1 

Chi c hon. A plot o f ozo ne concentratio n in Umke hr l ayer 9 VS. opLical depLh at 

380 nm i s s hm\' 11 in fi g . 63 . The s l o p e o f this pl o t gives the linear error 

term f o r l aye r 9 as 

Eg 

1 = 1'3(FO) 

where P3 is OZO ll e partial pressure 311d Td i s tile s tratosph eri c dust op tical 

dcpLh aL 380 nm. 

The s traight ljne lhro ugh th e points of fig. 63 \,'as dra vm \,'-itho u t regarrl 

to the po irlts beyond T = 0.25 be ca llse this may be a regio ll o [ no nlinea rity. 

However , lhis i s not ce rtain be cause o f [actors such as d us l pro file, seaso na l 

variation in bac kgr o und du sL optical deplh, and ozone prof il e , whic h have Ilo l 

been a cco unled fo r and may be invo lved. Such factors mu s t he invesli ga ted for 

a thoroug h underslailliing o f the presenl se t o f measurements. 

The most r ece nt lheore lically cal c ul ated s tratospheric dust Umk e hr errors 

indi c ate d an error sensilivity of about 950% pe r unil optical de pth of stratospheric dusl ( He rbert, 1980, pp. 65 - 68). The LO empiricaL error indi ca te s 

94 
J , ;0 

J .. .. E 

-" 

i 

0: I .. r ~ .t a 

- j 

0 

" ' 

: " , 

" , 

01 02 

td 1:iBO r.m. 

, 

.. , . 

Ol 

Figure 63. --Plot of Umkehr ozo ne 

partial pressure in layer 9 (-45 km) 

vs . El Chichon stratospheric dust 

op ti cal depth td a t A = 380 nm . 

Points beyond t = 0.25 were disregarded in the straight- line fit . 

that the error is more on the order of 400%- 500% per unit optical depth of 

stratospil eric dust. The difference may be due in part to errors in t he difficult theoretical calculation for a solar zenith angle of 900 , 

4. 10 NLO Trajectory Ensembles, April and tlay 1979-1982 

The transport of Asia n dust to the central Pacific Ocean has received 

considerable attenti on since the dramatic duststorm of late April 1979 at NLO 

(Shaw , 1980; Darzi and Ihnchester, 1982a), In February 1979 filter sampling 

began at NLO to determine aerosol chemistry (Zoller et al., 1981). The rela -

tive importa nce of the spring dust events of 1979 can be seen i n the accompa nying plot (fig . 64) of a lumi num (AI) concentrations measured during downslope winds (nighttime) . In discussing the Al concentrations, Parrington et 

al . ( 1983b) computed the concentration for February-June 1979 to be a factor 

of 10 greater than that observed during the remainder of the year . They also 

showed the pronounced decrease in Al concentration from 115 ng m- 3 in spri ng 

1979 to 57 ng m- 3 in spring 1980, The spring concentrations for 1981 and 1982 

are approximately the same as for 1980, In a n effort to understand the causes 

for the change i n the dust l oadi ng from 1979 to 1980, air mass trajectory 

ensembles representing each spri ng were obtained by plotting the 0000 Z, 

500 -mb back trajectories from NLO for April and Nay. These 2 months represe nt the peak of the dust season, and one trajectory per day was found to be 

fairly representative; t hu s, relati vely uncluttered plots containing 61 paths 

" 

" , . . . ', .. ~ 

95 

Figure 64 .--Weekly filter samples of 

Al obtained during downslope winds 

at MLO using a high-volume aerosol 

sampler (from Parrington et al., 

1983) . 
, '. 

,,,,', lilO'. 

100" 

/ 1lC)" • , ..... ",'~ 

100' • '!IO" "10' • 

"0" 

_1.0 .." WB TR"....,,"''''' .0."", ,PI! ",' ,"", 

-,' ;::.. "' ... -;.?-; 

~ .... - ~ ...: '--. 

" 

,l!J'r' 

Ill>' • l;J)" 

"0"'. '00' [ ". .'. '6(>" " ,. , 10' S 140" 

teo' • '00" 

Figure 65.--Back trajectories arriving above MLD along the SOO-mb surface for 

April and Hay 1979-1982. 

are used for comparison. The SOD-rub isobaric surface is considered representative of midtropospheric conditions for this period. 

Ensembles of back trajectories from HLO for April and Hay 1979-1982 are 

plotted in fig . 65. The trajectories were computed according to the method 

described by Harris (1982). In 1979 the transport paths from the west show a 

relatively direct route from the Asian deserts, the eastern parts of which are 

at -40 0N, 1000E . These trajectories have cyclonic curvature for the first 2-

3 days of transit off the Asian coast . During the last 2-3 days, as they approach Hawaii, the curvature is anticyclonic. The cyclonic curvature on the 

western part of the trajectories indi cates associated storminess in the source 

region. One would also expect that the air parcels arriving in the region of 

Hawaii are descending from high er levels following an anticyclonically curved 

path from the northwest . 

In 1980 and the subsequent 2 years, the westerly trajectories that track 

to Hawaii seem to originate in a region to the south of the deserts for a 

larger percentage of the time. The midtropospheric flow is often zonal, yet 

the transit times are longer in the latter 3 years than in 1979 . The trajectory model indicates that the air parcels are moving relatively slowly while 

making the sharp anticyclonic curve just before reaching the islands . Overall 

the indicated paths from Asia are longer than the paths in 19 79. The reduced 

96 
occurren ce of curved trajectories off the Asian continent indicates a lower 

frequency of storms for this period. The trajectory ensembl es for 1980-1982 

clearly indicate [ewer storms and longer transit paths to Hawaii originating 

to the south of the main Asian deserts. These three features are probably 

related and ma y explain the decrease in the dust concentration that occurred 

from 197 9 to 1980. 

Although sample s of 7-day duration are very useful in evaluating monthly 

a nd seasonal varia tions, the form of presentation in fig. 64 does not show the 

intermittent nature of the du st episodes. Filter samples taken on a mu ch 

s horter time scale (Darzi and Winchester, 1982a) and the analysis of wind, 

aerosol, and ozone measurements (Herbert el al. , 1982) have s hown the typical 

dust period to last 18- 36 hours . In one particular case that was reported to 

have lasted a week, a wi nd change occurred midperiod causing dusty air to 

recirculate from the east. Generally the dust-free periods have concentrations of crustal material that are representative of typical s umme r or fall 

values . Parrington et al . (1983b) contend that if sampl es of s horter duration 

were taken, the pea k co nce ntrati ons would be mu ch larger. Dust-free pe riod s 

during the spring have been found to correspond to trajec tories from the 

southwest. A relatively large number of the April and May trajectories originate well south o f the east Asian deserts or in the equatorial western Pacific. The spring traj ec t o ry e nsembles c l early s how that air arriving ove r 

Hawaii is not influenced by the No rth Ameri can continent. 

4.11 The Ph otovoltaic PO\,e r System at S~10 

The majority of the "urk on the PV power system for SMO in 1982 invo l ved 

the pro curement, construction, and testing of the compone nts of the sys tem. 

This project i s funded in part by the DOE Fed eral Photovoltaic Utilization 

Program. From t he six respondees to the second issue of the Request [or Proposal (NOAA RFP 54 -81 ), the source evaluation board selected So l arex Corp ., 

Rockvill e , Md., as the s uppli er for the entire sys t em. After further cost 

eva luation, the government chose to purchase the batteri es directly from the 

supplier recommended by Solar-ex and to provide i nstallation. It \.las also 

de termin ed to be less expensive for the government to procure t he materials 

and cons truct th e PV array stands directly, usi ng local Polynesian hardwoods . 

Detailed plans and specifications were provid ed by Solarex. All outside " iring and internal installation were also done by government employees. By 

March 1982 the details of the agreement had been resolved and a co ntract was 

signed . 

One of t he main evalua tion criteria co ncerned the me thod proposed for 

battery charge regulation and protection. A typical voltage regulator establishes a ceiling voltage when the batt e r y approaches full c ha rge . This method 

of charge cont ro l is rela tively i nef ficien t because a battery accepts e nergy 

only as the voltage is rising. A better me t hod of charging, especially at 

st a te-ot-cha rge levels between 85% and 100%, is one where the vol t age oscil -

lates be t ween t"o seLpoints. Sola r ex suggest ed just s uch a system cal ling it 

"pump- charging." The high setpoint is s ubstantia lly above the ceiling vo ltage 

of a typical regulator. IYhen this voltage is reached, a module is shed from 

eac h string in th e PV array , t hu s r educing the voltage on the battery. When 

the voltage drops to the lower se tpoint, the array output i s restored to ful l 

vol tage, ca usi ng the battery voltage to rise. Additional energy is pumped 

i.nto the battery as the voltage rises. IYhen the voltage rises to the high 

97 
Honth 

Jan 

Feb 

tla r 

Apr 

tlay 

Jun 

Jul 

Aug 

Sep 

Oct 

Nov 

Dec 

Table 31.--Honthly average ratios of the daily insolation on a 

tilted surface to that on a horizontal surface, for 1982 

Variable 

14° tilt , 14° tilt, tilt, 

this study Jordan and Liu (1977) this s tudy 

0.87 0 . 93 0 . 94 

0.91 0.97 0.94 

0.95 1. 06 0.95 

0 .96 1. 15 0.97 

W' 1. 22 tp', 

1 . 10 1. 26 1. 23 

1. 08 1. 24 1.22 

1. 01 1. 17 1.03 

0 . 97 1. 08 0.93 

0.92 1. 00 0.92 

0.98 0 . 96 1.04 

0 . 94 0 .91 1. 04 

"'tl = missing data . 

setpoint , the module is shed again, initiati ng another pump cyc l e . This is 

the preferred method of battery charging because in addition to bei ng the most 

effic i enL , it drives the battery br iefly to a vo ltage high e no ugh to ca use the 

electro l yte to emit gas sl i ghtly . This cond ition eliminates electrol yt e stratification, ensuring efficient charging and good battery life . 

The system consists of six major comp onents . (1) The PV array is made up 

of 10 strings of 10 modules each ; 1 or 3 modules ca n be s hed from each string 

to control the voltage. The modules are Solarex no. HE- 80 with a peak power 

current of 3 . 8 A at about 17.5 V DC . The modules are mounted i n five subarrays of 20 modules each (2 . 4- x 6 . 1-m panels at a height of 3.7 m) . The panels cover a total area of about 75 m2 . (2) The battery bank co nsists of 10 

C & D type 6ZP75 -1 3 deep discharge batteries. The bat t ery cel l s have a nominal 5 10- Ah capaci t y with a 16-h rating. The bank physically comprises 10 

identical six - cell modules co nnected i n series. Hyd roge n recombiners will be 

in s t a l led on each cel l. (3) The i nverter is a 2-kW, continu ous (3 kW for 

2 seconds) capaci t y unit manufactured by Abac us, no . 423-4H3-120. (4) A So l a -

rex model ACR - 6 con trol l e r, with t wo -stage PV module shorting, controls the energy flow to the batteries. (5) A battery charger , Cust om Power no . BCI - 6020 , 

suppl ies 20 A at 120 V, nominal, "'hen prolonged cloudy periods significantly 

reduce inso l ation . (6) A transfer switch, to s hift the load t o island power 

in case of inverter failure, is built into the system . By December 1982 all 

major components had been purchased and tested. The entire system will be 

tested and installed in April and Hay 1983 . 

Early in 1981 two pyranometers were installed on tiltable stands . One 

stand was fixed at an angle equal to t he latitude of the station, _14°. The 

other was cha nged monthly between angles of -10° and 35° . The ratio of the 

daily in solation on the tilted pyranometer to that on a horizontal pyranometer 

was computed and averaged by mont h (ta bl e 31) . Mea s urements for 1982 s how the 

greatest e nh ancement during the SouLhern Hemisphere winler month s of June and 

98 
July. Except for the summer months , the theoretical estimates of Jordan and 

Liu (1977) overestimate the enhancement resulting from tilting. Improper 

t reatme llt of c l oudiness is probably the cause of this error. On a month-bymonth comparison , the values measured in 1982 are within a percent or two of 

those measured in 198 1 (Bodhaine and Harris, 1982, p. 103). Becaus e changing 

t he Lilt of 100 photovoltaic panels requires mu ch effort , a schedule requiring 

f our c ha nges per year will be used with the PV system . 

4 .1 2 Atmospheric CO 2 Measurements Aboard R/V DISCOVERER, 

May -June 1982 

4 .1 2. 1 I ntroduction 

In ay and June of 1982 the IT G Gro up participated in a NOAA/P~IEL project , Marine Si nks of Atmospheric CO 2 , aboard the R/V DISCOVERER in the equatorial and northern Pacific Ocean . J . Cline used a portable sampling unit to 

co llect 36 pa irs of flas k samples in 500 -cm3 gl ass flasks for CO 2 ana l ysis. 

The cruise track and locations of sampli ng are shown in fig. 66 . 

The principal objective of t he GMCC sampling program was Lo obtain atmospheric CO2 data from remote mar i ne regions for comp arison with t he G~ CC CO 2 

flask network data . Since land-based stations may be influe nced by l ocal 

anthropogenic or bi osp her ic SOur ces and /or sinks of C021 the shipboard data 

are useful in assessing the suitability of these stations for obtai ning regional or background atmospheric CO2 daLa. Also, the s hipboard daLa are valu -

abl e for determining atmospheric CO2 gradients over this region of the Pacific 

Ocea n and identi(ylllg possibl e marine sources and sinks of CO 2 , 

t---~---f---~----------------~~ 

99 

Figure 66 .--The cruise track and 

sampling locations (circles) of the 

1982 cruise f l as k sampling program 

aboard R/V DISCOVERER. Three GMCC 

CO 2 flask sampling sit es are shown 

for reference . 
4.12.2 Results 

The resulLs of the CO 2 analyses performed on the semi automati c NDIR CO 2 

flask analysis apparatus (Komhyr et al. , 1983) in Boulder are presented in 

table 32. The CO 2 concentration given is the average for a pair of simultane -

ously filled f l asks. In two cases (indicated by asLerisks) th e pair difference was greater than 0 . 5 ppm, and t he higher val ue was rej ec ted as being 

Table 32. --Date, position and CO 2 concentration for 

R/V DISCOVERER 1982 cruise samp les 

Latitude Lo ngitud e CO 2 

Date DaY (degrees) (degrees) (ppm) 

14 Hay 134 O.OON 159.75\. 342.22 

15 tlay 135 O.OON 165 .1 7W 34 1. 82 

17 tlay 137 O.OON 170 . 28W 342 .1 3 

17 tlay 137 O.OON 175 . 00W 342 . 08 

18 tlay 138 O. OON 180.00 342.11'" 

19 tlay 139 O.OON 175 . 00E 342 . 02 

20 tlay 140 O.OON 170.00E 34 1. 95 

29 tlay 149 16.00N 165.03E 344 . 96 

30 tlay 150 16.00N 165 .03£ 344 .66 

31 tlay 151 17.27N 165 . 03£ 344 . 77 

1 J un 152 20.95N 165.IOE 344 .59 

2 J un 153 20 . 97N 165.03£ 344 .96 

3 Jun 154 22 . 25N 165.02E 344. 75 

4 Jun 155 26 .10N 165.08£ 345 .09 

5 Jun 156 25.97N 164.92E 344 . 36 

6 J un 157 28 . 02N 165.03£ 344 .43 

7 J un 158 30 . 05N 165.12£ 344.63 

9 Jun 160 32.00N 165 .05E 344 .15 

10 Jun 161 35 . 00N 165.00£ 344 . 28 

12 Jun 163 34 . 77N 164 . 65£ 344 .41 

13 Jun 164 38 . 00N 165.00£ 343 .73 

14 Jun 165 38 . 93N 165 .08£ 342 .99 

15 Jun 166 41 . 9 7N 165 .05£ 343 . 30 

16 Jun 167 42.47N 165.03£ 34 1. 27 

17 Jun 168 45. 32N 167 . 25£ 339.57 

18 Jun 169 45.32N 167 . 37£ 342 .1 2 

19 Jun 170 47.67N 171 . 02£ 341. 56 

20 Jun 171 342.26 

21 Jun 172 49 . 98N 175 .00E 34 1. 05'" 

22 Jun 17 3 51 .58N 179 .53\. 343 . 25 

23 Jun 174 53 . 02N 171 . 32\. 342 . 79 

24 Jun 175 53 . 93N 160.73W 341. 12 

25 Jun 176 53 . 70N 151.38W 342.29 

26 Jun 177 52.72N 142.57W 340.66 

27 Jun 178 51 .2 3N 134.68W 342.69 

28 Jun 179 49.28N 127 .58W 341. 75 

*The pai r difference for two fla s ks was greater than 0 .5 ppm, and the 

higher value was rejected . 

100 
~ 355· 

~ . ~ 

U 

"' Z 

~ J5e · 

U 

a: 

'" ~ 

ISC OV£~£R 

COLD BAY 

CUIlM 

SAMOA 

I.e"=<! 

W). s - ~_ 

~ .' -.-J,,/ - '- ~ .: '\' .. ~ '" - ~ - - J . " (AY< , l: 

Q. 

a. 

N 

8 J3S~--.--

.~ '" ~ ~ 

D~Y OF YEAR 

Figure 67.--C0 2 vs. DaY 1982 for the 

data in table 32 (0). Also shown 

for comparison are GMCC flask data 

from Cold Bay, Guam, and Samoa. The 

NCAR point is from a mlcc analysis 

of a stainless steel flask sample 

obtained by L . Heidt of NCAR. The 

dashed line consists of data extracted from fig. 8, sec . 3.1 . 

probably contaminated through a leaking flask stopcock. The quality of the 

samples appears to be quite good, which is large ly attributable to the conscientious methods of the sample taker. The cruise data are plotted vs. DOY 

in fig . 67, along with GMCC flask network data for comparison. 

Essentially no atmosp heri c CO 2 gradient exists along the Equator from 

1600W to 1700E. Also, the equatorial concentration lies roughly midway between that at Samoa ( 14°S) and Guam (13°N) at this time of year. This gradient is unusual compared with previous years in which the northern tropics 

showed a higher CO 2 concentration because of the upwelling of CO 2 -rich waters 

(sec. 3. 1). The lower northern tropical concentrations during 1982 were probably caused by reduced upwelling associated with the unusually intense E1 Nino 

event. 

Although no GMCC samples were collected between the Equator and 16°N 

because of following winds, several sample s were collected along this track 

f o r L. Heidt of NCAR. One of these samples, collected at SON, was not contaminated and contain ed 34 4.43 ppm of CO 2 , This poinL, plotted in fig. 67 as a 

filled-in circle, indicates the existence at this time of a gradient of -3 ppm 

between the Equator and SON, the probable late spring location of the ITCZ 

(Bortniak, 1981). This s ugge s ts that the annual average interhemispheric 

gradient of 3 ppm is due to very slow mixing across the 1TC2 barrier during 

most of the year. 

Th e atmospheric CO 2 co nc entration mea s ured aboard R/V DISCOVERER (DSC) 

along 16SoE from 16°N to 42°N (DaY 149-166) is in good agreement with that 

measured at Guam (GMI) during the same period (C02nsc = 344 .4 ppm, N = 16; 

C0 2GMI = 344.0, N = 4). That the agreement is good over such a range of latitude is partly due to the latitudinal gradient of CO2 being a t its minimum at 

this time of year in the Northern Hemispher e (see sec. 3. 1), 

A note on the sample data sheet indicates that the Subarcti c Front, a 

boundary between warm midlatitude and cold northern water) was crossed on 

DaY l6S . This c rossing was followed by a s harp drop in atmospheric CO 2 concentration of -3.S ppm by DaY 168 (4S0N) . Comparisons with s imultaneous pC02 

measurements of the surface seawater made by C. Wong will be useful in interpreting this sudden drop in atmospheric CO 2 con c entration. 

101 
From 165°E to 128°W (DOY 166-179) through the North Pacific, the atmospheric CO 2 concentration was quite variable, but it is still in good agreement 

with the few values available from Cold Bay, Alaska, during the same period 

(C02DSC = 341.8, N = 14; C0 2CBA = 342.1, N = 3). The variability is probably 

due to the proximity of the ship to the Aleutian Islands, where the CO 2 concentration may be influenced by the local terrestial biosphere and short-term 

atmosphere-ocean interaction. 

The dashed line in fig. 67 represents data extracted from fig. B 

(sec . 3.1), a three-dimensional surface that is a smoothed interpolation of 

the zonally averaged CO 2 concentration vs. latitude and DOY, for the sea-level 

stations of the GMCC flask sampling network. The agreement of the cruise data 

with the surface is remarkable both in shape and actual concentration, supporting the representativeness of the flask sampling network. The systematic 

difference of <1 ppm is because the surface is zonally averaged, the Atlantic 

values being generally lower than the Pacific values. 

From these results it is apparent that high-quality CO 2 data can be obtained by flask sampling aboard ships. It is also clear that stations such as 

Guam and Cold Bay are in fact suitable sites for measuring background CO 2 

concentrations representative of large regions. However, a network of landbased stations is not able to locate the sharp CO 2 gradients that were found 

between the Equator and 50 (ITCZ) and in crossing the Subarctic Front. This 

information, which can only be obtained by shipboard sampling, is significant 

and will be useful in understanding the global distribution of CO 2 and the 

natural variability of the global carbon cycle. 

Our interpretation of these data will be extended by considering various 

meteorological and oceanographic parameters, such as location of the rTCZ, sea 

surface temperature, pC02 in the sea water, and large-scale atmospheric circulation. Also, the results from this cruise have encouraged participation in 

several cruises to be made in 1983, including a circumnavigation of Antarctica 

by the USCG Icebreaker POLAR STAR . 

4.13 Airborne Optical Measurements of the El Chichon Cloud 

The potential climatic impact of the enormous El Chichon volcanic eruption in 1982 attracted considerable attention from climatic specialists, the 

general scientific community, and the general public. Consequently, much 

research effort has gone into attempts to quantify and describe the radiative 

effects of the long-lived stratospheric cloud. Previous theoretical work 

suggested t hat an eruption of this magnitude (stratospheric impact) would 

sufficiently impact the global radiation balance to cool the lower troposphere 

by a few tenths of a degree Celsius (e.g., Toon and Pollack, 1980). 

Application of radiative transfer calculations to, and subsequent verification of, climatic effects relative to the major stratospheric aerosol event 

resulting from EI Chichon, is complicated by the spatial distribution pattern 

of the debris material. Sustained uneven distribution of the material would 

invalidate one-dimensional models that assume uniformity for global effects. 

Additionally, two- or three-dimensional models that could properly account for 

the spatial distribution of the debris material also need to include atmospheric dynamics that coul d respond to the perturbed radiative forcing. 

102 
As an initial step toward identification of the climatic effect of the EI 

Chic hon stratospheric debris, the GNCC ARl'1 group participated in three survey 

flight series sponsored by NASA. The flight series were designed to establish 

the latitudinal extent and variability of the cloud's optical properties as 

determined from remote measurement of its optica l effects on sunlight. The 

flights were flown near the top of the troposphere so that the measured effects on the direct solar beam would only be influenced by the stratosphere 

and above. Spectral solar ex tincti on was measured on all three flight programs, while 2rr-sr diffuse-to-total flux ratios and total reflectance were 

measur ed on only one . The remainder of this report discusses the results and 

implications of the direct solar beam extinction measurements made on these 

flights. 

Spectral aeros ol optica l depths for the three flight series were derived 

from the spectral solar extinction measurements obtained by hand-opera t ed 

sunphotometers on the aircraft. The results for one spectral wavelength are 

shown in fig. 68 where the flights' date s are also indicated. The flights 

were in the general longitude range of the continental United States. Details 

of thes e observations and subsequent analysis and interpretation were given by 

Dutton and DeLuisi (1983b). 

The main features shown in fig. 68 are the relative maximum in the Northern Hemisphere tropics, the local minimum indicated at 25°N in flights 2 and 

3 , and the increase in optical depth at the northern end of the flights. The 

tropical maximum corresponds to the original cloud, which was observed by 

satellite to remain confined to this latitude region for several months following the eruption. The satellites were not designed to quantify the shortwave optical properties of the cloud, however. Thp hi gh values in the north 

were unexpected and raise some questions about the transport mecha nis ms. The 

spa tial extent of the cloud and relatively high values of optical depth 

(stratospheric background is close to 0.005) 8-10 months after the eruption 

provide useful information about the extent of the effect of the cloud on the 

global shortwave radiation balance. 

An important conclusion from these observations is that significant latitudinal variations existed at least up to 8 mon ths after the eruption. If 

there are significant impacts by the cloud on climati c radiative forcing, the 

perturbations will have definite latitudinal variations. 

'10<'12-",o.!1 ~ 'Xl-: . • ) 

1 .o.c!2 ,,.'11 "0 '30':1' ~~ 

'" J n,J."u~re<>a1 ~~'S :. I>·) - ' 

'" 

'" ,J 

'" "--', 

'" ','W 

" " '" " " '0 So~,~ " " LaLtude 

-1 

'" " r~ orln " " 

103 

Figure 68.--Aerosol optical depth 

above the aircraft for three NASA 

flights at 500-nm wavelength. 
4.14 MLO Normal Incidence Irradiance Record 

eas re ts of normal incidence solar irradiance have been made at MLO 

since 1958. The instruments and methods used have been described in past GMCC 

Sununary Reports, and by Ellis and Pueschel (1971), ~lendonca et a1. (1978), and 

Bodhaine et al. (1981). 

In the solar irradiance record , several decreases in normal incidence 

flux have been observed after explosive volcanic eruptions . By inference, the 

decreases in solar irradiance at MLO have been used as an indirect measure of 

the transport, intensity, and duration of stratospheric vo l canic de b ris ove r 

MLO and the equatorial Pacific. The validity of this assumption was confirmed 

after Hoyt (1979) and Bod h aine et a1. (1981) documented that the magnitude and 

variability of the seasonal annual c hange in solar irradiance caused by tropospheric attentuation above ~lLO was too small to account for the long-term 

c hanges observed in the record. Other contr ibutions to secul ar cha nges in 

tropospheric attenuation at MLO have been shown by Bodhaine and Pueschel 

(1974), Mendonca et al. (1979), and Shaw (1980) to be very s mall and barely 

detectable, if at all. Consequentl y, the major cause of secular cha nge i n the 

normal incidence solar irradiance aL ~tLO has been attributed to explosive 

volca n ic eruptions. 

Figure 69 s hows an updated plot of ye arly means of normal incidence solar 

irradia nce for 1958-June 1983. Values are plotted for irradiances obtained at 

relative air masses of 2, 3 , 4, and 5 during cloudless skies. Only morning 

values are used because they are more representative of the undisturbed atmosphere above MLO. tleasurements in the afternoon are subject to a mountain 

upslope circulation that carries moisture and clouds to the observatory a nd 

makes the afternoo n measurements responsive t o local cond itions. 

llOO,------ - - - - - --- --- ---, 

IIXll 

700 

i 

i 

- "" E ! , 

,f i 

~ 

500 

Figure 69.-- Normal incidence irradiance values fo r relative air ma sses 

2, 3, 4, and 5 (top to bottom) at 

MLO. Irradiances are averaged for 

the year du r ing cloudless sky condi -

tions as the Sun rises in the morning. Data for 1983 include only 

January to June. 

104 
The normal incidence irradiance values are also plotte d after they have 

been cor rected for instrument drift u s ing the method described by Robinson 

(1982). Previously the data were presented as an apparent atmospheric transmission. Robinson's method allows for exami nation of decreases in actual 

sola r irradiances after each volcanic episode and in relation to the apparent 

atmospheric transmission changes . 

In fig. 69 the data from the different relative air masses (2 - 5 from top 

to bottom) track each other well. Th is is to be expected, but the fact that 

every rise and dip is mirrored at all air ma sses also attests to the uniformitv of the atmosphere in the mornings at ~lLO. 

Wh en the pre-Agung years 1958-1962 are used as a base t o determine the 

magnitude of the decreases in normal incidence flux, a comparison can be made 

between the decreases in apparent transmission described by Ellis and Pueschel 

(1971) a nd Mendonca et a 1. (1978) and the decreases in normal inciden ce flux. 

Table 33 s hows the comparisons . In fig. 69 and table 33 several features are 

evident. The decrease observed after the eruption o f E1 Chi chon in April 1982 

is by far the largest observed in the 26-yr record. Even up to 14 months 

l ater (the data for 1983 include only January to June) the normal incidence 

flux and apparent transmission are lower than after the Agun g eruption. Although the Agung eruption as measured at MLD shows a s maller decrease in normal incidence flux compared with E1 Chi chon, the recovery time is long, and 

near-background irradiance values are not observed until 1970. It s hould be 

stated that t he long recovery time cou ld have been influenced by other e rup -

tions that may have occurred close in time to Agung and Awu . These could have 

added debris to the stratosphere during the period 1963-1967 (Mendonca e t a1., 

19 78) and prolonged the return to background. The decrease after De Fuego is 

the smallest observed that can be attributed to a particular volcani c eruption 

and is s hort lived. 

A hemispheric ci rculation shift and corresponding hi gh irradiance values 

a t MLO in 19 76 and 1977 s h ould be noted. The irradiance values measured during the winter of 1976-1977 and 1977-1978 were the hi g hest recorded at MLO for 

Table 33.- -Percent decrease in apparent transmission 

and normal incidence flux at lLO for five selected periods, 

using the pre-Agung 1958-1962 period as a base 

Apparent Normal incidence fluxt 

EvenL 

Agung 1963-1965 

Awu 196 7 -19 68 

De Fuego 1974-1976 

El Chi chon 1982 

Jan-Jun 1983 

t ransmiss n~', 

(%) 

2 

2 

9 

4 

2 

2 

2 

I 

17 

8 

3 

4 

4 

2 

20 

13 

(%) 

4 5 

5 

5 

3 

30 

16 

7 

7 

3 

34 

23 

Aver. 

4 . 5 

4.5 

2.3 

25 . 3 

15.0 

*Apparent transmission decreases are averages for relative air masses 2- 5, 

obtained from Mendonca et al. ( 1978). 

tNormal incidence flux decreases are give n at relative air ma sses 2-5 . 

105 
the entire record. The daily log sheets at MLO show unusually clear and dry 

periods over these winters. ~Iore than 82% of the mornings during these winLers were clear, to the extent that a complete set of solar irradiance measurements was obtained. 

When the apparent transmission decreases are compared with the irradiance 

decreases, a one -lo-one agreement is observed at a relative air mass of 2 

until the EI Chichon eruption. For EI Chi chon, the percent decrease in actual 

irradiance is about twice that determined by the apparent transmission record 

at a relative air mass of 2 . Normal incidence irradiance values at relative 

air mass 2 (zenith angle 60°) are used as an approximation for the daily total 

of irradiance received during a cloudless day near the Equator. The relationships between the apparent transmission decreases and normal incidence irradiance decreases for the different relative air masses are shown in table 33 . 

Lower Sun angles (larger air masses) give larger decreases. 

The apparent transmission record and the normal incidence irradiance 

record at MLO both indicate decreases after explosive volcanic eruptions, with 

recovery times lasting from a few months to several years . The eruption of EI 

Chichon volca no has resulted in the largest decrease in normal incidence flux 

measured at MLO si nce observations began in 1958 . As of June 1983 the atmo sphere over MLO was still more turbid than at any time after the Agung eruption 

in 1963, even after debris from EI Chichon had already spread around the 

world. ~Ieasurements will continue to be made to monitor the lifetime, evolu -

tion, and spread of the cloud over MLO . 

106 
5. COOPERATIVE PROGRAMS 

5.1 tleasurements, Sources, and Sinks of Atmospheric Benzene and Toluene 

5. I. I Introduction 

R. A. Rasmussen and M. A. K. Kil alil 

Oregon Graduate Center 

Beaverton, OR 97006 

Benzene (C6" 6) and toluene (C7"8) are short-lived trace gases in the 

atmosphere that arise from a number of natural and anLhropogenic sources . 

Their common sources include automobiles, so lvent uses, chemical manufacturing, diesel fuel, forest fires, refuse combustion, petroleum, la cquer and 

polymer manufacturing, gasoline vapor, sewage treatment, toba cco smoke, landfills, and possibly natural sources (Graedel, 1978). We recently found that 

burning wood, such as for heating homes, also produces benzene and toluene. 

The main atmospheric removal process for both compounds is believed to be 

reaction with tropospheric DH radicals, resulting in atmospheric lifetimes on 

the order of weeks for bellzene and a few days [or toluene. On a global scale 

Lh e concentration of benzene and particularly of toluene is dependent on nearby so ur ces . 

During the past ye ar and a half we developed a gas chromatographic system 

(GCfFID) with a capi llary co lumn to measure the concentration of benzene and 

toluene along with dozens of other hydrocarb ons in the range of parts per 

trillion by vol ume . The system has a detection limit of about 5 pptv for benzene and toluene, anu a precision of ±10%. The analytical system is rlpsrribed 

in more detail by Rasmuss en and Khalil (1983). 

Over the last year or so air samples were co llec ted in stainless steel 

flasks at nine sites, including several supported by our cooperative agreement 

with GtICC. The sampling containers and collection procedure s are designed to 

keep the samples free from contamination and Lo allow extended storage (Rasmuss en and Khalil, 1980). Laboratory studies have verified that concentrations of benzene, toluene, and other hydrocarbons do not change over periods 

of s torage much longer than usually encountered in this experiment. The measurements at Cape Meares , Oreg., were ba sed on large -volume, high pressure, 

cryogenically collected air samples, using sampling co ntainers that are even 

better in preserving air than the smaller flasks used at the other, more distant sites. 

5.1.2 Data 

Table 34 gives the benzene and toluene data obtained so far, showing 

daily average concentrations. Often two or three smaller air samples collected on the same day were combined before analysis . Sometimes several sampl es collected on the same day were analyzed separately, in which case the 

concentrations obtained were combined to form a daily average. The distinctive features are analyzed and dis cussed by Rasmussen and Khalil (1983). 

Samples obtained from SPO revealed no Significant levels of benzene and toluene. Following are some conclusions on the sources, sinks, and distribution 

of benzene and toluene based on the collected data. 

107 
Table 34.--Benzene and toluene concentrations 

Date Concentrations 

(pptv) 

1982 

22 ~la r 294 73 

26 213 BDL 

29 245 96 

30 263 49 

8 Apr 220 5 1 

12 256 49 

14 250 27 

20 216 3 1 

24 230 BDL 

26 212 17 

7 ay 145 BDL 

13 123 BDL 

15 97 BDL 

18 80 BUL 

24 89 BOL 

1 June 67 36 

10 42 3 1 

14 53 75 

26 38 28 

I Jul 44 BDL 

5 29 29 

12 BOL 33 

22 BOL BOL 

29 34 BOL 

7 Aug 41 44 

9 24 BDL 

21 142 15 1 

31 BO!. BO!. 

6 Oc t 90 27 

14 305 393 

23 10 1 24 

29 182 ImL 

I Nov 171 94 

22 19 7 68 

3 De c 164 68 

14 195 BOL 

20 182 84 

27 194 95 

198 3 

14 Jan 245 117 

2 1 313 184 

24 280 235 

31 252 136 

8 Feb 270 200 

IS 232 138 

22 269 102 

II ~Ia r 251 7 I 

13 276 120 

6 Apr 235 48 

7 282 44 

9 229 31 

14 209 56 

15 165 BD!. 

19 179 BD!. 

20 132 BD!. 

2 1 191 22 

27 143 BD!. 

4 ~Iay 85 BOL 

10 164 BDL 

17 76 BDL 

Cape ~Ieares ! Oreg. (45°N) 

Date Concentrations 

1980 

10 Dec 

3 1 

1981 

IS Jan 

25 Feb 

II ar 

18 

1 Apr 

17 

29 

13 ay 

27 

17 J un 

1 Jut 

15 

29 

19 Aug 

2 Sep 

16 

30 

1 Ocl 

14 

28 

20 Nov 

2 Dec 

16 

30 

1982 

13 Jan 

3 Feb 

24 

10 ar 

24 

7 Apr 

21 

19 tlay 

16 J un 

14 Jul 

28 

II Aug 

22 Sep 

24 Nov 

30 

8 Dec 

29 

19 83 

(pp tv ) 

701 

160 207 

184 234 

196 117 

165 87 

531 7 12 

IBO 42 

224 224 

96 88 

108 36 

61 37 

34 BDL 

79 127 

60 66 

19 2 1 

601 

29 26 

17 1 254 

85 6 1 

247 237 

155 95 

410 575 

587 960 

357 472 

514 754 

313 334 

415 552 

285 289 

448 596 

234 220 

140 53 

401 420 

155 89 

83 20 

23 28 

68 

165 140 

58 BDL 

269 192 

291 297 

166 139 

144 IDS 

300 156 

12 Jan 201 147 

113 

98 

254 

3 1 IB4 

11 Feb 16 7 

23 254 

9 ~Iar 207 264 

NWR (400 N) 

Date Co ncentrations 

1982 4 ~lay 

14 

18 

25 

2 Jun 

8 

16 

22 

29 

6 Jut 

13 

20 

3 Aug 

10 

17 

27 

3 1 

8 Sep 

14 

23 

28 

5 Oc t 

12 

26 

2 Nov 

9 

16 

7 Dec 

12 

19 

28 

1983 

4 Jan 

8 

16 

22 

29 

5 Feb 

13 

20 

26 

20 a r 

25 

I Apr 

12 

26 

(pptv) 

36 29 

76 31 

40 33 

54 15 

BDL BOL 

39 29 

36 BDt 

43 34 

28 28 

28 BOL 

55 31 

34 5 1 

33 34 

BOL 49 

29 50 

182 71 

155 30 

134 22 

140 20 

78 20 

73 23 

70 22 

63 22 

74 35 

94 44 

210 BOL 

52 BDL 

491 689 

4z I3UL 

113 37 

445 

125 44 

93 38 

285 320 

226 11 9 

152 88 

180 65 

89 23 

134 44 

129 60 

253 200 

200 168 

156 15 

24 1 303 

232 412 

108 

5~IO (14 0 5 ) 

Date Co ncentrations 

(pptv) 

1982 

17 tlay 

28 

5 Jun 

12 

22 

28 

29 

10 Jut 

17 

26 

6 Aug 

25 

30 

10 Sep 

25 

6 Oct 

9 

17 

1 Nov 

13 

27 

6 Dec 

8 

11 

17 

18 

25 

1983 

1 Jan 

8 

15 

19 Feb 

26 No'lr 

16 Apr 

23 

30 

24 

BDL 

114 

46 

BDL 

21 

47 

63 

BDL 

BDL 

BDL 

229 

207 

136 

167 

90 

150 

93 

88 

73 

88 

85 

40 

127 

39 

43 

62 

55 

BDL 

57 

79 

3 1 

11 

BDL 

119 

BDL 

BDL 

22 

39 

50 

34 

59 

41 

37 

115 

4 3 

2 1 

39 

29 

33 

14 

14 

20 

BDL 

BDL 

16 

BDL 

BDL 

BDL 

21 

21 

33 

BDL 

28 

12 3 

88 

12 

8DL 

8DL 
Table 34.--Benzene and toluene concentrations-- Continued 

tlLO (200 N) WFtI (44°N) Tasmania (42°5) Ca~e Pto, S.Africa (35°5) 

Dale Concentrations Dat e Concentrat ions Date Concentrations Date Concent.rations 

(~ptv) (I2Elv) (I2Elv) ----'.I>~ CsHu C7C8 CSH6 C7C8 CsHs C7C8 CsHs C7C8 

1982 19B2 1982 1982 

-----zs Apc 66 BDL B Aug 160 253 15 tlay 41 2B 24 Nay 30 59 

6 Hay 22 22 9 90 105 27 179 167 2 Jul 30 43 

15 73 SOL 10 73 19B 2 Sep 56 16 3 Aug 33 52 

19 339 21 11 41 97 7 53 BDL 1 Sep 304 BDL 

26 33 13 12 121 834 9 Nov SOL SOL 2 Nov 115 SOL 

2 Jun 22 5 13 84 92 16 8DL SOL 8 64 110 

9 108 36 19 170 152 25 BDL BDL 

16 38 2 Sep 397 254 6 Dec 71 26 1983 

23 49 3 63 9 395 103 15 reb BDL 3B 

30 SOL SOL 10 781 256 1983 18 Apr 102 243 

7 Jul 17 BOL 13 278 79 ---v; Jan SOL SOL 

14 SOL BDL 21 213 205 28 tla r 11 BDL 

29 317 11 6 1 Oct 290 173 

4 '\U8 3B 7 , 216 14 3 

12 SOL BOL 22 162 43 

25 217 32 27 185 72 

1 Sep 151 20 14 Dec 343 160 

B 69 27 

6 Oct 118 28 19B3 

15 173 SOL 25 Jan 543 62B 

20 23 BDL 3 reb 591 B04 

27 B4 BDL 4 311 22B 

3 Nov 76 BDL 9 233 130 

10 140 19 10 195 11 6 

1 Dec 53 BDL 21 3B5 257 

B BDL SOL 1 tla r lB3 B1 

15 65 SOL 5 191 BDL 

23 BDL 39 7 138 B5 

29 271 SOL 10 430 44 

14 166 95 

1983 1, 228 93 

7 Ja n 91 SOL 16 273 76 

20 Apc SOL SOL 17 339 1BB 

27 3B 27 

BDL = Bela ... ' Detection Level 

5.1.3 Discussion 

The data s how that benzene a nd toluene concentrations are variable i n 

both space a nd time . Generally t he concentrations observed reflect the effects of local so ur ces . Transport over l ong distances is possible at high 

latitudes in wintertime when OH levels are extremel y low. Transport of these 

gases from one hemisphere to the other is not like l y to occur because of the 

hi gh l evels of OH that are believed to ex ist in the tropics and the sl ow latitudinal mi xing at these latitudes. For benze ne a nd toluene seasonal varia -

tions of OH ca n have enormous effects on the ambient concen trations . Su ch 

effects have been observed, as shown by Rasmussen a nd Khalil ( 1983) . 

The lifetimes of these gases depend primarily on the local and seasonal 

conce ntrations of OH. ~Ieasur ed reaction rate constants are about 1 . 2 x 

10- 12 mole cule-s cm- 3 for be nz e ne a nd 6 . 4 x 10- 1 2 mole cule-s cm- 3 for t ol ue ne 

(Graedel, 1978; Hampson , 1980; Perry et a!., 1977) . The l ocal lifetime may be 

estimated by 1 ~ KIOH l. If typical average atmospheric OH concentrations are 

109 
(0.5- 1.0 ) x 106 , then the typical lifetimes of benzene and toluene will be 

10- 20 days and 2- 4 days respectively. Since OH is believed to exist on!§ 

during daytime, the OH levels would have to be (1 - 2) x !O6 molecules cm 

during the day for the lifetimes calculated above to be effective. At high 

latitudes, the seasonal variation of solar radiation flux and water vapor ma y 

cause the OH levels to be an order of ma gnitude lower in wi nter , thus allowing 

benzene and toluene to survive for several months . Under these circumstances, 

benzene, toluene, and similar gases could be transported over long distances. 

The global sources of benzene a nd toluene are extremely difficult t o 

estima t e accurately, since they are many and varied. A global mass balance 

may be constructed as § = Eli, where § is the annual emissions (Tg yr -1), E 

is the global burden (Tg), and i is the average global lifetime (yr) . Since 

the concentrations vary with latitude and longitude, especially for toluene, 

the estimate of E based on present meas urements is subj ect to sizable uncertainties. Similarly, the eva luation of an average lifetime leads to uncertain 

results . Within these co nstraints, the most likely values for the global 

emissions of benzene and toluene based on the present data were estimated. 

First the globally averaged ground-level mixing ratio Co was evaluated. The 

atmosphere was divided according to latitude. at intervals of 0.1 for sin .; 

thu s , 20 equal-vol ume boxes were obtained . The estimate of ground-level co ncentration was then obtained from the avai1able measurements in or near these 

boxes . BRW da La were used for 0.8 < sin • $ I. 0; Cape tlea res, I,HI, and N\\'R 

data for 0.5 < sin • ~ 0.8; MLO data for 0 < sin. $ 0.5; SMO data for -0.4 < 

sin • ~ 0; Tasmania and South Africa data for -0.7 < sin. $ 0.4; and SPO data 

for -I ~ si n • ~ -0 . 7. This weighted the sites latitudillally and provided a n 

estimat e of 

Tl/2 

Co = f Co(.) cos IP dIjJ . 

-Tl/2 

The values of Co for benze ne and toluene are 90 pptv and 62 pptv respectively. 

NexL, a decrease of mi xing ratio with hei ght had to be accounted for (see Rasmussen et al., 1983). The height profile was estimated by a one - dimensional 

model as C(2) = Co exp(-z!.JK ... T), .'here 2 is height and K ... is the up"'ard diffusion parameLer (Khalil and"Rasmussen, 1983). K ... is Laken to be approximaLely 10 5 cm2 s-l. The global burden is esLimat~d to be 

I

ZT 

C(2) dz (4) 

o 

I,'here C is in Tg, NT is the number of molecules of air in the troposphere, No 

is Avogadro's number, M is the molecular weight (g mol-I), zT is Lhe average 

height of the tropopause, and C(z) is in ppLv (see Khalil, 1979). Because of 

the short lifetimes, (4) becomes 

110 
Thus, from (5) the global burdens f of benzene and toluene are estimated to be 

0.3 Tg and 0.1 Tg respectively, assuming _average OU levels of 0.7 x 10~ molecules cm- 3 to determine the lifetimes. S then turns out to be 8 Tg yr I for 

benzene and 14 Tg yr- I for toluene. As stated earlier, these estimates are 

subject to uncertainties; still, they constitute a beginning for evaluating 

annua l global emissions of these hydrocarbons. 

Since benze ne and toluene have different lifetimes and often come from 

the same sources, measurements of their concentration ratio can be used, along 

\\'ith other atmospher i c data, to trace the origins and locations of the sources 

of poilu Lion on regional scales. The use of benzene and toluene as tracers of 

air pollution is currently being investigated. 

5.2 Aerosol Light Absorption at MLO 

A. D . Clarke and R. J. Charlson 

Environmental Engineering and Science Program 

University of Washington, Seattle, IvA 98195 

A filter sampling program aimed at characterizing the optical and 

chemical features of the size-fractionated aerosol at MLO was initiated with 

measurements during 28 Hay-28 June 1981 (Clarke and Charlson, 1982) and continued during 25 April-29 Hay 1982. These studies involved separate day and 

night sampling of the aerosol along with measurements of the size distributions using a modified Royco 220 OPC. From June 1982 through June 1983, 3-h 

samples of the downslope (Mendonca, 1969) aerosol were taken nightly to eliminate local upslope contamination and to obtain aerosol samples representative 

of mid tropospheric air subject to long-distance transport. Samples representative of both the ann ual and daily variability associated with the springtime 

aerosol Lransport from Asia (Uematsu et al., 1983) were collected along with 

Lhose representative of summer "unperturbed" conditions. 

The intent of these measurements was to exanline the variability in both 

fine- and total-aerosol light-absorption properties, single-scatter albedo, 

and total/excess sulfate fractionation for the background midtropospheric 

aerosol. The measuremenL of the absorption coefficient b (m- I) is valuable 

ap 

as a direct measurement of r~diative effects and, in conjunction with the 

scattering coefficient b (m I), it allows specification of the single-scatter sp 

albedo w = b I(b + b ) for assessment of climatic effects. These meassp ap sp 

urements were compared and interpreted in conjunction with Asian -dust concentrations (Parrington et aI., 1983b), light-scattering data, and meteorological 

data availab l e at HLO over the same time period. 

During sample collection, a 3- cm-diameter tube conveyed the aerosol from 

the top of the HLO sampling tower (10 m) to tapered, diffusing filter holders. 

Two Pallflex QAS 2500 quartz fiber filters were changed daily to obtain concurrent samples at 60 Q min-I. Upstream of one filter a modified Bendix Model 

18 Cyclone provided a 50% size cut at a particle diameter of about 0.7 ~m, 

corresponding to t he intermode minimum between fine and coarse ope mass peaks 

observed at HLO (Clarke and Charlson, 1982), so that total- and fine-aerosol 

characteristics could be intercompared. The light-absorption coefficient was 

later measured at the laboratory using the nondestructive integrating sandwich 

technique (Clarke, 1982). 

111 
Some results for the limited springtime samplin g in 1981-1982 are presented in fig . 70 . Apart from the indicated day and night samples, the figure 

also reveals the ~ffect of excluding sample periods when CN concentrations 

were above 300 cm 3. This is a common criterion for background midtropospheric air and generally serves to eliminate periods of intruding boundary layer 

air at MLO. The range of the l ower background values of b was (1 - 7) x 

ap 

10- 8 m- 1 for May-June 1981 and (3-17) x 10- 8 m- 1 for April-May 1982 in spite 

of apparent elevated Asian-dust transport for the 1981 period. The higher b 

values for 1982 are also reflected in relatively low background values of w ap 

(fig. 70) that averaged about 0.97 (1981) and 0.93 (1982). Most of the absorption (70% ± 10%) was co nfined to the fine - particle mode passed by the 

Cyclone. Crustal material in this mode appears to account for only a sma ll 

fraction of this absorption, a nd EC is s ugge sted as the primary light ab -

sorber. 

Because of limited resources, sample collections have continued only on a 

nightly basis, and only a limited preliminary analysis of those data is available. At present, initial measurements indicate that the overall annual variability of b parallels that of b and that both coe ffi cients increase together durinlPthe spring incursionlPof Asian-dust aerosol (Parrington et al . , 

1983b) and drop considerably by mid summer. Nightly high variability indicates 

that such aerosol incursions have considerable spatial and temporal variability. Light-absorbing particles appear concentra t ed in the fine-particle mode 

throughout the year although some variability in the proportions seems evident. Indications are that fine-mode crustal material cannot account for most 

of the measured light absorption, and the long-distance transport of continentally derived soot is implicated. I,hen sprinytime b values are divi.ded by 

the specific absorption of EC (about 10 m2 g- ) , th ea~es ulting estimate s of 

MLO background EC concentrations are in the range of 1-20 ng m- 3 a nd are in 

close agreement with recent minimum values measured for the Atlantic marine 

boundary layer (Andrea, 1983). 

More than 800 filter samples have been accumulated to date . The optical 

and chemical data that could be obtained would be of particular value for 

comparison with the light -sca ttering and elemen tal-analysis data that are also 

available for this period. A selection of samp les from various times of the 

year having simultaneo us changes i n the data should be examined to evaluate 

the significance of con tinental sources and long-distance transport for the 

ma intenance of a background tropospheric aerosol. An annual record of the 

magnitude and variability of the single-scatLer albedo for the remote midtroposphere would be a valuable parameter for current climate modeling and also 

for predicting future trends. It is relevant to note that such measurements 

are both necessary and central to the primary [uncLion of the GMCC program. 

In sofar as soot is implicated as a primary light absorber at MLO, b co uld be ap 

an effective tracer for aerosol reaching MLO [rom continental combustion 

sources. The variability in b co ul d also be valuable in the interpretation 

of other background atmospherigPstudies at tILO . 

11 2 
,-. 

<. , 

'e ,r 

,u 

x 

"-cr: 

ao 

o 

o 

w 

ao 

.J ,:r 

cr: 

W 

0-

0-

cr: 

"-' 1/1 

w 

G 

:;: 

-'J, 

28 May - 28 Jun 1981 

30 

20 • o 

10 • 

• 

~ 2~ 38 10 5~ 

50 

30 

20 

• 

10 • 

• 

• 

,95 • .. , 

.9 • 

.85 

,8 

.75L-~~--~~~--~~~~~-: 

6 10 2e 3t:1 -it) 51) 

TIME SERIE5· 19(:1 

co 

, 

., 

X 

Q. 

a: 

III 

, 

l: 

v 

(X) 

, 

., 

" 

x 

"-a: 

III 

o 

o 

w 

Col 

.J 

cr: 

cr: 

W 

0-

0-

a: 

<.' 

til 

w 

.J 

LO 

:;: 

-If' 

56 

10 

36 

26 • 

16 

50 

20 

10 

,95 

,9 

.8S 

,8 

25 Apr- 25 llay 1982 

. ' 

• • 0 

.

,

• 

. l( 'vh ": ~ .• fl •• 

15 36 

• • 

t • .. ... 

• 

• 

• • 

•• • 

o 

• 

• 

• 

• ·0 

\.. 

' . 

• 

• 

• 

TIME SERIES 1382 

• 

• 

• 

75 

Figu r e 70 .--Time se ri es by sample number for indicated sampling periods 

a t MLO for da ytime up sl ope (X) and nighttime downs lopes (0 ) condi tions . 

From top to bo ttom: abso rpti on coe ffi cient (BAP) for all sampl es ; BAP 

for ba ckground cond itions (CN concentration < 300 cm - 3 ) ; and si ngl e : 

sca tter al bedo f or background conditi ons (CN concentrati on < 300 cm 3). 

11 3 
5.3 Solar Radiation Assessment f or BRW 

G. \vendle r 

Geophysical Institute, University of Alaska 

Fairbanks, AK 99701 

The four c l i mat ic regions in Alaska are the maritime region in the south, 

the intermediate zone, the interior continental region , and the Arctic region 

north of the Brooks Range. Solar radiation stations were established at 

Kodiak, Anchorage, Fairbanks, and BRW, respectively, to represent the four 

regions. These stations will give a basis for the amount of solar radiation 

available at different times of the year and on different exposed surfaces in 

these four regions. 

The foll owing measurements were added to those already being t a ken at BRW 

by G~lCC and the Smithsonian Institution: (I) global solar radiati on, (2) reflected solar radiation, (3) all-wave in coming radiation, (4) all-wave outgoing radiation, (5) sky radiation, (6) global radiation on a south slope i nclined to la titude, and (7) global radiation on a south wall . The data are 

recorded on a Datel data logger. 

The data are helpful in the design of systems such as PV arrays currently 

being used for such applications as thawing road cu lverts and operation of 

remote railroad-crossing lights. Design of buildings t o maximize the passive 

use of solar energy is a nother application. 

Besides these practical applications, some theoretical problems are of 

interest. Examples are s nowmelt and the multipl e reflection between s now 

cover and the stratus clouds, or the radiation phenomenon found in BRW in 

spring. This radiation phenomenon, which i s being studied systematically, 

showed that even in late Ma y at noon the net radiation (shortwave and thermal 

IR) is less positive under clear sky than under cloudy conditions and results 

in colde r temperatures for a clear day . This is, of course, common knmdedge 

for the Alaskan willt er ; however, that this is also experienced in ~Iay at noon 

is at first s urprising. Cloudiness does not decrease the global radiation 

substantially, because multiple reflection between the lower extent of the 

clouds and the highly refl ec ting snow s urfa ce increases the sky rad ia tion. On 

the other hand, the cloud cover is rather opaque in the thermal IR region, a nd 

protects the sur fac e from larger IR losses. 

5.4 Climatology of Aerosol Co nce ntration at spa 

February 1974-December 1982 

J. A. Samson and A. W. Hogan 

Atmospheric Sciences Research Center 

State University of New York, Albany, NY 12222 

ASRC and GMCC began a joint aerosol r esearch program at spa in 1974. 

Total CN concentration is measured with a photoele c tri c CNC twice daily at 

0000 Z, once coincident with radiosonde launch and once at another time, at 

least 8 hour s apart . These observations have continued without interruption 

to the present. The measurements have been made by several GMCC and ASRC 

observers over tIle years. The observations are recorded in duplicate in nolebooks archived both at ASRC and at G~ICC, Boulder. Each observation consists 

114 
of date, time, relevant comments, and 20 individual parameters including the 

C~ concentra ti on . The Antarctic aerosol is unique in tile study of climatological trends, because it represents a background aerosol appearing at the end -

POiIlt of nature's meteorological removal processes, unadulterated by contamination from vegetation, ~ind blo~n spray, or fossil-fuel combustion. 

The study of the Antarctic aerosol has been limited by instrument problenls encountered ~ith measuring lo~ values of concentration and with the practical operation of instruments in such a harsh envrionment. Voskresenskii 

(1968) was the first to measure the total concentration of CN in Antarctica, 

along the coast near the Mirnii region in 1965. The CN measurements used in 

this paper were made with a Pollak photoelectric CNC with convergent light 

beam (Pollak and Metnieks, 1960) , which is sufficiently sensitive to measure 

the low concentrations found in Antarctica with high accuracy (Hogan et al., 

1981). The Pollak counter is attached to the Komhyr (1983) stainless steel 

sampling stack. The size and charge of ambient aerosol are determined using 

the Sinclair (1972), Rich (1966), and Spurney et al. (1969) techniques. A 

diffusion battery, filter, or denuder is inserted in the sample line, and the 

loss of particles of selected physical property is determined by repeti ti ve 

measurement . 

The photoelectric CNC operates on the principle that the percent of light 

transmitted through the chamber after a fog has been formed on the nuclei is a 

function of the aerosol concentration. The 2.S-em-diameter chamber is about 

58 em long and is lined with porous ceralnic that is kept moist. Air is allowed to flow through this chamber and is then contained by closing the upper 

and lower flush valves . An overpressure of approximately 105 torr is produced 

by compressing the air in the chamber. Quickly releasing the pressure causes 

an adiabatic expansion to produce water fog. The amount of fog formed is 

measured by the extinction o f a light beam passing through the column using a 

light source and photocell . 

Three separate readings are made at each observation . These readings are 

taken ove r a period of about 5 minutes, because 1- 2 minutes are required per 

reading, to flush the chamber and to achieve saturation prior to expansion. 

Ea ch reading is then converted to the number of particles per cubic centi -

meter, using the calibration of Pollak and Metnieks ( 1960). Three readings 

per observation, averaged to obtain a mean aerosol concentration [or the ob -

servati on, increases the reliability of t he value obtained and determines the 

variabi l ity of the aerosol concentration. 

Figure 71 and table 35 show the monthly mean aerosol cOllcentration f or 

1974 -1 982; table 35 also gives the number of observations per month. A repeatable seasonal variation is eviden t, with the aerosol concentration highest 

during the austral summer and lov.'est during the austral \,'intcr. No apparenl 

increase or decrease in mean aerosol concentration is detectahle over the tinlC 

span of the observations . The lowest monthly mean concentrations OCCllr in 

June, July , or August o f each year, whereas t he highest monthly mean co ncentrations appear to be bimodal and are divided among the summer month s . November 

consistently has a high monthly mean, wi th the average concentration in December alv,lays lo\o,'er. With equal frequency, January, February, and arch also 

experience a large monthly average . The wide range in concentrations that 

occur in November were noted by D. Nelson, station chie f, during the initial 

year of observations in 1974. 

115 
• t ! , 

t 

I: L, " • ., I .,' I .... ! .,' i .' 

Figure 71.--SPO monthly mean aero -

sol concentrati on for 1974 - 1982. 

Tab le 35 .--SPO mo nthly me a n aerosol concentration* 

1974 1975 19 76 1977 19 78 1979 1980 1981 1982 

Jan --t 103 138 119 254 109 19 3 208 146 

--t (25) (43) (48) (62) (33) (97) (60) ( 105) 

Feb 85 109 226 159 188 289 426 139 21-+ 

(6) (56) (42) (48) (56 ) (55 ) (56 ) (53) (b3) 

fla r 349 1 19 140 120 121 303 104 105 87 

(22) (91) (72) (62) (84) (6 3) (62) (59) (62) 

Apr 109 47 57 44 30 63 51 39 50 

(22) (85) (56) (54) (l02) (6 1 ) (60) (58 ) (58 ) 

flay 29 24 49 31 20 17 29 25 1~ 

(4) (61) (60) (62) (93 ) (61) (61 ) (61 ) (03) 

J un 29 13 871 22 7 15 17 I I 13 

(13 ) (57) (58) (59 ) (90) (60) (60) (58 ) (59) 

J ul 23 12 126t 15 !O 15 12 19 13 

(49) (59 ) (6 1 ) (62) (93 ) (62) (b l ) (b I ) (60) 

Aug 19 16 15 16 9 22 25 18 22 

(19) (63) (62) (62) (91) (62) (b2) (bO) (b2) 

Se p 48 36 37 43 27 32 47 29 32 

(94 ) (57) (83) (60) (90) (60) (60) (57) (60) 

Oc t 117 99 124 178 79 101 119 78 85 

(56 ) (40) (61 ) (62) (93 ) (62) (b3) (b2 ) (b2) 

Nov 159 254 364 169 172 225 188 Ib 7 11 9 

(23) (25) (55) (56 ) (80) (83) (58 ) (71 ) (59) 

Dec 89 131 12 I 16 1 154 146 129 I-u ' - 14 

( I ) (41) (32) (57) (53 ) ( 101 ) (lJ) (b8) (59) 

Annua 1 82t 68 li n 88 76 11 6 11 4 84 77 

mea n (309 ) (660) (685) (692) (987) (763) (773 ) (728) (77 2) 

(we i ghted) 

Annual 96t 80 124t 90 89 I I 1 11 2 82 -f _ , mea n ( I I ) ( 12) ( 12) ( 12) ( 12) ( 12) ( 12) ( 12) ( 12) 

(l"we ighted) ----- -- - ---- - -- -- -----

-:'Va lues in parentheses ind i ca te t he llulIlilp r o f obs e rv.l l iOlls pe r mOlllh. 

Hli ss in g or quest i onable data. 

1 16 
The standard deviations associated with these means are least in the 

winter months and greatest in the summer. These standard deviations vary from 

3 to 19 cm- 3 for the winter and from 40 to 95 cm- 3 for the summer averages. 

The concent rati ons are more variable in spring and summer months. The wide 

range of obse rved concentration in November is due to frequent exchange in 

lower layers, accompanying the breakup of the polar vortex. Concentrations 

va ry little throughout the winter because minimwn low-layer exchange occurs. 

Measurements rarely exceed 50 cm- 3 in winter and occasionally approach the 

threshold sensitivity of the instrument. A minimum deflection of the meter is 

equivalent to about 3 em- 3 , The lowest monthly mea n concentrations vary from 

7 to 19 cm- 3 during these 9 years of data. 

The data collected by this joint program have been stratified by season 

and wind direction to provide a preliminary climatology of aerosol concentration . Recent analysis of the 9-yr data set s hows that rising barometric pressure most frequently occurs concurrent with northwest (grid) winds at the 

surface, and brings not only cloudiness and precipitation but increa sed surface aerosol concentration as well. The rising barometric pressure is evi -

dence of actual transport of air from the coastal regions to the Polar plateau, which brings lower latitude influence along an upslope path. 

The most recent GMCC-ASRC cooperative field program was conducted during 

January 1983. A cascade impactor was operated simultaneously with the GMCC 

aerosol, ozone, and meteorological instrumentation in the CAY . A slm\l-rising 

radiosonde was launched each day, in addition to regular radiosonde flights, 

to de termin e stability and mixing parameters near the surface. These observations s howe d manyfold increases in aerosol concentration and a slight decrease 

in ozone concentration to accompany near-surface mixing that results from 

destruction of the radiation inversion by cloudiness. These mixing events are 

brief, with few surviving long enough to be detected on successive radiosonde 

launches. This indicates that aerosol events detected at SPO result from 

brief downward mixing of mor e highly aerosol-laden air. The surface concentrations may be enhanced for several hours after the mixing occurs. The simultaneous decrease in ozone, observed with an increase in aerosol concentration during these events, is evidence that this exchange is confined to the 

lower layers of the tropospher e . 

5.5 Size Characteristics of Asian Dust Sampled at MLO 

T. A. Cahill and D. A. Braaten 

Air Quality Group, Crocker Nuclear Laboratory 

University of California, Davis, CA 95616 

5.5.1 Introduction 

Long-range transport of soil dust from arid regions of central and eastern Asia, which include the Gobi, Takla Malan, and Ordas deserts, can significantly increase the particulate load of the portion of the troposphere above 

the marine layer at MLO during February-June . This results from both synoptic 

flow patterns that provide the necessary transport flow regime, and increased 

duststorm activity throughout central Asia resulting from low rainfall amounts, 

117 
increased occurrence of strong s urfa ce winds associated with co ld fronts, and 

soil cultiva tion. This l ong-r ange transport of dust ha s bee n ve rified in 

terms of both meteorological trajectory a nalysi s a nd particle sampling . Mill er (1981a) establi s hed a 5-yr climatol ogy of tra jectories to MLO and showed a 

predominance of trajectories from the region of duststorms (northwest of MLO) 

du ri ng periods of greatest activity . Relations hips between trajectories and 

sampled particles at MLO have been investigated by Parrington et al. ( 1983b) 

a nd Darzi and Winchester (1982a), and relationships between trajectories and 

light-scattering properties have been stud ied by Sha w ( 1980) . To date, sampling a nd a nalysis of transport ed Asian dust have been limited to a t otal 

sample with no size differentiation. This discussion focuses on the properties of transported Asian dust segregated by size . 

5 . 5 . 2 Procedures 

Parti c l es were sampled a t MLO between J an uary 1980 a nd February 1982 t o 

obta in information on the size distribution and chemistry of background mid -

tropospheric part icles . Sampling was cond uc t ed using a modified multiday 

sampl e r (Flocchini et al ., 1976) consisting of an inlet stack to exclude particles having diameters greater than 15 ~m, two grease-coated Mylar i mpaction 

stages with cutpoints of 3 . 0 and 0.5 ~m respectively, and a -~m Ghia Teflon 

final filter for the remaining particles having diameters less than 0.5 ~m. 

Sampl in g was performed 7 hours per day, between 2200 and 0500 LST , for a dura -

tion of 8 days . Limiting sampl i ng t o only t hese hours, whi c h corres pond to 

downsl ope winds, s hould normal l y res ult in the sampl e d parti c les being of midtropospheric origi n and not locally generated . Sin ce the sampler was triggered by time rather than wind directio n , the possibility does exist that particles of local origin were sampled during upslope flows. The 8-da y sampling 

period was c hosen to ass ure suffici ent particle loadings for elemental analy -

sis . 

5 .5. 3 Results a nd Dis cussio n 

The period between 5 May a nd 25 August 1981 was analyzed a nd appears to 

include a dust transport episode at MLO followed by a period without signifi -

ca nt concentrations of soil-related particles. The period between 12 May and 

8 J un e was strongly influenced by Asian dust, 16 June-25 August was c l ean , a nd 

5 -11 May and 9-15 June were transition periods. 

The characteristi cs of the dust tra ns port episode were hi gh conce ntra -

tions of soil-re lated elements on the final filter stage (stage 3) and the 

second drum stage (st age 2). Also, low co ncen trations of Cion the first drum 

stage (stage I) were used to indicate whet her the sampled aeroso l was primarily of mi dtropospheric or local marine -layer origi n. Both the relative con -

centra tions a nd size distribution of the soil- r e lated elements meas ur ed during 

the Asian-dust e pisode and the postdust peri od were significantly different 

on stages 2 and 3 for all soil-related elements. 

Figure 72 s hows the mea n re lati ve co ncentra tion and uncertainty for Si 

a nd S during the Asia n-du st episode and the period following, which had little 

or rIo Asia n- dust influence. During the dust episode the relative conce ntra -

tion of Si was increased significantly for stages 2 and 3 , and the size distribution was s hifted toward a greater mass in the smaller particle size 

ranges . Cautio n is advised, howeve r, in interpreting fig. 72 in terms of s i ze 

11 8 
t 

1--01 

i 

:~' I . : 

, 

, 

, 

, 

, 

: 

Figure 72. --Comparison of size -

segregated Si and S during and 

after an Asian -dust episode . 

. I: 

r f'" .. r* I 

~ ~ I 

, . , . , 

Figure 73.--Size-segregated ratio of 

Si to Fe during and after an Asiandust episode. 

distribution since some bounce-off between stages 2 and 3 did occur , as iden -

tified by scanning electron microscopy, because of the heavy particle loadings 

in duststorm periods. No stat.istically significant difference bet,,'een the 

dust episode and the postdust period was found for concentrations of coarse 

soil particles (stage 1), nonsoil-related elements such as S, or the S size 

distribution . This is contrary to the findings of Darzi and Winchester 

(1982a) who found a direct relationship between increased conce ntrati on o[ 

soil-dtlst elements and increased S concentrations . 

Various mean elemental ratios during the Asian - dust episode and the postdust period were calculated. Figure 73 shows the mean ralios and standard 

deviations of Si and Fe for both periods . During the Asian-dust episode, 

stage - 2 ratios were very co nstant and were within the range of Si /Fe ratios of 

3- 4 for North China dust particles in the size range of 2-4 ~m (Wang et aJ., 

1982 ) . During the postdust period the stage-2 SilFe raLio increased La a 

mean value o[ 5 .0, whi c h is the mean crustal SilFe ratio . 

5 . 5.4 Conclusion 

The measurement of size - segregated midtropospheric aerosols and subsequent e l emen tal ana lysis by PIXE has permitted identification and chara cteri -

zation of soil dust transported [rom central and eastern Asia to MLO. The 

majority of Lhe transported dust is in the size range of 0.5 - 3.0 ~m aerodynamic diameter and is composed primarily of Si, AI, K, Ca , Ti, and Fe. Asiandust episodes were identified by increased concentrations of soil- related 

elements on stages 2 and 3 , and low concentrations of Cl (scasalt parLicles) 

on stage 1. Results indica Led a shift toward higher concentrations of soijr elated elements in the smal ler size ranges and a nearly consta nt stage-2 

SilFe ratio corresponding to that observed in North China [or soil-du st particles of the same size range. 

Ack nowledgment 

The assistance of K. Coulson and his sLaff at MLO in operating the sampler is greatly appreciated. 

11 9 
5 . 6 C02 and Other Air Chemistry Studies a t Palmer Station 

E. Robinson and W. L. Bames berger 

Laboratory for Atmospheric Research, Col l ege of Engi neering 

Ivas hington State Universi t y , Pullman, WA 99164 

The first year of operation of the air chemistry facility at Palmer Sta -

tion, Anvers Island, Antarc t ica, was completed in February 1983 , and some 

preliminary sampling results for CO 2 and other trace atmospheric constituents 

ca n be r eport ed. A description of the st ation ca n be found in Robinson and 

Bamesberger ( 1982) . 

The air chemistry facility is used as a base for gatheri ng CO 2 flask samples f or analysis in the GtlCC laboratories. In addi t ion, gas - chromatographic 

instrumentation is operated to measure CO 2 and other tra ce co nstituents con -

tinuously. A Carle Hode l 211 automati c GC is used for CO 2 monitori ng. The 

instrument is calibrated against standard CO 2 -in- air mixtures that in turn 

ha ve been given a preliminary standardi zation che ck by the GHCC C02 laborat ory. Figure 74 shows weekly ave ra ge CO 2 co nce ntrations based on hourly sampl es f rom 6 February t o 15 J uly 1982 and 15 December 1982 to 4 Ju ne 1983. The 

approximately 25 - wk brea k i n the co ntinuous record was caused by a failure in 

the hydrogen generator for the automatic GC. During this period canister samples were collected at a frequency of abo ut 2 mo- I and subsequently analyzed 

at WSU . The CO 2 concentrations from the individual canisters are shown in 

f i g. 74 and noted as "canisters.1I 

The concentration trend in these data is c learly inc reasing by about 

1.5 ppm yr- I . The regression line for the - 16-mo period shown in fig. 74 is 

CO 2 (ppm) = 336 . 084 + 0 .029X, where X is weeks since the week of 6 February 

1982 . In addition t o the general upward trend, some s horter- period cycles 

a l so appear in the co nt inuous data. In late Harch and early April 1982 there 

was a marked decrease in CO 2 conce nt rations, while late in the period cove red 

there was a period of s harply in c reasing concent ra ti ons conta ining a clear 

cycle with about 1-1.5 month s be t wee n ma ximum and min i mum. Both the 1982 and 

1983 shorter-term cyc le s occu rred in about the same season, Ilanle l y in late 

Harch and April . It should be emph asized t ha t the calibra t ions used as a 

basi s for t hese data are preliminary and will be rechecked against GMCC standards before fina l data are publis hed . 

342 

.\4 0 

• •• • E 338 

c- .". .. o. 336 • 

, 

<flO • ., , - N 334 

0 l CANIS1ERS 

u 

332 

330 L, 

N 

<D , ;;; Q CT> '" '" N , 

" '" '" 

•• 

.-

r 

,.., 

'" , 

'" 

• II 

-

, , <D 

N " 1 

,.., '" 

Figure 74 .--Weekly Ilvcrage CO 2 CO I1-

ce nLralio llS a t PaLrl1er Stali o !l, ilased 

o n a utomat i c GC RllaLyses excepL 

,,'here ind i v idual ca njsler s:l mpJes 

eire indi ca l ed. 

120 
Table 36 . --Anvers Island, Palmer Station, trace atmospheric 

constituent da ta, 1982 preliminary r esults 

Co nstituent 

Mean concentration 

Decemb er 1982 1982 annual trend 

CFC- ll 

CFC-12 

CH 3CC13 

CC1 4 

N20 

CO 2 

CH 4 

CO 

190 . 0 ppt 

304 . 6 ppt 

117.5 ppt 

148. 1 ppt 

300.9 ppb 

337 . 4 ppm 

1 . 50 ppm 

0 . 059 ppm 

+8.5 ppt yr- 1 (4.7%) 

+11. 2 ppt yr- 1 (3.7%) 

+6.7 ppt yr- [ (6 .0%) 

+3.1 ppt yr- 1 (2.1%) 

+4.37 ppb yr- 1 (1 .5%) 

+1.51 ppm yr- 1 (0 .45%) 

Not availa bl e 

Not available 

As mentioned above, other trace gas co nstituents in addition to CO2 are 

measured continuously a t Palmer . Table 36 lists these comp ound s , the approxima te average concentrations mea s ured in Decemb er 1982 , and the time trend s observed du ring the 1982 sampling period . It i s impo rtant to note that all of 

the constituent s with anthropogenic so urces, such as t he ha l ocarbons, show 

upward annual trends. The trend for N20 is a l so upward by about 1. 5% yr- 1 . 

Even though t his is primarily a biologically generated compound there is probably some perturbation of th is consti t uen t by ag ri cultural operations and 

large f uel combusti on sources . However , an upward trend of this mag nitud e i s 

not typical of t he dat~ from other locations, and it wi ll be given ca reful 

study. The trend s of the halocarbon concentrations , 3%-5% annually, are about 

half the annual trends observed i n Antarctic halocarbon sampl es taken in the 

years 1975-1978 a t McMurdo and SPO. Additional mea s urements showed the ap -

proximate ann ual range f~r 03 concent ra tion to be 10-30 ppb and for CN concentration t o be 20 -1 000 cm 3 

5 .7 Raman Study of Graph itic Carbon Co ncentra tion s in the Wes t ern Arctic 

H. Rosen and T. Novakov 

Lawre nce Berkeley Labo r ato r y 

University of California , Berkeley , CA 94720 

Recent studi es at g r ound level in the Ala s kan Arc ti c (Ra hn and McCaffr ey , 

1980; Shaw, 1981; Ros e n et al ., 1981) show the presence of substantial concen -

t rati ons of carbon- and sulfur-containing particles that seem to be charac te ristic of the Arctic region as a whole (Barrie et aI., 1981; Ottar, 198 1; 

Heintzenberg , 1980). These particles are eff ective scatterers and absorbers 

of visible radiation (Rosen et a l., 198 1; Bodhaine et al., 1981 ) and appear t o 

be responsible for the phenomenon of Arctic haze first reported by Mitchell 

( 19 57) . On the basis of trace - e lement analysis, it has been suggested that 

t hese particles ori gina t e from anthropogenic sources a t mi dlatitudes (Rahn and 

McCaffrey, 1980 ; Barrie et al ., 1981). Direct substa nti ation of combusti on -

gene rated particles in the Arctic atmosphere has been provi ded by th e identificatio n of l arge concentrations of graphitic carbon part icles at BRW (Rosen 

et al., 198 1) . These graphiti c particles, which ca n only be produ ced fr om 

high-temperature combu stion processes, have been identified on a mol e cul a r 

level using Raman spectroscopy . If one exc lud es natura l burning processes 

121 
that are not expected to be a significant source during winter and spring when 

the Arctic haze is at a maximum, then one can attribute these graphitic particles directly to anthropogenic activities . These particles, which have large 

absorption cross sections (~10 m2 g-l) in the solar spectral region, can lead 

to significant heating effects (Shaw and Stamnes, 1980; Porch and MacCracken, 

1982; Cess, 1983). The magnitude of these effects largely depends on the vertical and horizontal distributions of the graphitic particles as well as their 

concentrations as a function of time of year. 

This paper reports on an extension of these studies of carbon particles 

1n the Alaskan Arctic to the Canadian and the Norwegian Arctic . These studies, using the Raman scattering technique, identify substantial concentrations 

of graphitic-carbon particles at ground-level sta tions throughout the western 

Arctic. Results s how that the large concentrations of graphi ti c particles 

found at BRW do not constitute a local phenomenon but are characteristic of 

ground-level stations throughout the western Arctic. 

The Raman spectra are obtained directly from aerosol particles collected 

on various filter media without any pretreatment procedures . These spectra 

are s uperimposed on a large fluorescent background, which is due both to the 

filter media and the highly fluorescent material in the sample. Irradiation 

of the sample with an argon laser for 24 hours reduced this background by 

about an order of magnitude. The intensity of the Raman spec tra was typically 

about 1% of the fluorescent background. Aerosol samples were obtained from 

six Arctic sites : BRW in the Alaskan Arctic; Mould Bay, Igloolik, and Alert in 

the Ca nadian Arctic; a nd Bear Island and Spitzbergen in the Norwegian Arc ti c. 

The samples from the Alaskan Arctic were collected on prefired quartz-fiber 

filters (Pallflex 2500 QAO) with a sampler installed at BRW ill cooperation 

with B. Bodhaine of the GMCC program. The samples from the Canadian and 

Norwegian Arctic were co llected on Whatman 41 filters and were provided respectively by L. Barrie of AES and B. Ottar of NIAR. 

Raman scattering and IR absorption spectroscopy are complemen t ary techniques that measure vibrational spectra of gases, liquids, and solids. Often 

vibrational modes that are IR inactive are Raman active and vice versa. Graphitic structures in which trivalent carbon atoms occupy lattice sites in a 

two-dimensional hexagonal honeycomb network have intense Raman modes but very 

weak IR vibrational spectra. These Raman modes, which were first observed by 

Tuin stra and Koenig (1970), e nabl e the identification of grap hiti c structures 

even in the presence of a comp l ex mixture of substances . Solvent extraction, 

heat treatment, op ti cal absorption, and morphology studies (Wolff and 

Klimisc h, 1982) can provide indirect evidence for a grap hiti c component , but 

Raman spectroscopy appears to be the only presently available method for making unambiguous identifications on a molecular level . 

The Raman scattering technique ha s been applied to identify substantial 

concentrations of graphitic particles in combustion effluents , urban air 

(Rosen et al., 19 78 , 1980), a nd the Alaskan Arctic at BRW (Rosen et al., 

1981). The spectra from these samples show the presence of two Raman modes 

located at ~1350 and 1600 cm- 1 that are ca used by phonons propagating within 

graphitic planes (Tuinstra and Koenig, 19 70) . In fig. 75 these measurements 

are ex t ended to samples collec ted from three sites in the Canadian Arctic 

(Alert, Igloolik, and Mould Bay) and two sites in the Norwegian Arctic 

(Spitzbergen and Bear Isl and). All samples were collected at similar times of 

the year, but due to sample availability, some samples are from 1980 and 

122 
,~. '-- . 

.. ..:.--~-. , '-'--.'-'-

... 

'coo 1200 

Berre :. 

Alerl 

--If--''''---t--'-':'_X.-.. '-'" -' .'~ 

..--;- Igloo", , 

. , .•.•... '. ".'"" -'. . .•.. 

Mould Bay 

-- ,'-:~-. '-,--.,:, 

.' .. ) Spitzbergen 

J - " 

.-fJ 

Bear Island 

'---,"":"-.":""'-.-:'. 

1400 1600 1800 2000 

e m-I 

Figure 75 .--Raman spec tra of particles collected in the Alaskan Arc ti c 

(Barrow, 23-28 J a n 1980) compared 

wi th sampl es coll ected in the Ca nadian Arctic (Alert, 20 - 26 Ja n 1981; 

Igloolik, 26 Jan-3 Feb 1981; Mould 

Bay, 26 Jan-2 Feb 198 1) and the 

Norwegia n Arctic (Spi tzbergen, 21-

23 Jan 1980 ; Bear Island 28 - 30 Jan 

1980) . 

others from 1981. It is c l ear from the spec t ra that al l sites s how the pre -

senc e of significa nt concentration s of g r aphiti c parti c le s . There are some 

differences in the relative intensities and line shapes of the two Raman 

modes, but these could be due to systematic errors in fl uorescence subtraction 

for the 1350 cm-[ mod e , which is located on a highly slop ing background. If 

one ass umes fixed opti ca l constants (Raman cross sections, abso rpti oll cross 

sections) , one ca n us e t he i ntegrated intensity of the 1600 cm- 1 Raman mode as 

a meas ure of the re l ative co ncentrations of graphiti c parti c les at the sit es . 

These analyses indicate that the concentrations at all t he sit es are quite 

comparabl e , with the largest and smallest wi th in about a factor of 3 of each 

other . The relative orde rin g of these co ncentrations for Spitzbergen, Bear 

I sl a nd, DRI<, Mould Bay, Alert, and I gloo l ik are 2 .1, 1. 7, 1.0, 0 . 8, 0 .8, and 

0.7. It s hould be emphasized that t his analysis is for a particular time in -

t erval , and the rela tive contributi ons coul d vary considerably from one time 

period t o the next. 

Acknowledgments 

Vie ack nowledge B. Bodhaine of GNCC , L. Ba rrie of AES, and B. Ot ta r of 

NIAR for providing samples from the Alas kan Arctic, the Canadian Arctic, and 

the No rwegia n Arctic, respectively . This work was supported by DOE under con -

tract DE -AC03 - 76SF00098 and by NOAA / ERL under co ntract NA8 1RAG00254 . 

123 
5.8 Ultravi olet Erythema Global Measuring Network 

D. Berger 

Skin and Ca ncer Hospital, Temp le University 

Philadelphi a, PA 19140 

The gl obal network of meters has been recording the half-hourly dose of 

s unburning (erythema) UV solar radiation since 1973 . The number of stations 

has i ncreased fro m 30 in the past years to 40 this year. Three of these meters are located at BRW , IL , and S~ . 

Meter response correlates not only wi th erythema but with DNA damage , 

vitami n D synthesis , no nmelanoma skin cance rs, tobacco-leaf spotting , egg 

morta lity o f some fish species , sewage - wat er purification, and various plant 

stresses. In seven U. S . communi ties the met e r is being used t o educa te the 

publi c abo ut skin cancer risk by publicizing in the local media the daily erythema intensity. A report on the results from 14 of the longe st r unning sta -

tions was published by Berger and Urbach ( 1982) . The absol ute radiant energy 

of the meter was measured by DeLuisi and Ha rris (1983). Data from this network are distributed by NOAA/ARL, 6010 Executive Blvd., Rockville, MD 20852 . 

5 . 9 Aerosol Co ncent rati on Periodicity and Optimum Sampling Strategy at MLO 

M. Darzi and J . W. Winchest er 

Depart ment of Ocea nograp hy, Florida State University 

Tal l a hassee, FL 32306 

5.9.1 In trod uc ti on 

The location and high altitude of MLO, as well as of HVO and other sites 

on the isla nd of Hawaii , are ideally sui led for monitoring ae rosol co nstituents in the mi dLroposphere. Since 1980 several reports have shown thaL dust 

transport from Asia to Hawaii is a regular spri ng occur rence, bringing soil 

minera l parti cles , and possibly s ul fur (S) and other an thropoge ni c pollutants , 

not on l y to the 3 . 4-km LO sit e but t o the lower, 1. 2-km HVO site as well . 

Most i nvestigators have considered that the successful measurement or sampling 

of aerosol that has been t ra nsported from afar s hould guard against inte rference from aerosol particles that may be of local island origin, e . g . , by sim -

ply avoidi ng upslope wind conditions that could carry locally derived aerosol 

from lower e l eva t ions to the s ampling site . However , apparently it is not 

generally understood that such a discrimination may bias the sampling of the 

long-range -t ransported aerosol constituents, resul ting in misleading information, f or example concerning their mean maximum concentrations and important 

s hort-term periodicities (Darzi a nd Wi nchester, 1983) . 

A diurnal sampl ing strategy, based on local meteorological conditions, 

for exampl e , daily upslope -downslope wind s hi fts, or on time of day, has often 

been empl oyed to avoid local aerosol components (e.g., Simpson, 1972; Bigg, 

1977; Dittenhoefer, 1982; Parrington et a!., 1983b) . For ,,'eekly average sampl es, ni ghttime downslope ai rfl ow samp ling periods have bee n composited. How -

ever , suc h a strategy may lead to aliasi ng , an alteration of t he apparent peri odicities , withi n the time-series record of concentration for tile long-range 

components if t hey s hou ld be periodic but not di urnal . No t only may it result 

124 
in an incorrect assessment of the mean maximum concentrations of these components, for example, terrestrial dust and air pollution S of Asian origin, but 

some potentially important linkages between them may be obscured if they 

should exhibit similar short-term periodicities . 

5.9.2 Nondiurnal Periodicity of Spring Aerosol Concentrations at MLO 

Several investigators have now established, on the basis of physical and 

chelnical measurements of aerosol concentrations, that spring dust concentra -

tions at MLO are mainly of Asian origin. During this season, dust storms often occur over Japan. Over Hawaii, haze layers can be observed, aerosol light 

scattering exceeds that of other seasons, and dust composition resembles that 

of continental rather than island basaltic material. Air trajectory calculations suggest that arid lands of China are the most probable source. Darzi 

and Winchester (19820) have determined that this dust exhibits a regularity of 

fluctuation in concentration that is shorter than diurnal, a periodicity that 

cannot be caused by local meteorological effe cts, which on Hawaii are generally strongly diurnal. This pattern is distinct from what has been observed 

(Darzi and Winchester, 1982c) at the lower elevation HVO where concentration 

maxima average 24 hours apart during the same spring period of observation, 

and can be attributed to daily changes in winds. 

A comparison of these two simultaneous sets of measurements is shown in 

fig. 76. In neither case are volcanic emissions important contributors to the 

soil elements determined (Darzi and Winchester, 1982d), but instead surface 

dust from weathered Hawaiian volcanic rock is the dominant component during 

daily maxima at HVO, and surface uusL frolll a continental source, apparently 

Asia, is dominant during MLO concentration maxima, peaks that occur on the 

average about every 21 hours . This periodicity, apparent by inspection of 

fig. 76, is also determined to be statistically significant by time-series 

analysis of the concentration measurements into Fourier componenLs. A similar 

nondiurnal periodicity is found in the NOAA record of hourly light-scattering 

measurements made concurrently by a nephelometer (Darzi and Winchester, 1982b). 

10 00 

~!: ~ 

". ': ~ i\ :/'~': MLO .. ; \ i t:~ i \ ~ 3.4km ' . ... ,.' .:' .• : : " iV\'\.: ' 

,o ; , , '\ , " i \ ~\i! ': + ! \I~ : \ . :, ,~t V ' " 1 . , ' : : ':I 100 :: I,' 

. 

u ' , ' , .,. t : 

c :,; 

If. 

'0 

" 

i 

" " " " 1 2:l 2:~ 2:~ 26 21 28 29 30 I 

OATE 1979 

f~ ." , -: 

: , ~! \ ' : :. .', ,, :,., .;" ~ \~ i~' \ , ~ " ., , . 

\," 

\ .tVO 

12: km 

3 4 !I 6 

"" 

Fig~re 76.--Fe concentrations (ng 

SCM I ) for 3.7-h sampling time steps 

for aerosols collected concurrently 

at ~ILO and HVO. Days having ?,1.3 mm 

of total rainfall at HVO are indicated by the bar at the bottom. 

Dots on the MLO curve are Fe concentrations at 0200 LST. The figure 

illustrates the strongly diurnal 

variation of Fe at HVO, especially 

during nonrainy days, and the regular but less than 24-h variation of 

Fe at MLO during an Asian dust episode (Darzi and Winchester, 1982c) . 

125 
By time-series analysis, light scattering at 850 nm was fo und to be 

strongly coherent with iron (Fe) concentration, but less so with aerosol S 

concentration; however, at 450 run the coherence is stronger with S than with 

Fe, suggesting that S occurs in smaller particle sizes (by oxidation of gaseous sulfur dioxide) than does dispersed soil aerosol containing Fe. Coherence of either element, however , is mu ch weaker with CN concentration, implying that the CN measurement is not as useful an indicator of aerosol mass 

concentrations during spring at MLO as is light scattering. The observed concentration fluctuations of S are more complex than those of Fe, but timeseries analysis shows a 21 -h period to be present, and a 24-h period is not 

found, suggesti ng ca uses of the variations in S to be principally outside the 

influence of local meteorological processes on Hawaii . 

At the 2 1-h period a strong coherency between Fe and S is found, s uggesting that both vary in part because of similar meteorological processes remote 

from Hawaii, e.g. over the Asian mainland, where their prinCipal source locations may not be far from each other, as well as during their transport over 

the Pacific. Possibly both dust, containing Fe and other soil elements, and 

air pollution, containing S and other constituents, are transferred from their 

sources to the midtroposphere and transported above the boundary layer to 

Hawaii. If initially diurnal pulses of aerosol are transferred upward over 

the source areas into horizontally moving air with wind speed convergence, a 

shortening on the order of 1% per day of travel from Asia would be required to 

account for the observed average times between arrival of the pulses at 

Hawaii. Thus, the periodicities in the time-series records of concelltration, 

as well as the concentrati ons themselves, are of value in inferring the 

sources and long-range transport of these aerosol constituents. 

5 .9. 3 Considerations for Aerosol Sampling Strategy 

It should be clear from the above discussion that the sampling strategy 

is of great importance when samplill g the long-range transported componen t s at 

MLO since the strategy chosen wi ll have a bearing on the interpretation of 

results. In particular, a diurnal sampling strategy can lead to a serious 

loss of information when onl y the nighttime samples are examined in the belief 

that they are more representative of the free troposphere and that aerosol 

concentration variations durillg the spring are similar to olher seasons. InlportanL information on the maximum concentration of Asian dust, for example, 

would be lost since our results s how that Asian -du st maxima may be as likely 

to occur during the day in the spring when this comp onent dominates at all 

times. During spri ng, therefore, both day and night sampl es may be of equal 

interest. 

The imposition of a diurnal sampling strategy 0 11 an aerosol whose major 

variations occur with a period of less than 24 hours (or, more generally, 

twice the sampling interval) gives rise to the problem of aliasing, causing a 

distortion of the apparent periodicities of the concentration tinle series . 

For examp le, during the MLO dust event of 23 April - 6 May 1979 shown in 

fig. 76, an examinalion of samples taken only at night causes a false 7-da y 

periodicity, 1/(1/21 - 1/24) = 168 cycle -', from the dominant 21 -h period of 

the actual record. We plotted points on the MLO curve at 0200 LST of each day 

to illustrate how this transformation to a longer periodicity occurs . A curve 

drawn through those points would convey the impression that synoptic events, 

which also act in periods of approximately 7 days, were mainly responsible for 

126 
Lhe variation in the concentration of the Asian dust. Moreover, a diurnal 

sampling rate would not have allowed the strong coherency of S and crustal 

elements at 21 hours to have been observed. It was this co herency that suggested to us that S sampled at MLO during this period had probably originated 

in Asia and had been transported to Hawaii together with the desert dust. A 

real periodicity of about 7 days may be present in springtime aerosol concen -

tration variations at MLO, as suggested by fig. 76. However, aliasing would 

introduce an additional apparent 7-day period if 24-h sampling strategy is 

used wiLh 21-h periodic concentrations. 

As a result of these considerations, detection limits permitting, investigators are strongly urged to use a sampling period as small as possible and 

not more than 8 hours when studying Asian dust during the spring at MLO . If a 

longer period is used, not only does loss of information on the varia Lions of 

the sampled species occur, but also erroneous longer-term variations may be 

induced. Consequently, the sampling time interval should be care fully considered by anyone collecting data on atmospheric species as a time trend. 

5.10 Chemical Analyses of Atmospheric Particulates at MLO and SPO 

J . R. Parrington, G. Tuncel, C. M. Thompson, and W. H. Zoller 

Department of Chemistry, University of Maryland 

College Park, ~m 20742 

5 . 10.1 Introduction 

In February 1979, the first version of a selective sampling system was 

installed at MLO. Two 24-h timers controlled the sampling pumps for upslope 

samples during 0800-1800 LST and for downslope sa mp les during 2100-0500 LST. 

To facilitate the collection of atmospheric particles at MLO, an improved and 

more versatile sector controller was designed and constructed as a joint project between the University of Maryland and NBS (Parrington et al . , 1983a) . 

The decision to sampl e is based on wind direction, wind speed, time of day, 

and CN concentration. To differentiate between upslope and downslope winds, 

the parameter controls were duplicated to provide two independent sampling 

sectors, downslope and upslope. A third case exists when neither sector is 

being sampled. In this case, an additiona l circui t is activated, allowing 

collection of samples that could contain valuable information about aerosols 

at MLO during storms or contamination episodes. The new system began operation at MLO in April 1980, and by the end of August 1980, the system appeared 

to operate reliably . Samples were collected every 10 days on three highvolume filters for subsequent chemical analysis. 

5 . 10.2 Results 

Concentrations observed for particulate samples are given in table 37 for 

four classes: downslope clean season, downslope dust season, upslope clean 

season, and upslope dust season. The clean and dust seasons are identified by 

a ten-fold increase in crustal material that is transported throughout the 

Pacific from Asian deserts between mid-February and July (a 19-wk period) for 

1979-1982. Geometric means are used in table 37 because the distribution of 

Al (and nearly all other elements) is apparently log normal during both the 

clean and dust seasons at MLO. 

127 
Table 37. --Geometric mean concentrations of e lements measured on downslope 

and upslope particle filters during clean (July to mid-February) and dust 

(mid-February to July) seasons at MLO from February 1979-June 1982':' 

Element Downslol2e Ul2 slol2 e 

(units) Clean Dust Clean Dust 

Na (ng) 6.6 (2 . 7) 22 (2.0) 86 (2 . 2) 140 0.9) 

~Ig (ng) 2.6 (2 . 1) 26 (2.5) 14.2 (2.1) 45 (2.0) 

Al (ng) 4.9 (2 . 1) 56 (2 . 5) 16. 0 (2.2) 73 (2.5) 

S (ng) 80 (2.0) 160 (1. 7) 150 0.8) 230 (1.7) 

Cl (ng) 2.4 (4 . 0) 3.4 (3 . 0) 19 (4 . 2) 30 (5 0) 

K (ng) 2.8 (1.8) 27 (2.3) 10 (1 . 9) 41 O· 9) 

Ca (ng) 3.7 (2.5) 64 (3.0) 13 (2 . 2) 83 (2.7) 

Sc (pg) 1.2 (2.2) 12.9 (2.6) 3.9 (2 . 1) 15.3 (2.1) 

Ti (ng) 0.53 (2.6) 4.3 (2.4) 2.4 (2 .5) 7.3 (2.2) 

V (pg) 10.5 (2.5) 104 (2.4) 48 (2.2) 157 (2.2) 

~In (pg) 62 (2.3) 810 (2.5 ) 280 (2.2) 1300 (2.4) 

Fe (ng) 4 . 0 (2.3) 42 (2 . 6) 15.5 (2 . 2) 52 (2.3) 

Co (pg) 3.2 (2.6) 20 (2.4) 9.0 (2.7) 30 (2.2) 

Cu (ng) 0.22 (5. 0) 0.85 (3. 0) 0.33 (4 . 0) 0.6 (3 .0) 

Zn (pg) 90 (4.0) 320 (2.2) 250 (3. 0) 700 (3 .0) 

Ga (pg) 8.4 (4. 0) 20 (2.5) 22 (2 . 7) 42 (2.0) 

As (pg ) 12 . 6 (2.9) 70 (4.0 ) 39 (2 .5) 111 (3 .0) 

Se (pg) 11 . 2 (2 . 0) 21 (1. 7) 22 (1 . 7) 36 0.7) 

Br (ng)t 1. 45 ± 0 . 60 1. 60 ± 0.45 1. 63 ± 0 .50 1. 92 ± 0.90 

Rb (pg) 15 . 5 (0 .1 9) 130 (2.5 ) 21 (2 .5) 150 (2.0) 

Sr (ng) 0 . 24 (1. 0) 0.(;2 (26) 0.28 (1. 8) 0.72 (2.1) 

Ag (pg) l. 36 (3. J) 1.8 (2.7) 2.8 (3 .5) 2.8 (4.0) 

Sb (pg) 1 . 85 (0.26) 7.7 (2.4) 4.6 (2.4) 9.7 0.9) 

I (ng)t 2.1 ± 1.3 1. 45 ± 0.60 2.2 ± 0.80 2 .3 ± 0.60 

Cs (pg) 0.95 (2.6) 9.9 (2.8) I. 05 (3 . 0) 11. 1 (2 .5) 

Ba (ng) 0.51 (4.0) 1. 05 (2 . 1) 0.42 (2 . 7) 1. 14 (3.0) 

La (pg) 3 .0 (2.3) 53 (3 . 3) 11.8 (2 . 2) 66 (2.5) 

Ce (pg) 7.8 (2.3) 71 (2 .5) 31 (2 . 5) 107 (2.6) 

Sm (pg) 0.52 (2.8) 7.0 (2 . 7) 2.0 (2.6) 10. 1 (3.0) 

Eu (pg) O. 19 (2.5) 1. 19 (2 . 4) 0.65 (2.2) 1.54 (2.4) 

Tb (pg) 0.20 (2.5) 0 . 96 (2 . 6) 0.41 (2.1) I. 12 (2.0) 

Yb (pg) 1.10 (2. 1 ) 3.2 (2 . 2) 1.55 (2.0) 4 . 0 (2.0) 

Lu (pg) 0.36 (3. I ) 0.51 (3.0) 0.48 (3.0) 0.85 (2.0) 

Hf (pg) 0.44 (2. 1 ) 3.3 (2 .5) 1. 7 (2 . 5) 5 .4 (2.2) 

Ta (pg) 0.23 (2.3) 0.86 (3 . 0) 0.58 (2 .5) 1. 54 ( 1. 7) 

W (pg) 2 . 7 (3.3) 6.0 (4.0) 12.7 (4.0) 17 (1.7) 

Au (pg) 0.15 (3.0) 0.24 (4.5) 0.28 (3.5) 0.37 (2.5) 

Th (pg) 0.80 (2.6) 11. 4 (3 . 0) 1.8 (2 .8) 12.7 (2.6) 

*Geometric standard deviations for elementa 1 concentrations are s hown in 

pa rentheses. 

tNormal means and standard deviations expressed for Br and I. 

128 
Another method of presenting the data is by comparison of the relative 

elemental abundances in the samp le to those of an average crustal source such 

as Taylor's crustal average (Taylor, 1964) . In this way it is possible to 

note which elemen t s have abundances similar to crustal material and, thus, 

probably originate from crustal sources. The crustal enrichment factor EF 

c 

can be calculated from 

EF c 

= (X/Al)sample 

(X/Al)crust 

where X is the element of interest and Al is the reference element. Al is 

used because it i s easi l y ana l yzed, has known abundances in several crustal 

materials with few other sources, and is conunonly used in this type of calculation. Figure 77 presents downs lope and upslope EF during the clean season. 

An element ha ving an EF of unity occurs in the samecrelative abundance in the 

sa mpl e as in the refere~ce so il. However, deviations are typical because of 

variations in soil composition and elemental fractionation during mobilization 

and transport. Thus, an EF range of abo ut 0.7-5 may be considered to be typical for an element that or~ginates primarily from crustal sources. 

As can be seen i n fig. 77, most elements, Se through Lu, appear to be 

primarily crustal in origin . Variations in the upslope and downslope EF 

va lues may be due to crustal source variations or contributions from add~tio nal sources. For example, marine sea sa lt is known to be about a factor of 18 

higher in up slope samp les than i n downslope samples . This source contai ns 

significa nt concentrations of Na, Mg, K, and Ca, which are reflected by the 

higher upslope EF for these e l ements . Anot he r example is Hawaiian basalt, 

which averages a ~actor of 5.4 hi gher in concen tration in upslope samples. 

This material exhibits slight enrichments of Sc, Ti, V, ~ln, and Fe, and depletions of Cs, Rb, and Th, all of which appear to aff ect the relative EF 's of c 

'0' 

'0' 

MEAN +08 - DOWNSLOPE -0 

B UPSLOPE 

Figure 77. --Downslope and upslope crustal enrichment factors calcula t ed f or 

elements in clean-season atmospheric particulate samples at MLO. 

129 
upslope elements in fig. 77. The anomalously enriched elements apparent in 

this figure are S, Cl, Cu, Zn, As, Se, Br, Ag, Sb, I, W, and Au. Sea salt ca n 

directly account for only a small amount of the S, Br, and I, so there remain 

additional sources for these elements related to natural enrichment from the 

ocean. 

The effectiveness of the separation of up slope and downslope aeroso l s can 

be assessed by comparison of marine components in the samples . The marine 

component can be calculated based upon excess sodium from 

Na

s 

= NaT - 0.0158 C, 

where Na

s 

is marine Na, NaT is the meas ur ed total concentrati on of Na on a 

sample, C is the mass of crustal material in t he sample, and 0.0158 is the 

estimated fraction of Na in average Asian dust (Parrington and Zoller, 1983a). 

The mass of crust al material in a sample is estimated based on the airborne 

concentrations of eight typical crustal elements (AI, Sc, Ti, V, Hn, Fe, Sm, 

and Th) and their concentrations in average Asian dust . Figure 78 is a plot 

of upslope and downslope marine Na determined in this manner. Upsl ope sampling was stopped after March 1982 to reduce the number of samples to be 

analyzed. 

The most striking feature of fig . 78 is the large amount of marine Na in 

upslope winds compared with downslope conditions . If t his difference is expressed as a ratio of the upslope-to-downslope marine Na concentrations , the 

ratio should reflect the efficiency with which the mountain wi nd s have been 

separated by the sampling conditions . The geometric mean of the ratio of 

upslope to downslope data for samples collected under the time - of-day controller (prior to May 1980) is 14 (a = 4.1, where a is the geometric standard 

g g 

deviation). The mean ratio increases to 21 (a = 4 . 1) with add i tion of the 

digital sector controller, indicating that thegnewer system indeed provides a 

better separation of upslope and downslope particles than the time-of-day 

method above does. In general, peaks in upslope marine Na correlate with 

storm activity; however, the influence of storm activity on downslope marine 

Na is mu ch weaker, with only strong storms of long duration (-5 days) appearing to be capable of sufficient tropospheric mixing to add much marine Na to 

the midtroposphere and hence to the downslope samples. 

~ , • 

2~r--'----r----,r---------------------r--.~,,------rrr~-----r----------------~ 

200 

1~ 

100 

1 

so 

u. us 

1911l 1980 

, 

, 

1981 

\. A IV. 

19112 

Figure 78.--Upslope (US) and downslope (DS) marine Na at MLO. 

l30 
Figure 79 is a plot of the upslope and downslope estimated crustal ma sses 

from February 1979 through 1982. The influxes of Asian dust from mid-February 

to July of each year are clearly evident in both the upslope and downslope 

traces of this figure. In general, upslope concen trations are larger than 

downslope concentrations, especially during the clean periods (July to midFebruary). During dust occurrences, downslope and upslope concentrations 

usually peak at similar times, as clearly shown in May 1979, February-June 

1980, and March 1981 . The average of all the upslope-to-downslope concentration ratios for crustal material again appears to be log-normally distributed 

with a geometric mean of 2.4 (0 = 2 . 8) . g 

To determine if the higher mass of crustal material found in upslope 

particles originates from local Hawaiian material, a chemical element balance 

of the samples was made (Gordon, 1980) . Accounted for in this balance were 

the compositions of various groups of airborne particles as a linear combinat ion of the compositions of four sour ce materials: Hawaiian basalt (Gladney 

and Goode , 1981), average crustal material (Taylor, 1964), average Asian-dust 

composition (Parrington and Zoller, 1983a), and a marine component. Results 

of these balances are s umma rized in table 38 . Quantities of Hal,'aiian basalt 

were nearly the same for the clean and dust data sets in both downslope and 

up slope winds; however, the upslope concentrations exhibited about 5 times as 

much local basalt as the downslope concentrations. 

During periods of high dust loading, downslope crustal particles consist 

of 93% Asian dust, and upslope crustal particles are 83% Asian dust-type material. From the results of similar balances on individual filters, the geo -

metric mean mass of local basalt is 15 ng m- S (0 = 3 . 3) in downslope winds - g 

vs. 87 ng m S (0 = 2.7) in upslope winds (Parrington and Zoller , 1983b). 

After removal ofgthe local crustal component, the average upslope-downslope 

crustal ratio drops from the previous value of 2 . 4 to 2.2 (0 = 2.5). This 

g 

ratio should be representative of crustal material transported from large 

continental sources, i.e., Asia or North America, to Hawaii. During the dust 

period, the upslope-downslope ratio of continental material drops to 1. 2 

(0 = 1. 7), s uggesting t hat this materi al is distributed with about an eq ual 

g 

probability in the troposphere at the altitudes from which downslope and upslope winds originate (-4 and 2 km, respectively). Similar observations were 

•. 0r-----~-----------------r--------------_r--------------------------------~ 

' .0 

' .0 

' .0 

1.0 

,. 

; 

j! 1 I, , i ~~ I I '" 

DO 

. UI tl 

, \ I \ 

/"I.i \" 

JFMAYJJASOH 

Hit. 

:l 

': 

D' 

Figure 79 .--Upslope (US) and downslope (OS) total estimated crustal ma sses at 

MLO. 

131 
Table 38.--Downslope and upslope components in ~JLO samples and 

geometric mean concentrations of all individual samples'" 

Component Downslol2e ~lass (ng m 3) 

Cleant Dust§ 

Sulfate""" 240 (2.1) 480 (J.7) 

~Ja rine 16 (3 .0) 22 (3.5) 

Co ntinental Crust 50 (2 . 2) 730 (2.4) 

Hawaiian Basalt 13 (3.1) 25 (3.3) 

*Geometric standard deviations are in parentheses. 

tSamples collected July to mid-February . 

§Sample s collected mid-February through June. 

**Total sulfate concentrations shown. 

Ul2s10[,e Nass (ng 01- 3 ) 

Cleani' Dust§ 

450 (J.8) 640 (J .8 ) 

250 (2.5) 320 (2.2) 

160 (2.2) 870 (2 . 4) 

82 (2 . 6) 115 (2 . 7) 

noted by Prospero et al . (1981) in reference to long-range transport of Sa haran dust across the Atlantic, where they found that Saharan dust became wellmixed throughout the troposphere, above the marine boundary layer, with some 

more stratified layers in existence after transport over several thousand 

kilometers. 

A detailed examination of the chemistry of Asia n dust episodes by Parri ngton and Zoller (1983a) between 1979 and 1982 r evea l s that, with the excep -

tion noted below, the composition is very un iform from year t o year , suggestive of a single major source of this dust. Results of other studies of dust 

episodes in Alaska and Enewetak exhibit elemental compositions nearly identical to the NLO dust composition (Parrington and Zoller, 1983a) . Thus, wide -

spread dust throughout the Pacific basin each spring apparently comes from the 

same Asia n sour ce area (or areas). 

During an 8- wk period, 20 Narch-13 Nay 1980, in the peak 1980 dust episodes, the composition of the dust changed. Several elements were enriched in 

this period, especially Sm, La, and As, and the distribution of severa l rareearth e lements , Ce, Eu, Tb, Yb, and Lu, was different from that of other 

c rustal ma terial observed at NLO. Thus, a different area could have been a 

significant source of dust over this period. Because no information is available on compositions of various desert sa nds or soils of China, this source 

area cannot be identified; however, air mass trajectories indicate the dust 

origina t ed in China (Parrington and Zoller, 1983a). Further research on Asian 

dust episodes may include studies of the compositions and dust ge ne ration i n 

the desert areas of China. 

Parrington and Zoller ( 1983a) examin ed the possibility that dust from the 

source areas normally responsible for spring Asian dust episod es continu ed to 

dominate crusta l materia l of cleaner periods at NLO. Sign ificant differences 

were noted for several heavy elements, Rb, Hf, and Ta, and l arge differences 

for the enrichmen t s of alkali ne-earth elements . These data, together with 

major changes in the rare-earth distribution pattern, i ndi ca t ed a different 

source area for the clean-period crusta l aerosol. 

132 
During Hay 1982, air was sampled with cascade impactors at HLD. The goal 

was to determine the size distribution of the Asian dust and atmospheric particles in the upper troposphere . UnfortunatelYj particle concentrations were 

unusually low during this period, about 1 g m (see fig. 79). Figure 80 is 

a plot of the percent Al per impactor stage vs . particle size. The vertical 

bars represent the standard deviations among five impa ctor se t s collected 

during this period. Al though the deviations are large, all of the impactors 

s how a simil ar size distribution. Host of the mass i s in the small-partic l e 

ra nge , with t he ma ss median di ameter being 2 .6 ~m (for particles of unit density). The mass on the first stage of the impactor ( 16 ~m ) is probably due to 

loca l p rod uction of large particles . 

The samples that we re coll ected at SPD ha ve also been analyzed by neutron 

activation analysis and some of the results are shown i n figs. 8 1- 83 . Because 

many sampl es from Antarctica were co ntami na ted, the quality of the data and 

the sampl es that were collected there are not as good as those from Hawaii . 

When obviously co ntaminated samples are removed from the data set, certain 

trends are easil y observed. A plot of the ave ra ge S concentration over the 

last few years is s hown in fig . 81 . From this plot it is obvious that the 

austral winter S_va lu es are lower than the summer val ues, and are usually 

abo ut 20 - 30 ng m 3 . The s ummer values show mor e variabili t y from year to year 

as wel l as within a year so that long-term trends are difficult to observe . 

Co ncentrati ons of two volatile elements that are highly enric hed in the 

Antarctic, As and Se, are plotted in figs . 82 and 83 . Both elements are high -

l y enri ched in anthropogenic emissions, but the data from SPD s uggest t hat 

they are of natural origin and their concentrations are not increasing. The 

very la rge i nc rease in As during the winters of 1975 and 19 76 was due to the 

inj ec t ion of volcanic debris into the Antarctic stratosphere by a vo l ca nic 

e ruption. Since that time, the concentration has decrea sed and is remai ning 

re l atively constant . For Se, t he volcanic impact is not as noticeable. An 

enhan cement of both e l emen t s appears during the summer months when transport 

from continental areas ca uses an increase of crusta l dust. No trends are 

evident at this time, but the data base is not of sufficient l ength to s how 

long-term trend s. 

50 

20 

10 

5 

%AI 

2 

0.5 

0.2 

Backup 0.5 2 4 B 

Particle diameter, fLm 

16 

133 

Figure 80 .--Percent Al per impactor 

stage vs. particle size at HLD duri ng the Asia n-du st episodes (downslope conditi ons) on 7, 9 , 15 , 22 , 

and 25 Hay 1982 . The mass media n 

diameter is 2.6 ~m. 
'00 " 

" " ,. 

" n 

" '0 

" " " {. !:IO 

~ 

" ,. ~ ,. 

' 0 "" 

" " , '0 , 

'0 , 0 0 

" 75 76 77 78 79 80 I!!Il 82 " 7S 76 77 78 79 eo 81 62 

,~ 

e::;z] SU"'~'ER ~ WitHER "", lZZI SUMMER m WINTER 

Figure 81.--Average S concentration 

observed at sPa. 

Figure 82.--Average As concentration 

observed at sPa. 

" ~------------------------------------, 

" 

, 

• 

, E ' 

[ , 

, 

11 75 76 71 78 79 80 81 82 

~, 

tz::ZI 5Ut,lMER ~ .... ~T(R 

Figure 83 . --Average Se concentration 

observed at sPa . 

5.11 Electric Fields and Currents in the Vicinity of a Mountain 

I. Tzur and R. G. Roble 

National Center for Atmospheric Research, P.O . Box 3000 

Boulder, CO 80307 

Because the electric conductivity of the atmosphere increases almost 

expo nentially with altitude, the Earth's orography can play an important role 

in the global electric circuit. In addition, the orography and its environment interact and produce local electric effects that are an integral part of 

the atmospheric electricity. The basic electrical parameters, namely the 

electric field, current, and ion conductivities, should be measured near mountain tops to avoid noise from air pollution, trees, buildings, and other local 

boundary layer disturbances. These electrical parameters depend on the altitude and geometry of the mountain and on atmospheric conditions like winds, 

clo ud s, aerosols, day-night variations, and solar events. To understand the 

atmospheric electric phenomena, the interaction between the electrical parame ters and these environmental conditions should be studied . At fiLa, elec tric 

field, current, and conductivity data are co llected along with valuable data 

on weather and atmospheric co nditions . 

134 
ElEtTR>C POTE MIAl, lOG 4> VI 

Figure 84 .--Distribution of electric 

potential and of current density 

over (a) a mountain peak and (b) a 

mountain plateau. The arrows indicate direction and intensity of the 

electric currents. 

In this research, a numerical model was developed that calculates the 

electric field and currents around various orographic features . The results 

s how that a mountain of a few kilometers in altitude, which extends in the 

horizontal to about 40 km or less, can amplify significantly the electric 

fie l d and current near its top; however, on a global scale the mountain ha s 

sma ll effect . When the horizontal extent of the mountain is larger than about 

50 km (Mauna Loa falls into this category), the current is increased at the 

top of the mountai n while relatively large vertical and horizontal currents 

develop in the large scale. These results are demonstrated in fig. 84, which 

s hows the electric-potential contours and current distribution around a mountain extending to about 20 km in the horizontal (fig . 84a) and a plateau ex -

tending to 100 km from its center (fig. 84b). The arrows represent the direction and intensity of the electric currents. 

Figures 85a and 85b show the contours of the electric potential a nd current for fair weather conditions, respectively, and figs. 85c and 85d show the 

same parameters when a cloud is situated above the mountain top. The surface 

electric field and currents for both cases are shown in figs. 86a and 86b. 

The calculated increase in the current is in agreement wit h the data collected 

EL£tlR,C POTEN1UL, l OG 4> tVI t ONOUC TION CU RRENT 110 ' A/m'l 

""'"T ---; " . - -\ . ",. 

I. J . . , " t .. .. 

~-:.. - . 

. . \-

-;;-~ " . .i 

Figure 85.--Distribution of electric 

potential and of current density 

flow around a mountain peak for (a) 

and (b) fair weather conditions, and 

(c) and (d) when a cloud is situated 

above the mounta in peak. 

135 
" 

;" t" '00 C 0.0 

(.; ~ 

1 

Co., ,-

Figure 86 .--(a) Surface electric 

field and (b) surface condu ction 

c urrent over a mountain peak for 

fair wea ther conditions and for when 

a cloud is situated above the mountain peak. 

a t NLO (Cobb, 1968). However , this research is in its beginning, and more de -

ta i l ed calc ulations of the Mauna Loa orograp hy and atmospheric cond itions must 

be done before further comparisons ca n be mad e . 

Acknowledgment 

NCAR is spo nsored by the National Science Foundation . 

5.12 Atmos pheri c Bromine in the Arctic 

W. W. Berg and P. D. Sperry 

National Center for Atmospheric Resear ch 

Boulder, CO 80307 

5 . 12.1 Introduction 

K. A. Rahn 

Graduate School of Oceanography 

Universi ty of Rhode Island 

Kingston , RI 02881 

E. S. Gladney 

Los Alamos National Laboratory 

Los Alamos, NN 87545 

Because of the potential ro l e that Br compounds may play in the stra t ospheric photochemistry of ozone (Wofsy et al., 1975; Yung e t al., 1980 ), increased attention has been fo cused on this halogen and its mov ement through 

the tropos phere. The geoc hemical pathway s of Br-containing s pecie s from 

oceanic, bio spheric, and anthropogenic sources have not been delinea t ed. 

Nounting evi dence suggests that a s ubstantial fraction of the gaseous and 

parti cu late Sr species found in the atmosphere has an oceanic sourc e either 

directly from seawa ter or indirectly from organisms in seawat er (Duce et al., 

1965; tloyers and Du ce, 1972; Lovelock, 19 75; Rahn et ai., 1976; Si ngh et ai., 

1977, 1983) . Smaller anthropogenic sour ces have been identi fied and include 

the production of CH 3Br, used as a soil fumigant; tetrabromobisphenol-A, used 

as a flame retardant in printed-circuit boards; CF3Br, us ed as a fire retardant a nd r efrige rant; and C2H.Br2, together wi th assorted brominated additives, 

used in automotive and other fossil fuels. The relative inte nsities of the 

various global sources of atmospheric Br compounds, however , r emain largely 

unknown. In additi on, r ecent stratos pheric measurements (e.g., Sedlacek e t 

al. , 19 79; Berg et al., 1980) have raised the possibility that one or more 

additional sources for atmospheric Br near the Earth's s urface remain to be 

identified. 

136 
'''~~~~~~~~~~~~~---~ 

HO~ 

p, 8,11 0_ , ':'10"0 (1,. ,.,. 15 7° ' .... ) 

- ,976 -11 

----- 1917 -18 

-- 978 9 

1979 -80 

:'Pt.' 1982 ' :.) 

SEPT OCT " 0" DEC "~ ~ fEll "' .... " APR I.O.M JI,. ~ JUl 4UG SEPT 

DAT E 

5.12 . 2 Results 

Figure 87.--Particulate Br content 

of the Arctic aerosol for 1976-

1980 at BRW. This 4-yr data record represents a compilation of 

over 200 analyses . The points 

shown with the error bars (above A 

and B) correspond to the data 

presented in fig . 91. The conversion 1 ng SCM- 1 = 0.816 pptm was 

used for the aerosol data. 

The results of our particulate Br measurements at BRW during 1976-1980 

are shown in fig. 87. The inflection points in each curve represent a single 

measurement of the Br content in the Arctic aerosol. Over 200 data points 

were used to develop the Br aerosol plots shown in this figure. It is clear 

that during this 4-yr period the Br content in the Arctic aerosol increased an 

order of magnitude ove r the background a e rosol values beginning every midFebruary and continuing for a period of 3 months. The particulate Br content 

in the Ar c tic ae r os ol (Br ) during the sllnuner, fall , and winter months 

typically ranged at aboutP6 ± 4 ng SCM- 1 During the 3-mo Arctic spring period, however, the Br content of the aerosol rea ched over 100 ng SCM- I , with 

typical values ranging near 65 ng Snl- I 

Similar plots over the same 4-yr period are presented in figs. 88 and 89 

for particulate CI and I, respectively . Both of thes e halogens exhibit a 

distinctly different annual behavior compared with that of Br. During the 

3-mo Br maximum, the CI and I content in the Arctic aerosol show no significant change from typical background values measured throughout the year. 

Since the BRW aerosol is strongly influenced by the Arctic Ocean and its 

adjacent seas, the Na content of the aerosol was also determined over the 

1976-1980 period. Na is an espe cially valuable elemental index since it is 

" I 

" " 

O:'T£ 

PI &,,"'" tl.!n, kc 

(71· /1. '5 7 "W 

1916-17 

1977-78 

--- 1978 - 79 

1979-80 

Figure 88 .- - Particula t e CI content 

of the Arctic aerosol for 1976-

1980 at BRW. 

137 

'.~' PI B""o ... . 1I O 

( 7 1" ". 157"W ) 

-1916-17 

1977 - 78 

1978- 79 

1979-80 

, . 

SEPT oc r hO.' DEC J" '~ fEB "' '''I ~" ", ~y JU'l JUL AUG SEPT 

OH£ 

Figure 89 .--Particulate I content 

of the Ar c tic aerosol from 1976-

1980 at BR\'. 
'" 4~~ 

, ' 

~ 4000 l 

~ ,~-

. ~ IDOOI- I \ , . U

= 2500 ., \ 

PI eQ"O ~ . .o '''Q :71' / •. 1~7' ) 

- 1916-71 

---. 1971-78 

---1978 -79 

1979 -BO 

; >000 ' •• /1", . ~ '''''' " i I: II \, '000 • -j)N 1'/i~'1t.- j \~ .. :, .. ' 500 ~ j ; ,Y: V ~~ ~ , ~ , ~- o "',,, . - '-- ~ ' " ~ .... -..: ... ,r 

-----_ ._ -- --------- JULI.o N O.oT[ I , , , I 

SEPT OCT NOv DEC J~N H B .... Iit lIP/I MAY JU Ii JUl AUG SEPT 

O.ol[ 

Figure 90.-- Particulate Na con t ent 

of t he Arctic aeroso l from 1976-

1980 at BRW. 

• u 

~ 

g 

w 

z 

0 • • m

-

" " , 

• ... 

'" ." 

". 

'" 

'" 

. ----------1 

1 __ ----..- t- --~~~ 

P' ''Q<! , 

{51 (41 

'" 

p--

.----1- __ _ 

(4 1 (9 1 ." • Teta! Ga"a<Jt B, 

• Tetal At ... el~~"1( 8, 140 3 ~ 

11l~ "' b., ot S'~ A oI,r"~l 0: IJud la Colc~lcl' .~n 112 2 1: 

~ 84 2 ~ 

. 56 1 1 

'" 

• 1200 0000 1200 0000 1200 0000 1200 0000 1200 oocx::r CW->7 1329 • ~ 6 8 27 

'" ALASKAN STANDARD TI ME (GMT -IOl 

Figure 91.--Gaseous and particulate Br data t aken at BRW during 

April and July-August 1982. The 

error bars represent one sta ndard 

dev iation of the mea n. The number 

of values included in the mean is 

s hown in parentheses. The conversion 1 pptv Br = 3 . 565 ng SCN -' 

l.Jas used. 

known to cross the air-sea inte r f a ce with no signi fican t enri chment i n t he 

aerosol relative t o seawater (Duce et a l. , 197 2 ; Duce and Hoffma n, 1976; Berg 

and Winc hester, 1978). Thp rtnn 1J rtl variation of Na in the Arctic aerosol over 

this 4-yr period is s hown in fig. 90 . The dominant s our ce for both Na and Cl 

in the Arc tic aerosol at BRW most proba bly is the oc ean. A detailed compa rison, peak by peak, of t he data In figs. 88 and 90 shows that t hese two e lements are closely coupled . 

The gaseous a nd particulate Br meas ur eme nts made during April and July -

August 1982 at BRW are s hown in fig. 9 1. During periods 1 and 2 in April, 

total gas-ph ase Br levels (Br ) averaged 422 ± 48 ng SCN-' ( 11 8 ± 14 pptv) 

g - - with a mi nimum va lue of 373 ng snl 1 a nd a maximum val ue of 498 ng snl 1 . Br 

averaged 52 ± 8 ng SCtl-' (42 ± 7 Ep t m) wi th total atmos pheri c Br levels p 

(Br t ot ) averaging 474 ± 49 ng SCN '. During periods 3 and_ 4 , however, all Br 

va lues s howed a marked decrease, with Br at II ± 5 ng SCN I, Br at 154 ± 

p- g 54 ng SCN- 1 , and Br 

1982 (period 5) s hoSg5 

27 ± 14 ng SCN - 1 . 

at 165 ± 54 ng 

very little Br 

SCN 1. The samples taken in July-August 

present, with the Br level averagi ng tot 

For comp arison, t he Br data in fig. 91 have be en plotted on the 4- yr 

particulate Br record shownP i n fig. 87 . The mean values of each of the four 

sa mp ling periods in April 1982 (a bove time line A in fig . 87) show c learly 

that the 1982 particulate Br data were no t atypica l for that time frame. The 

15 February-IS Na y Br aerosol peak that was observed in the 4-yr data record 

of fig. 87 was also present in 1982 at approximately the same strength. The 

gaseous Br l evels me as ured during April 1982 are als o probably typical for 

this period . This conclusi on is s upported by the fact that the gas-toparticle ratios plotte d in f ig. 91, running from 7 t o 18, are in the chara c -

teristic ra nge [or atmospheric Sr . 

138 
To ensure that the unusual gas phase Br levels did not occur at other 

times during the year, data were also taken during July-August 1982 (period 

5). As seen in fig. 87, this time frame represents a period in which the Arctic aerosol Br content is at a 3-mo sustained minimum. Figure 91 shows that 

the total atmospheric Br levels were, in fact, very low during this period. 

The corresponding Br levels, as expected, were also typically low for this 

p 

period as shown in fig. 87 (above time line B). The possibility still remains, however, that other periods may exist during a normal Arctic year in 

which high levels of gaseous Br products are present in the Arctic troposphere. In view of the above data, however, this possibility seems remote. 

5.12.3 Discussion 

A significant source (or group of sources) must exist that is capable of 

supporting exceptionally high levels of Br in the Arctic troposphere for periods of approximately 3 months. The source term must exhibit a strong seasonal 

dependence. It is unlikely that the Br comes directly from bulk seawater. 

Other potential sources include (1) local contaminatiod from power plant, oil 

well, or automotive emissions; (2) long-range transport, involving Br-containing gases and/or aerosols from anthropogenic sources possibly in eastern North 

America or from the Eurasian continent; (3) extraterrestrial input, entailing 

meteoric and other cosmic debris folding down from the low Arctic stratosphere; (4) natural terrestrial input, from the blooming of Arctic tundra or 

other flora; and (5) natural marine input, involving the production of brominated compounds in the water column, sea surface microlayer, or sea ice by 

various life forms including diatoms, dinoflagellates, and green, bluegreen, 

and red algae. 

The 4-yr Br data record was clearly subject to potential local contamination since no control was exercised over the wind direction during sampling. 

However, only the 3-mo aerosol peak period is of concern here since it has 

been shown t hat during the rest of t he year most of the Br appeared to be of 

marine origin . The data shown in fig. 91 were all taken during this 3-mo 

aerosol peak under rigorous clean-air sector-controlled conditions . During 

this peak Br episode (period 2), sampling was conducted entirely in the cleanair sector with winds from 60° to 100°. Hence, period 2 was most likely not 

subject to local contamination. 

A comparison of data taken in the Arctic with published values from other 

areas of the world reveals that t he Br content of the Arctic aerosol during 

the 3-mo peak period exceeds all other measurements made in the unperturbed 

troposphere by factors ranging from 5 to 10 . Gas phase Br levels also exhibit 

this same behavior. I,hen particulate and gaseous Br levels are considered 

together, the levels of total Br in the Arctic atmosphere during the 3-mo 

maximum exceed all measurements made in the natural troposphere by up to a 

factor of 10. A more comprehensive description and evaluation of this field 

study was given by Berg et al. (1983). 

Acknowledgments 

The field portions of this research were made possible by the help and 

support of B. Nendonca of GNCC. We also greatly appreciate the support of 

R. Fox and K. Bauer, the G~ICC observatory staff at BRW, who helped with the 

139 
measurements there. NCAR is sponsored by the National Science Foundation. Los 

Alamos National Laboratory is operated by the University of California for DOE. 

5 .1 3 Spectrum and Cross-Spectrum Analysis of Daily Meteorological 

and Chemical Data at BRW 

Iv . E. Raatz 

Geop hysical Institute, University of Alaska 

Fairba nks, AK 99701 

Time series of data can be analyzed by spectrum analysis in order to 

estimate wh i ch oscillations of a specific frequency (period) con tribute signifi cant portions to the total vari a nce of the time series. In this way, a 

time-series spec trum is analogous to an op ti cal spectrum, ind icating the contribu tion of different wavelengths or fre qu encies to the total energy of radiation. 

When two time series appear to be co rre lated, the correlation could be 

due to a correlation between high-frequency comp onents (short periods) or 

low-frequency comp onents (long periods) of the data. Two time series may 

appear t o be un corr elated because the l ow-frequency comp onents are negatively 

correl ated and the high-freq uency comp onents are positively correlated. A 

cross-spectrum analysis determines the coherence, which varies from a to 1 and 

is analogous to the square of a correlation coefficient. The coherence repre -

sents a frequency-dependent correlation coefficient. 

Daily data of noncrustal vanadium (XV) , noncrustal manganese (XI'ln ), surface temperature, and press ur e during 5 December 1979-30 April 1980 were subjected to a spectrum and cross-spectrum analysis program (SAS 79 , SAS Institute, Cary, N.C.). Gaps in the chemi cal data series were c l osed by filling in 

the data of the previous day. Some times sampl es were collected over 2 days 

instead of over I day. However, 2-day sampl es did not coi ncide with wee kends, 

which would produce an artificial period in t he s pe ctrum. The seasona l trend 

was removed by ca l culating mean va lues for each element for each mont h and 

subtracting them from t he actual data. Thus, our data set of temp erature, 

pressure, Xl'ln, and XV concentrations represents dai ly deviations from the 

monthly means. I nspection of t he time seri es o f the deviations showed that 

removi ng the monthly trend did not cause a distortion of the origi nal time 

series. 

In fig. 92 the power spectra for XV and XMn are presented . I n eac h case 

the 80% confidence limit is indicated. Both spectra have a similar appearance 

with several peaks . The XV spectrum reveals significant periods at 24.6-

18.5 days, 7.7 - 7.0 days, and 4.1-3.8 days. The Xlln spectrum reveals signi fica nt periods a t 8 . 7- 7.7 days, 49.3-29.6 da ys , 4.7-4.4 days , and 2.5 days. It 

appears that the spectrum of Xl'ln compared with that of XV is slightly shifted 

toward longer periods. The cross- spectrum analysis revealed that high coherency values of 0 . 93 and 0 . 78 were present in the periods of 7 . 0-6.5 days and 

21.1-1 6 .4 days, respectively. It should be not ed that highest coherency was 

fo und at the shoulders of the pea ks in the spectra and not at the peaks themselves. This high coherency, however, seems to support the overall high correlation coefficient between XV and Xl'ln. 

The power spectra for temperature and pressure are presented in fig . 93. 

It is obvious that these spectra are similar to each other but different from 

140 
-

;'~N 'I 

L 0 1 

W 

~ ::0 

;:: 

<f) 

W 

>-

CUi 

Z 

~OOI 

-' '" a: 

cu 

w 

Cl. 

<f) 

0-001743015 10 8 76 5 4 3 

PERIOD (DAYS) 

2 

I.ocr-.--,---,r-r---,----,---,--- -----,-c:] 

>-

CUi 

z 

~ 0.01 

-' '" a: 

cu 

w 

Cl. 

<f) 

0.00174 301510 8 7 6 5 4 3 

PERIOD (DAYS) 

2 

Figure 92 .--Power spectra for (le ft ) excess va nadium and (right) excess manganese, for 5 De cemb er 1979-30 Apri l 1980 at BRW . The 80% confidence limit is 

indicated. 

the power spectra of XV and X1'ln. The spectra of t empera ture and pressure fall 

off rapidly with sma ller periods and do not s how as mu ch detail as the spectra 

of XV and X1'ln. The pressure spect rum reveals significa nt periods at 29.6 -

21 . 1 days and 6.4- 5 . 9 days . The tempera ture spec trum reveals significa nt 

periods at 21.1 -1 6.4 days and 4.9 - 3 . 8 days. In t his case, the spectrum of 

pressure seems to be slightly s hift ed to longer periods than t he spectrum of 

temperature, ana l ogous to X1'ln and XV . Applyi ng a cross- spectrum ana lysi s on 

temperature and pressure resu l ted in a coherency of 0.86 in the period of 

4 . 3- 4.0 days. Again strong coherency was not present between the centers of 

the peaks but was di splaced to t he shoulders of the peaks . Cross-spectrum 

ana l ysis between the meteorologica l elements and the chemi cal e lements resulted in overall wea k coherences . Some stronger coherence s were s uggested 

but never occurred within the significant periods. Therefore , the significa nce of these coherences appears doubtful . 

The following hypothesis is presented to explain the signficant periods 

found i n the spectra . By inspecting daily weather maps it can be estimated 

that about every 6-7 days polluted air masses were injected over sour ce r egions in midlatitudes . On t he average, such injections lasted fo r about 4-

5 days . These two periods seem to be refle cted i n the spe c tra of XV and X1'ln. 

Investigation of height-time cross sections of potential t empera tu re and mixi ng ratio a t BRW for December-Harch showed that the presence of Ar ctic and 

141 
100 

~ 

E" 0 

w 

!;r 

~ 

>-

<f) 

w 

>-

C:: 

<f) 

z 

w 

0 1 

-l 

« 

a: 

>-

u 

w 

CL 

<f) 

0. 1 ~~"""C+*",-!--':---!-----=---±----' 7430 15 to 8 7 6 5 4 3 2 

PERIOD (DAYS) 

Figure 93 . --Power spectrum for (left) 

5 December 1979-30 April 1980 at BRW. 

100 

~ 

N SI 

~ 

W 

!;r 

~ 

>-

<f) 10 w 

>-

>-

u; 

z 

w 

0 

-l 

« 

a: 

>-

u 

w 

CL 

<f) 

74 30 15 10 8 7 654 3 

PERIOD (DAYS) 

temperature and (right) pressure , for 

The 80% confidence limit is indicated. 

Pacific air masses seems to alternate with a period of about 18 days. The 

presence of Pacific air at BRW l asted for about 4-5 days; Arctic air was usually present over a longer time. Therefore, it appears that the large-period 

peaks in all four spectra can be associated with the varying influence of 

Pacific a nd Polar air, or in other words, the large-scale synoptic situation. 

Pacific air is clean ; Arctic air is polluted. The peak at small periods in 

the pressure and temperature spectra mi ght reflect the duration of Pacific air 

present. 

In summary, spectrum and cross spectrum analyses suggest that the largescale variations of the atmosp here are represented in the long periods of the 

spectra of all four parameters investigated. The peaks in the smaller periods, however, are due to different physical processes and therefore are not 

correlated with each other. In the case of XV and X1'ln, the peaks can be explained based on the frequency and duration of pollution surges in midlatitudes. Peaks in the spectra of temperature and pressure can be explained by 

the l ocal synoptic conditions. 

Acknowledgments 

This research was sponsored by ONR (ONR:N-00014-C-0435) and NSF (Grant 

DPP79-19816). K. Rahn of URI kindly provided the chemical data. 

142 
5.14 Changes in the Seasonal Amplitude of CO 2 at MLO 

L. P. Steele 

National Research Counci l Resident Resear ch Associate 

Geophysical Monitoring for Climatic Change, Boulder, CO 80303 

The GMCC conti nuous CO 2 data from MLO for 1975-1982 inclusive have been 

analyzed for evidence of changes in the amplitude of the seasona l cycle. The 

primary data used were daily mean values after a preliminary selecti on procedure had been carried out by W. Komhyr. The method us ed for the analysis was 

essentia lly identical to that described by Ba castow et al. (1981a), in which a 

long-term trend was fir st removed from the data. It was removed in th is work 

by fitting a cubic spline to the monthly means . Knots were located every 12 

months (January of each year), and the spurious end effects of the splinefitting procedure were overcome by appending 2 years of monthly data (suitably 

adjusted for an estima ted long-term trend) to each end of the time series. 

The next step was to generate 5-day mean values from the daily data (including one 6-day va lue i n February of each leap year), and then t o subtrac t 

the long-term trend from these data by eval uating the fitted cubic spli ne at 

each 5-day point. A function of the form S = a sin 2nt + b cos 2nt + 

c sin 4nt + d cos 4nt (where t is in years) was fitted by methods of linear 

least squares to the resultant 5-day values to determine the parameters of an 

average an nual cyc le. Finally, each year of the detrended 5-d ay data was 

taken in turn and a function go + glS was fitted. The resultant values of gl 

are thought to provide an estimate of how the amplitude of the seasonal cycle 

in any year compares to an average val ue taken over all availa ble yea rs . As 

expected, the va lues of go are close to zero in each case . The va lues of g l 

as percentages (re lative to the average seasona l amplitude) are 91.9, 103 . 8, 

103 . 5, 98 . 0, 98 . 2, 100.0, 99 .0, and 109.9, for 1975-1982 respec tive l y. 

If these values of gl are regressed linearly with time, a slope of 1 . 1 ± 

0.8% yr- 1 is obtained . This result comp ares closely wit h that r eported by 

Ba castow et al. (1981b) for 11 yea rs of CO 2 flask da t a ( 1970-1980) collected 

at Station P in the north Pacific . Nevertheless , some cau tion is urged in the 

interpretation of the results from the present ana lysis . First, the se l ection 

of the MLO data is no t yet comple ted . Second , the largest val ue of gl occurred f or 1982, a year of a very strong El Ni~o event . Further, when the 5-day 

data for 1982 were plotted together with the fitted function go + g lS for that 

year , it was obvious that the function did not provide a good description of 

the minimum in the da ta, with the difference between the two be ing approximately 1 ppm. This featur e was a lso evi dent in the data for 1976, another 

year with an El Ni~o event. 

It would seem to be necessary t o make some explicit allowance for the 

perturbations in the amplitude of the CO 2 seasonal cycle that are ca used by 

these El Ni~o eve nts prior to searching for evidenc e of changes in the amplitud e that may be due to ot her ca uses such as a global increase in the l evel of 

photosynthetic activity. Such a scheme has been described recently by Bacastow et al. (1983) , where the va riation in atmospheric CO 2 was modeled as the 

s um of three independent comp onents: (I) growth in us e of fossil fuel, (2) the 

seasonal cycle (with allowa nce made for changes in ampl itude), and (3) a measure of the Southern Oscillation. They reported a growth in amplitude of the 

cycle at MLO of 0.75 ± 0 . 06% yr- 1 over the period 1958 -19 83. A particularly 

noteworthy feature of this result i s the small error t erm , which differs mark -

edly from the erro r found i n this work and the errors quoted previously by 

Sacastow et al . (1981a , 1981b). 

143 
6. INTERNATIONAL ACTIVITIES 

The monograph on the status of U.S. aerosol research and climatic implications, which is being written in parallel with a U.S . S.R . effort under the 

sponsorship of the U.S.-U.S.S.R. Working Group VIII Committee on the Environme nt, has progressed beyond the planning stage. Several contributions were 

submitted to the U. S. Chief Editor, G. Robinson, for review. See GtlCC Summary 

Report No . 10 (Bodhaine and Harris, 1982, sec. 6), for additional details on 

the U.S.-U.S.S.R . joint monograph . 

A workshop was hosted by GMCC i n Boulder on 8-9 February 1982 to write 

chapter 2, "Soil Aerosols," of the U. S . contribution for the Aerosols-Climate 

Assessment Monograph being prepared under the U. S.-U .S. S.R. Working Group VIII 

scientific exchange program. Participants were J. Prospero of University of 

Miami, C. Patterson of Georgia Institute of Technology, M. Jackson of University of \Yisconsin, J . Rosinski of NCAR, and D. Gillette, convener, of GtICC . A 

first draft report was largely completed reviewing U.S. research over the last 

5 years. The Soviet side will be preparing a similar report reviewing their 

literature. 

Funding was received in 1982 from EPA, CtIA, and Wl'10 for automation of six 

Dobson ozone spectrophotometers for Umkehr observations at a select global 

network . The stations within this network have been tentatively identified as 

MLO; Poker Flat, Alaska; Haute Provence, France; Pretoria, South Africa; 

Huancayo, Peru; Perth, Australia; and Boulder, Colo. For more details, see 

sec. 4.3. 

GMCC continued the program to upgrade foreign Dobson spectrophotometers 

under the auspiccs of 1-'1'10 (see sec . 3 . 2.2). The calibration check, of Dobson 

spectrophotometers in the global network continued; details can be found in 

sec. 3 . 2 . 3 . 

CIRES Research Assistant, A. Chopra of the Indian tle t eorological Service, 

New Delhi, India, who began temporary employment with GMCC in December 1980, 

continued ~ork during 1982 in assisting with development and testing of ECC 

ozonesondes for high altitude use (up to 40 km). Emph asis in the research was 

accurate meas ur ement of so nde pump efficiencies in the range 50 - 2 mb. Chopra 

also helped with routine ozo ne soundi ngs and sonde data processing in Boulder, 

as well as with logistics of the MLO ozone sounding program, including data' 

processing . Furthermore he participated in a program at Hilo, Hawaii, in 

Septemb er 1982 to measure ozone and S02 in the presence of the El Chichon 

volcanic cloud, a nd assisted with Dobson instrument optical adjustments and 

calibra tions from key station s of t he world. 

W. Komhyr traveled to the Main Geophysical Observatory in Leningrad, 

U.S . S .R, 23-29 tlay 1982, under the auspices of the U.S. - U.S . S.R. Working Group 

VIII Committee on the Environment, to check on progress of the Soviet scientists in establishing a facility for co l lecting air samples from ocean Station 

C i n the North Atlantic, and in analyzing the sampl es for atmospheric CO 2 

content . During a visit to Boulder earlier, A. Shashkov of the Main Geophysical Observatory studied GMCC methodologies for CO 2 monitoring and obtained 

specifications for building a semiautomatic CO 2 analyzer apparatus (Komhyr et 

al., 1983). Tests co nducted on the apparatus built in Leningrad by Shashkov 

a nd co lleagues indicated highly satisfactory performance. 

P. Obtinario, a meteorologist from Pagaso Weather Bureau, Philippine 

Meteorological Service, visited GMCC in Boulder during II August- 3D September 

144 
1982 under a Wl'10 fellowship to obtain training in operation and calibration of 

Dobson ozone spectrophotometers and to obtain information on all facets of t he 

GMCC ozone program. During his visit, Manila Dobson instrument no . 52 was 

shipped to Boulder, repaired, and recalibrated . The majority of Obtinario's 

training goals were achieved, even though his planned duration of stay in 

Boulder was curtailed for health reasons. 

P. Steele from Australia began a l-yr term as an NRC-NOAA Research Asso -

cia t e on 15 September 1982. His objective is to continue work on carbon cycle 

mode ling begun during the previous year whil e visiting GMCC as a CSIRO Postdoctoral Student. 

P. Fraser of the CSIRO Division of Atmospheric Physics (now Atmospheric 

Research) arrived at GMCC during November 1982 to assume a l-yr position as a 

CIRES Research Associate sponsored by GtICC. This appointment continues an 

informal, reciprocal arrangement for cooperative overseas study by research 

staff of NOAA and CSIRO . The major purpose of the visit is to make detailed 

comp arisons of gas chromatographic and IR absorpti on techniques for the measurement of CO 2 co ncentrations in the atmosp here, and to evaluate the feasibility of measuring methane and carbon monoxide through the GMCC global flask 

sampling network. 

During 12- 18 December 1982, E. Dutton participated in a NASA- sponsored 

flight program based in Acapulco, Mexico, to measure optical properties of the 

s tratospheric cloud ca used by t he eruption of El Chi chon. In cooperation with 

the Mexican and Ca nadia n meteorological services , this program involved measurements along 120 0 W longitude between 60 S and 20 0 N latitude. 

Flask sampling for C02 at Sta nley, Falkland Islands, ceased on or about 

1 April as a result of local hostilities. The last shipment of samples was 

received in Boulder on 7 April and included those collected through 4 Febru -

ary . Word was received in November that t he 64 flasks and p3 samp ling apparatus then on hand had been l ost . 

Arrangements we r e made in J une 1982 with the British Antarctic Survey to 

begin weekly coll ec tions of CO 2 flask samples at Halley Bay, Antarctica, commenci ng i n 1983. The initial supply of flasks was sent to England to be transpo rted to the station by the supply ship RRS BRANSFIELD. The first year's 

sample s are expected in Boulder by June 1984. 

Arrangements were made through L. Heidt, NCAR, for a cooperat i ve sa mp ling 

program to be carried out by M. Verstraete, NCAR GHOST Flight Stati on, Christchur ch, New Zeala nd , at Kaitorete Spit, South Island, New Zealand, a coastal 

site about 50 mi from the city. Samples are collected in stainless steel evac -

uated co ntainers once per week. L. Heidt provides one container each week for 

the exclusive use of GMCC for CO 2 analysis . The first samples were collected 

on 25 October 1982; regular weekly sampling began on 14 December 1982. 

B. Mendo nca visited Brazil, Chil e, and Peru fr om 26 November t o 20 December at the request of \,rt10 as a consultant to the BAPtloN program in these cou ntries. In Brazil, siting criteria and identification of potential locations 

fo r the establis hment of stations were discussed. Instruments "ere installed 

and the measurement program commenced on Easter Island. A review of 1 year of 

BAPMoN operation, da t a collection, and instrument maintenance at the Huancayo 

and Cosmos sites in Peru was made. 

145 
7 . PUBLICATIONS AND PRESENTATIONS BY GHCC STAFF, 1982 

Bodhaine, B. A. Background aerosol measurements at four remote sites . Preprints, Second Symposium, Comp osition of the Nonurban Troposphere, 

Ihlliamsburg , Va., 25-28 tlay 1982, American Heteorolog ical Society, 

Boston, Hass., 154 -1 58 . 

Bodhaine, B. A. The GHCC four-wavelength nephelometer. In Light Absorption 

£.Y. Aerosol Particles, H. E. Gerber and E. E. Hindman (eds.), Spectrum 

Press, Hampton, Va. , 149-168. 

Bodhaine, B. A., and J. H. Harris. 

condensation nucleus counter. 

Calibration formulas for the Pollak 

~ Aerosol Sci. 13(2): 121-1 26. 

Bodhaine, B. A. , and J. H. Harris (eds.). 

Change, No. 10 : Summary Report 1981. 

t ories, Boulder, Colo. , 158 pp. 

Geophysical Honitoring for Climatic 

NOAA Envirorunental Research LaboraCharlson, R. J., T. Silver, A. D. Clarke, and B. A. Bodhaine. Comments on 

"Transport of Asian Desert Aerosol to the Hawaiian Islands." ~ ~ 

tleteoro1. 21(11) : 1775- 1776 . 

Cline, J. D., R. H. Gammon, and D. Ihsegarver . Heridional distribution of 

dissolved Freon-I I in the eastern North Pacific Ocean. Paper 41A-4 presented at Ocean Sciences: AGU/ASLO Joint Heeting, San Antonio, Tex., 

16-19 February 1982. 

Dutton, E. G., a nd J. J. DeLuisi . Results of a sunphotomptpr intercomparison 

held at Boulder, 19 October to 16 December 1981. NOAA Tech. tlemo . ERL 

ARL-1l4, NOAA Environmental Research Laboratories, Boulder, Colo., 47 pp. 

Gammon, R. II., and J. Bullister . Age-dating the North Atlantic deep water 

with chlorofluoromethane transient tracers. Paper presented at the AGU 

Fall Heeting, San Francisco, Calif., 7-15 December 1982. 

Ga~non, R. H., and J. Bullister. Freon penetration into the North Atlantic 

deep water. Paper 41A-3 presented at Ocean Sciences: AGU/ASLO Joint 

Heeting, San Antonio, Tex., 16-19 February 1982. 

Ga ~non, R. H., and W. D. Komhyr. The global atmospheric CO 2 monitoring net-

.'ork of GtICC/NOAA. Paper presented at the Carbon Dioxide Research Con -

ference: Carbon Dioxide, Science and Consensus, Berkeley Springs, W. Va ., 

19-23 September 1982, sponsored by DOE. 

Ga mmon, R. H., J. Cline, and D. Wisegarver . Chlo rofluorome thanes in the 

Northeast Pacific Ocean: Heasured vertical distributions and application 

as transien t tra cers of upper ocea n mix i ng. ~ Geophys. Res. 

87(C I2):944 1-9454 . 

Gillette, D. A. Decomposition of annual patterns of atmospheric carbon 

dioxide concentratio ns: A preliminary interpretation of one year of data 

at 13 globally distributed locations. Atmos. Environ. 16(11 ):2537 - 2542. 

Gillette, D. A. Future research in resuspension. Paper presented at the 

Fourth International Conference on Precipitation Scavenging, Dry Deposition, and Resuspension, Santa Honica, Calif ., 28 November- 3 December 1982. 

146 
Gillette, D. A. Threshold velocities for wind erosion on natural terresLrial 

arid surfaces (a summary). Paper presented at the Fourth International 

Conference on Precipitation Scavenging, Dry Deposition, and Resuspension, 

Santa Honica, Calif. , 28 November- 3 December 1982. 

Gill ette, D. A., and C. Cowherd. The concept of resuspension rates applied to 

problems of fugitive dust emissions and wind erosion. Paper presented at 

the Fourth International Confere nc e on Precipitation Scavenging, Dry Depos ition, and Resuspension, Santa Honica, Calif., 28 November-3 Decemb er 

1982. 

Gillette, D. A. , J. Adams, D. Huhs, and R. Kihl . Threshold fri c tion velocities and rupture moduli for crusted desert soils for the input of soil 

particles into the air. L Geophys. Res. 87(CI1):9003-9015 . 

Harris, J. H. The GHCC Atmospheric Trajectory Program. NOAA Tech . Hemo. ERL 

ARL-ll6, NOAA Environmental Research Laboratories, Boulder, Colo ., 30 pp . 

Herbert, G. A., J . H. Harris, B. A. Bodhaine, and S. J. Oltmans. Variations 

of atmospheric trace constituents meas ur ed during periods representative 

of the background troposphere at Hauna Loa Observatory . Preprints, 

Second Symposium, Composition of the Nonurban Troposphere, Ihlliamsburg, 

Va., 25-28 Hay 1982, American Heteorological Society, Boston, Hass., 

209-213 . 

Mendonca, B. G., J. J . DeLuisi, and J. A. Schroeder. Arctic ha ze and solar 

irradiance me asurements at Barrow, Alaska. Preprints, Second Symposium, 

Comp osition of t he Nonurban Troposphere, Williamsburg, Va., 25-28 Hay 

1982, American Heteorological Society, Boston, Hass., 176-178. 

Hiller, S. W., and B. A. Bodhaine. Calibration of Pollak co ndensation nu clei 

counters using charged, monodispers e aerosols. J . Aerosol Sci. 13(5): 

419 - 428. 

Miller, S. W., and B. A. Bodhaine . 

condensation nuc lei counters: 

13(6) :481-490. 

Supersaturation and expansion ratios in 

An historica l perspective. J. Aerosol Sci. 

Oltmans, S. J . , and J. London. The quasi-biennial oscillation in atmospheric 

ozone . J. Geophys. Res. 87(11):8981-8989. 

Osborn, J., J. DeLuisi, and R. Fegley. Stratospheric lidar investigations of 

the Ht. St. Helens volcanic cloud over Boulder, CO. NOAA Tech. Memo. ERL 

ARL-llO, 45 pp. 

Patterson, E. H., B. A. Bodhaine , A. Coletti, G. W. Grams. Vol ume scattering 

ratios dete rmined by the polar and the integrating nephelometer : A comparison . ~ ~ 21(3) : 394 - 397 . 

Peterson, J. T., W. D. Komhyr, T. B. Harris, and L. S. Waterman . Atmospheric 

carbon dioxide measurements at Barrow, Alaska, 1973-1979 . Tellus 34(2): 

166-175. 

Radke, L. F ., B. A. Bodhaine, G. A. He rbert, and J. H. Harris. Aerosol light 

scattering and condensation nucl e i measurements at Barrow, Alaska (discussion). Atmos. Environ. 16(5): 1274-12 75 . 

147 
Schnell, R. C. Airborne ice nucleus measurements around the Hawaiian Islands . 

~ Geophys . Res . 87(Cll):8886-8890. 

Schnell, R. C. Increased production and reduced energy costs in snowmaking: 

Some recent research results . Ski Area tlanage . 21: 78-80. 

Schnell, R. C. (ed.). Report on the tlount Kenya Baseline Station Feasibility 

Study. Environmental Pollution tlonitoring Programme, No. 12, Horld 

tleteorological Organization, Geneva, Switzerland, 171 pp. 

Schnell, R. C., and S. N. Tan . Kenyan tea litter: A source of ice nuclei . 

Tellus 34:92-95. 

Schnell, R. C., S. H. tliller, P. A. Allee, and B. Hrobel. Ice nucleus measurement intercomparisons using three systems and three natural ice 

nucleants. Preprints, Conference on Cloud Physics, Chicago, Ill., 

15-18 November 1982, American tleteorological Society, Boston, tlass., 

119-122. 

Schnel l , R. C., R. F. Pueschel, and D. L. Hellman . Ice nucleus characteristics of tlount St . Hel ens effluents. J. Geophys. Res. 87(CI3): 

11109-11112. 

Thompson, T. tI., and S. K. Cox . Subtropical climatology of direct beam solar 

radiation. ~ ~ tleteo rol. 21(3):334- 338 . 

148 
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158 
9 . GHCC STAFF, 1982 

Director's Office 

James Peterson, Director 

Bernard He ndonca, Deputy Direc t or 

Jeanne Kelsey, Secretary 

Carol Fee, CO-OP 

Paul Fraser, Guest Scientist, CIRES 

Dale Gillette, Physical Scientist 

Chandra Shastri, CIRES 

Gregory Siede lb erg, Electronic Technician 

Paul Steele, Guest Scientist 

Acguisition and Data Hanagement Group 

Gary Herbert, Chief 

Jo- Ann Garner, Secretary 

Richard Clark, Computer Programmer 

Edward Green, ClRES 

Joyce Harris, Computer Specia l ist 

Troy Higgins, Jr. Fellow 

Gloria Koenig, Computer Programmer 

Kenneth Thaut, Electronic Technician 

Honitoring Trace Gases Group 

Walter Komhyr , Chief 

Jo-Ann Garner, Secretary 

Ruth Alvirez , CO-OP 

~nar Chopra, CIRES 

Thomas Conway, CIRES 

Robert Evans, CIRES 

Richard Gammon, Chemist 

Robert Grass, Physicist 

Thomas Harris, Contract 

Kent Leonard, CIRES 

Samu el Oltmans, Physicist 

Frank Polacek, III, Heteorological Technician 

Steven Rush, CIRES 

Thayne Thompson, Physicist 

Kirk Thoning, CIRES 

Alberta Vieira, CO-OP 

Lee Waterman, Chemist 

Aerosols and Radiation Honitoring Group 

John DeLuisi, Chief 

Bonnie Hill, Secretary 

Barry Bodhaine, Meteorologist 

Kenneth Cameron, CIRES 

Forrest Cook, Electronic Technician 

Ellsworth Dutton, Heteorologist 

Daniel Endres, ClRES 

Stuart Naegele, CIRES 

John Osborn, NOAA Corps 

Kenneth Thorne, CIRES 

159 
Analysis and Interpretation Group 

John DeLuisi, Acting Chief 

Bonnie Hill, Secretary 

Joanne Edwards, CIRES 

Bradley Halter, ClRES 

Russell Schnell, CIRES 

Hauna Loa Observatory 

Kinsell Coulson, Director 

Judith Pereira, Secretary 

Arnold Austring, Physical Scientist 

John Chin, Physicist 

Thomas DeFoor, Electrical Engineer 

Steven Garcia, Contract 

Darryl Kuniyuki, Jr. Fellow 

Cynthia ~IcFee, NOAA Corps 

Hamoru Shibata, Electronic Technician 

Alan Yoshinaga, Analytical Chemist 

Barrow Observatory 

Randy Fox, Station Chief 

Daniel Bea rd, Station Chief 

Kenneth Bauer, Electronic Technician 

Timothy Wolfe, Electronic Technician 

Samoa Observatory 

Donald Nelson, Station Chief 

Roger Williams, Electronic Technician 

Efaraima Peau, W. G. Laborer 

South Pole Observatory 

Rusty Brainard, NOAA Corps, Station Chief 

Steven Fahnenstiel, Physicist 

Robert Williscroft, NOAA Corps, Station Chief 

Hark VandeRiet, Electronic Technician 

160