So Ilrl Reporl1984 

U.S.OEPARTMEIT 

OF COMMERCE 

IllATiOIAL 

OCEAIIC AID 

ATMOSPHERIC 

AOMIIISTRATIOI 

EIVIROIMEITAL 

RESEARCH 

LABORATORIES 

• 

• 

• 

• 
Geophysical Monitoring 

for Climatic Change 

No. 13 

Summary Report 1984 

Everett C. Nickerson , Editor 

Air Resources Laboratory 

Geophysical Monitoring for Climatic Change 

Boulder, Colorado 

February 1986 

u.s. DEPARTMENT OF COMMERCE 

Malcolm Baldrige, Secretary 

National Oceanic and Atmospheric Administration 

Environmental Research Laboratories 

Vernon E. Derr, Director 
NOTICE 

Mention of a commercial company or product does not constitute an endorsemen t 

by NOAA Environmental Research Laboratories, Use for' publicLLy 0" advertisi ng 

purposes of information from this publication concerning proprietary products 

or the tests of such products is not authorized, 
CONTENTS 

Page 

ORGANIZATIONAL CHART ••••••••••••••••.•.••••••••••••••••.••••••••••••.•••• v 

GMCC STAFF .••••••..•...••.••••••.•••••.••••••.•..•••••••••••••.••.•••.• • vi 

1 • SUMMARY •••.••..••.•.•••••••••.••••••.•••••••••••••••••••.•.••.•.•••• 1 

2. OBSERVATORY REPORTS •••.••••..•••••••.••••••••••••..•••••••••.••.•••• 3 

2.1 Mauna Loa •.••••••••.•.••.••••••••.••••.•••••.••••••••.••••.•••• 3 

2.2 Barrow ••.••.•••••••.•••.••••.••••••••••••••.•••••••••••.•••••• 10 

2 • 3 Samoa .••••••••.••••••••.••.••••••••••••••••••••••••.•.••••••.• 1 3 

2 . 4 Sout h Pol e .•.••••••.••••••••••.••.•.••••••••..••••••••••••.•.• 16 

3. AEROSOLS AND RADIATION GROUP ....................................... 20 

3.1 Continuing Programs ••.••••••••••.••.• . ••••••.•••••.••••.••..•• 20 

3.2 References ••.•.••••••.••••••••••..•.•••.••••••.•••••..•••••••• 29 

4. CARBON DIOXI DE GROUP ••••••.•.••••.•••••..•...•.••.•••••.••.•.••...• 30 

4.1 Continuing Programs .•.•••••.••• ••••.••••••••.••••••••.•••••••• 30 

4.2 Special Proj ects •.•••••..•••.•••.•..••••.••..••••••••••.•••••• 36 

4.3 References .................................................... 48 

5. TRACE GASES GROUP .•.•••••••••••.••••.••••••••••••.••••••••••••.••.• 51 

5.1 Continuing Programs ••••••••••••••••• •••••.••••• ••••••••••••••• 51 

5.2 References ••••••.•••.••.••••••••.••••.•••.••••••••.••••.•••••• 60 

6 . ACQUISITION AND DATA MANAGEMENT GROUP ••.••••••••••••••••••••••••.•• 62 

6.1 Continuing Programs ••••.•••••••.••.•.••.•••.••••••.•.••••••••• 62 

6.2 Atmospheric Trajectories ••••••• •••• • •••.•••.••.•••. • .•.••••••• 71 

6.3 References ••.•.•.•••..•.•.••••••.•••••.••.••••••••••••.••••••• 75 

7. DIRECTOR'S OfFICE ••••••.••••.•••••••..•.••••••••. •••.•••••••••••••• 76 

7.1 Continuing Programs •.••••••..•••.•.•.••••••.••••••.•••••.••••• 76 

Precipi tation Chemistry ••••••..•••••.•••.••••••.•••• . •.••.•••• 76 

(R. S. Artz) 

7.2 Cooperati ve Programs .•.••••••.• •••••• ..••.••••••••••.•.••.•••• 79 

Precipitation Amounts on Alaska's North Slope .•.•••••••••••••• 79 

(G. P. Clagett) 

6C" in Atmospheric C02 ....................................... 83 

(I. Friedman, J. Gleason, J. Stacey) 

Measurement of Ultraviolet Irradiance Between 290 nm 

and 325 nm •••••••••••••••••••••.••••••.•••.••.••••••••••.••••• 86 

(B. Goldberg) 
Recent Contributions of the Global Precipitation Chemistry 

Project ....................................................... 88 

(W. C. Keene, J. N. Galloway, G. E. Likens, and 

J. M. Miller) 

Trichlorotrifluoroethane (F-113): Trends at Pt. Barrow, 

Alaska ...•.................................................... 91 

(M. A. K. Khalil and R. A. Rasmussen) 

Detection of Atmospheric Tracers in Antarctica ................ 94 

(E. J. Mroz, M. Alei, J. H. Cappis, P. R. Guthals, 

A. S. Mason, T. L. Norris, J. Poths, and D. J. Rokop) 

Further Studies of Data Collected During the Arctic Gas 

and Aerosol Sampling Program (AGASP)--Spring 1983 ............. 97 

(R. C. Schnell) 

Atmospheric Submicron Particle Collection at the South 

Pole Observatory .........•................................... 102 

(R. E. Witkowski, W. A. Cassidy, and G. W. Penney) 

8. INTERNATIONAL ACTIVITIES .......................................... 104 

9. PUBLICATIONS AND PRESENTATIONS BY GMCC STAFF ...................... 106 

10. ACRONyMS ................•........................•...........•... 110 
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v 
GMCC Staff, 1984 

Director's Office 

James Peterson, Director 

Bernard Mendonca, Deputy Director 

Jeanne Kelsey, Secretary 

Roland Christofferson, CIRES 

Dale Gillette, Physical scientist 

Paul David Herrera, CO -OP 

Lori Neff, Scientific Data Clerk 

Everett C. Nickerson, Meteorologist 

Rita Rosson, Clerk-Typist 

R~ssell Schnell , CIRES 

Chandra Shastri, CIRES 

L. Paul Steele, Guest Scientist 

David W~ertz , CO-OP 

Acquisition and Data Management Group 

Gary Herbert, Chief 

Karen Ciocchetti, Secretary 

Bonnie, Hill, Secretary 

Richard Clark , Computer Programmer 

Teresa Davenport, Physical Science Aid 

Joseph Drewno, Physical Science Aid 

Edward Green, CIRES 

Joyce Harris, Computer Specialist 

Troy Higgins, Jr. Fellow 

Gloria Koenig, Computer Programmer 

Steve Roughton, Physical Science Aid 

Kenneth Thaut, Electronic Technician 

Aerosols and Radiation Monitoring Group 

John DeLuisi, Chief 

Karen Ciocchetti , Secretary 

Bonnie Hill, Secretary 

James Baumhover, Electroni c Technician 

Barry Bodhaine, Meteorologist 

Ellsworth Dutton , Meteorologist 

Linda Mitchell, CIRES 

Stuart Naegele, CIRES 

Martz Oryshchyn, Physical Science Aid 

Jeffrey Pratt, Physical Science Aid 

Timothy Quaken bush , Physical Science Aid 

Traci Simms, Physical Science Aid 

Kenneth Thorne , CIRES 

Wolfgang Raatz, NRC Postdoctoral Research Associate 

Carbon Dioxide Group 

Richard Gammon, Chief 

Rita Brown , Secretary 

Susan Dozier, Secretary 

Brian Anderson, Physical Science Aid 

Thomas Conway, Research Chemist 

Bryan Dickerson, CO -OP 

vi 
Christopher Fortescue, Physical Science Aid 

Tom Gorczyca, CIRES 

Bradley Halter, Meteorologist 

Gary Horton, CIRES 

Kenneth Masarie, CIRES 

Ted Myers, Physical Science Aid 

John Parker, CO-OP 

Kirk Thoning, CIRES 

Alberta Vieira, CO-OP 

Lee Waterman, Chemist 

Monitoring Trace Gases Group 

Walter Komhyr, Chief 

Rita Brown, Secretary 

Bradley Chaffee, Physical Science Aid 

Susan Dozier, Secretary 

Robert Evans, CIRES 

Marc Fish, Physical Science Aid 

Paul Franchois, CIRES 

Robert Grass, Physicist 

Thomas Jones, Physical Science Aid 

Kent Leonard, CIRES 

Samuel Oltmans, Physicist 

Frank Polacek, III, Meteorological Technician 

Thayne Thompson, Physicist 

Ronald Thorne, Physical Science Aid 

Barrow Observatory 

Daniel Beard, Station Chief 

Daniel Endres, Electronic Technician 

Steve Fahnenstiel, Station Chief 

Timothy Wolfe, Electronic Technician 

Mauna Loa Observatory 

Elmer Robinson, Director 

Judith Pereira, Secretary 

Arnold Austring, Physical Scientist 

John Chin , Physicist 

Thomas DeFoor, Electrical Engineer 

Thomas Garcia, Physical Science Aid 

GuoAn Ding, Guest Scientist 

Dorothy Johnson, Physical Science Aid 

Darryl Kuniyuki, Jr. Fellow 

Stephen Lent, Physical Science Aid 

Cynthia McFee, NOAA Corps 

Lisa McPherson, Physical Science Aid 

Mamoru Shibata, Electronic Technician 

Alan Yoshinaga, Chemist 

Samoa Observatory 

Donald Nelson , Station Chief 

Roger Williams, Electronic Technician 

Efaraima Peau, W. G. Laborer 

vii 
South Pole Observatory 

Frank Migaiolo, NOAA Corps , Station Chief 

Robert Platzer, Electronic Technician 

James Waddell, NOAA Corps, Station Chief 

Mark Mihalic, Electronic Technician 

viii 
GEOPHYSICAL MONITORING FOR CLIMATIC CHANGE 

NO. 13 

SUMMARY REPORT 1984 

1. SUMMARY 

At MLO , the main event of the year was the eruption of Mauna Loa on March 

25 and 3 weeks of lava flow down the northeast slope of the mountain. One 

effect was severance of the electrical power line to the observatory. A 

temporary generator was installed in late April and full , regular service was 

restored on July 24. New scientific activities during the year included 

upgrade of the lidar system, installation of a gas chromatograph for in situ 

CO 2 and CH4 measurements, initiation of weekly ozonesondes, and start-up of 

high precision UV radiation measurements. 

At BRW, the year was highlighted by smooth , uneventful operations. Both 

interi or and exterior of the observatory were renovated, including new 

carpeting , painting, and sound insulation. The GMCC and cooperative 

measurement programs had few problems . 

At SMO , we significantly improved facilities by adding a new remote 

sampling building on the ridge. This prefabricated structure will house both 

GMCC and OGe operations , but in separate rooms. The photovoltaic system 

received final testing and certification. The system is working well and 

generating solar-powered electricity at the observatory . The land lease for 

use of Samoan communal land was renogotiated for another 5-year term. 

Negotiations were rather delicate since a successor had not yet been chosen 

for Chief Iuli, Togi, who died in September 1983. 

At SPO , snow buildup around the CAF continued to be a major problem of 

growing concern. This is causing immediate logistical problems and the 

potential for severe drifting if CAF is not raised soon. A new meteorological 

tower was installed. Equipment performance for GMCC and cooperative programs 

was exceptional. 

The ongoing GMCC core measurement programs continued at the four 

observatories. These programs include CO 2, total column ozone, ozone vertical 

distribution, surface ozone, stratospheric water vapor, CFC-11 and -12, N20, 

stratospheric aerosols, volumetric aerosol scattering coefficient, CN 

concentration, solar radiation, meteorological variables, and precipitation 

chemistry. In addition, a wide variety of cooperative programs were conducted 

for university , other agency, and foreign investigators. 

In the Aerosols and Radiation Group, a computationally efficient model 

for direct and global solar flux in the atmosphere was adapted to the four 

observatories for comparison to our measurements. The model will be used to 

study anomalies in the data and to develop cloud climatologies. The special 

program for measurements of albedo at SPO continued . A thorough analysis was 

completed of the MLO lidar record from 1974-1983. The range of optical 
thickness exceeded two orders of magnitude from 

1977 to the striking El Chichon event of 1982. 

aerosol backscatter from El Chichon reached the 

a quiescent period in 1976-

The altitude of maximum 

remarkable value of 27 km! 

The Carbon Dioxide Group continued the long-term in situ CO 2 measurements 

at the observatories and flask analyses of CO2 and CH4 at 24 sites. The mean 

CO 2 global growth rate for 1984 was about 1. 5 ppm/year. The effects of the 

1982-83 El Nino/Southern Oscillation waned as the global CO 2 distribution 

returned to more normal patterns. The flask methane measurement program 

continued to mature, showing a long-term concentration increase of about 1% 

per year, distinct seasonal variations, and significant large-scale 

latitudinal gradients. Special projects included installation of a gas 

chromatograph at MLO to compare its results to the NDIR method of CO 2 

measurements, collection of flask samples aboard occasional oceanographic 

cruises (Long Lines Expedition to the equatorial and south Atlantic and NOAA 

DISCOVERER to the equatorial and north Pacific), and application of a twodi men sional carbon cycle model for comparison to the GMCC measurements. 

The Trace Gases Group continued responsibility for total ozone 

observations at 16 sites; the longest records date back to the early 1960's. 

A highlight of the year was the initiation of an agreement with NOAA/NESDIS 

for GMCC to provide data validation information for the SBUV/2 satellite-based 

ozone profiling instrument. GMCC measurements for NESDIS will include total 

ozone at 16 select Dobson sites, weekly vertical ozone profiles by ozonesondes 

at three sites, and vertical profiles by the Umkehr technique at seven 

automated Dobson sites. The program became operational in 1985. The 

observatory surface ozone records from 1973-1984 were analyzed for long-term 

trends. Secular increases at BRW and MLO contrast with decreases of SMO; the 

cause is postulated to be general circulation changes. Monthly balloon 

soundings of stratospheric water vapor at Boulder continued. Ongoing flask 

measurements of CC1,F and CC1 2F2 at the observatories showed long-term 

increases of about TO ppt/yr and 17 ppt/yr, respectively. 

The Acquisition and Data Management Group oversaw development and 

installation of a new data acquisition system at the observatories. Station 

climatologies showed , for example, an all-time record minimum temperature at 

Barrow of -50.0°C and near normal wind rose distributions at SMO and SPO . 

Many isobaric atmospheric trajectorles were computed with emphasis on Arctlc 

locations in support of AGASP, precipitation chemistry research, and Southern 

Hemisphere sites. Further development of the isentropic model included 

extension of the lowest surface to 1000 mb and capability to produce forward 

trajectories . 

Many scientists from universities and other government agencies continued 

to use the observatories as a base for cooperative research. Summary reports 

from several of these projects are included here . They cover such topics as 

precipitation quantification at Barrow, CO 2 isotope measurements, high 

resolution solar UV observations at MLO, analyses of background chemistry of 

precipitation, CFC-13 trends at BRW, description of the Antarctic Tracer 

Experiment, analyses of data from the AGASP experiment, and measurements of 

submicron particles from meteorites at SPO. 

2 
2. OBSERVATORY REPORTS 

2.1 Mauna Loa 

FACILITIES 

The major event for MLO during 1984 was undoubtedly the March-April 

eruption of Mauna Loa. There had been a 9-yr quiet period since the small 

summit eruption in 1975. 

The 1984 Mauna Loa eruption began at about 1 :30 a.m., March 25 with lava 

fountaining in the southwest corner of the summit crater. Within 2 to 3 

hours, 80% of the crater was covered by lava and there was concern that lava 

might flow from the crater toward MLO. Fortunately this did not happen 

because the eruptive activity soon shifted to the northeast rift zone . By 

about 5 p.m. on the 25th, the major activity had moved to the 9,200-ft level 

on the northeast rift, 2,000 ft below MLO, and concern over the safety of the 

facility lessoned greatly. 

The Mauna Loa eruption continued for 3 weeks until April 15. An early 

major impact on MLO operations was the inundation by flowing lava of the power 

line serving the Observatory on March 26 . After the eruption activity ceased, 

it was possible to set up a large motor generator on the power line about 10 

miles from MLO and beginning on April 28, this generator powered the 

Observatory until regular power-line service was restored on July 24. 

Throughout the eruption, considerable extra effort was required of the MLO 

staff and the staff of the NCAR High Altitude Observatory which shares the MLO 

site . In addition , vital cooperation was provided by the local electrical 

utility an d our local governmental agencies. 

The MLO observational routine was generally back to normal on the 

generator power on April 28, and the switch back to the power line in July was 

uneventful. USGS

6

Scientists estimated that the 1984 Mauna Loa er uption 

produced 220 x 10 m3 of lava and covered an area of about 48 km 2. The MLO 

staff was awarded a NOAA Special Act award for its service during the 

eruption . 

Elmer Robinson was appointed Director of MLO and assumed his position on 

July 1, 1984. 

A program to upgrade the MLO lidar system was begun in August with the 

support of a grant from EPA. 

A specially designed automatic gas chromatograph was put into service for 

CO 2 and CH q monitoring in March, taken out of service during the eruption, and 

put back into service in September. 

An ozonesonde program was begun in December . The bal l oon releases are 

scheduled weekly from the Hilo NWS station and are in support of the NOAA-F 

satellite SBUV observations to determine ozone profiles based on backscattered 

UV. Support for ozonesonde operations and other SBUV satellite support 

activities at MLO is provided by NESDIS. 

3 
The CAMS units were substituted for ICDAS in November and after the usual 

post-installation problems, operations were generally satisfactory in early 

December. It should be assumed that there were breaks in the records of most 

instruments during the ICDAS to CAMS changeover period of November 26-30 . 

Mr . GuoAn Ding, PRC, arrived at MLO February 22, 1984 to spend 

approximately 1 year as a visiting scientist. The purpose of his visit was to 

become thoroughly familiar with baseline monitoring so that he could guide PRC 

activities in this scientific area. His visit ended in January 1985. 

The safety of the MLO electrical system was augmented by operating each 

pump through a separately fused connector designed to blow if the pump load 

increases through an overload . This should guard against pumps overheating 

and posing fire hazards. 

PROGRAMS 

The principal programs carried out at MLO during 1984 are listed in table 

1. Brief comments on some of the programs are given below. It should be 

assumed, however, that all electrical instruments were down between March 25 

and April 28 because of the loss of the power line due to the advancing lava 

flow. 

Table 1.--Summary of sampling programs at MLO in 1984 

Prograz 

Gases 

----co; 

Surface ozone 

Total aioone 

Ozone profIle 

CFC-II. CFC-I 2, and N20 

Aerosols 

Condensation Nuclei 

Optical properties 

Stratospheric aerosols 

Skylleht polarizationSolar Radiation 

Global Irradlance 

Direct Irradlance 

I fl3trulIent 

URAS-2T Infrar ed analyzer 

3-~ glass rlask9 

O.S-L glass flasks, p3 

O.5-L glass fla3ks, throueh analyzer 

5-L evacuated glass rlasks 

Daslbl ozone meter 

Dobson speclrophotomHers nos . 63. 

65, and 16 

Dobson spectrophotOOleters n03. 63 . 

65, 76 

Balloonborne ECC 

300-IIIL stainless steel rIasks 

Pollak CNC 

G. E. CNe 

Four -wave leneth nephelometer 

Lldar 

Polarlzlne radiometer' 

Eppley pyranomelers with Q, G022, 

OGI, and RCB rllter!! 

Eppley pyrhellometers (2) with Q , 

rllters 

Eppley pyrhellometer wIth Q , OGI , 

RG2, and RCB rllters 

Salnpll ne 

frequC!ncy 

Cont I nuous 

1 pair Wk- I 

1 pair WI(-1 

1 pair wk- 1 

1 pall" WIe"'" 

Con t I nuous 

3 day-\ 

30a),-1 

1 wk- 1 

I pair wk- I 

Discrete 

Conti nuous 

Cont I nUOU3 

Discrete 

Discrete 

Conti nUOU5 

Conll nuous 

Discrete 

Remar ks 

MLO and Kumukahl 

seacoast 

HLO and Kumukahi 

HLO only 

HLO and Kumukahi 

No. 65, Jan-Jut 

Auto-Dobson 140. 16, 

Har-Dec 

Umkehr, Auto-Dobson 

No. 16 , Mar-Dec 

From Hila Airport 

beelnnlne. Dec 

Weekdays 

1150 , 550 , 700 , 850 nm 

6911 .3 nlll; av!~aee 1 

prof Il e wk 

320 . 365 , 1100, 500. 600. 

'(00 . SOD , 900 nil!; 

nar'rowband 
Table 1.--Summary of sampling programs at MLO in 19B4--Continued 

Prvgrall)s 

Solar Radlatlon--Cont. 

Direct Irradiance 

01 frl.se i rradl ance 

T\lrbldlty 

MeteorologY 

AII' Temperdtllr~ 

Oewpol nt te:Dperature 

Relatlv~ h~~lalty 

Press!Jre 

Wind (speed and direction) 

PreclpitaUun 

Total precipitable water 

PreCipitation Chemistry 

pH 

Cond!Jctlvlty 

Chemical compvnents 

Cooperative Programs 

CO2 (5jO) 

CO z. 1 C . NZO (SIO) 

Surrace S02 (r)Al 12 COZ' CO , CH~, CI ICt 

(CSIROl 

CO2 , CH~ and other trace 

gasest (/lCAR) 

Hrl01 and HCL vapor t 

(Colorado College) 

Total surface particles 

(DOE) 

Total suspended particles 

(EPA) 

Atmospheri c electricity' 

(rIOH) 

Ultraviolet radiation 

{Temple Unlv.l 

Ultraviolet radlatlont 

(Smithsonian) 

Precipitation cullectlon 

(DOE) 

Precipitation collect l ont 

( ISWS) 

Pr~cipitatlon cvllectlon 

(Unlv. o r Virginia) 

Wet-dry depo.>s\t i c,m 

( ISWS) 

Aeros ol chemistry 

(Unlv. of Maryland 

Aer osol chemistry 

(Unlv . or Arlzuna 

13C (USGS , Denver') 

Rad!ocarbunsl (USGS , 

Henl ..:. Park) 

Carbvn Mono xide 

(Hax Planck Inst.) 

Ozone and S02 

(AES. Canada) 

VariOUS trace gases 

(Ol'egvn Grad. Center) 

In.jtr.lmt'flt 

Eppley pyrhellumcte., with 13 filters· 

Eppley/Kendall active cavity radlometer 

Sampling 

r"eQuency 

Continuous 

Discrete 

Eppley pyranometcr Io'IUl ~hatJlne disk Contim.:ous 

and Q fill er' 

J-ser I es 1982 s~nphc,tOllleter:5 Discrete 

WPL seven-lo';Jvl;;!erlt\Lh sunplluLomeLerPHOO three-waveleneth sunpholometer 

ThermlstOl" (aspiraLe,l) 

Max .-mln. thermometers 

II ygr,:,t hermugf'ol ph 

Oewpolnt hygrometer 

Hygrvthermograpll 

CapaCitanc e transducer 

Hlcrobaroeraph 

/-ter'curlal bar<'>'Tlder 

Bend I x Aerovane 

Rain gauge, 8-in 

Rain gauge, 6-ln 

Rain gauge, weighing 

HAO Inf."ared hy~rumetef' 

pH meter 

Conductivity brld~e 

Ion ch r vmatograph 

Infrared analyzer (Applle<i Physics) 

S-L evaouated gl~~~ fl~ak~ 

Chemical bubbler system 

Pre~surlzed gl.JSs flask :;limple 

Evacuated stainless :iteel fla::;ks 

SpecIal sampling system 

Hlgll-volume ~olmplef' 

High-vo lume SolClplcr 

field mill , all' condu~tivlty meter 

Ultraviolet ranlumeter (~I'YLhema) 

7-wavelength UV radiometer 

Exposed collection pails 

Aerochemetr\c utom~tic co\\ectur 

Aerochemetrlc automatiC ~~llectur 

Aerochemetric aut~matic QQllectur 

Nucleporc rlfters 

Quartz rUters 

10-L stainless steel f1a.jks 

"aOiI collector 

Chcmlcal reacti (m with 11130 

Brewer HK I spectrophotometer 

Stainless steel flasks 

ConUnuous 

Cuntinuous 

COllt I ~~o!Js 

I day 

CUllt I nuous 

Cont.ln~0.J9 

CrmtlnuCJus 

Cuntlnuous 

C(JIltl nuol.S 

Discr(:le 

ContlnJuus 

1 da),-l 

1 Io'k- 1 

Continuous 

ConlinuCJus 

Discrete 

Discrete 

Discrete 

Cont I nuous 

1 palrlo'k- 1 

Ev(:r"y 12 days 

1 mo- 1 

pall' wk- I 

periods yr- 1 

ContinuOUS 

J::very 12 days 

Cont I nJOUS 

Cant I nuous 

ContinuOUS 

Con tlnuC/us 

Continuous 

Conlin .. ous 

ContlnuolJS 

Cont I fHJOUS 

Cont I nuous 

Biweekly 

Oiscf'~le 

Cor,t I nU'JUs 

'indicates program discontinued during 198Q. 

tIndicates new program initiated during 198~. 

5 

Remarks 

380 , 500 , 776, 862 nm; 

narrowband 

]80, ~22, 500 , 596 , 660 , 

776, 862 nm; nal"rllwband 

380, 500 , 778 n~; 

narrow blind 

2 III helgtlt 

Stdndard .jhe!ter 

HLO a"d K ... lanj Hguka 

HLO and K ... lanl Hauka 

6 PI height 

Kulanl Mat.ka 

Ralnlo'at~r collect l uns , 5 sites 

Rainwater collectlons, 5 sites 

Ralnlo'ater co 11 ectlciOs , 5 sites 

~LO and Kumukdlli 

2~ hr (OO-2~ hI') sa:aple 

MLO , started feb 

HLO and Kum!Jkaill 

first sample In Oct at HLO 

Dependent on ~lnd direction ; 

1 filter wk 

21j-hr (00-2Q hr) sample 

Radiation r'esponslble ( or sunburning of of sk i n 

Measurements began Aug 

AnalysiS (or 7SE and lOBE 

started feb 

Organic acid analysis 

tlA DP 

Upslope·d~wnslope d lscrl mlnatl,;,n 

Upslo~-d~lo'nslope dlscrimlnatiun 

I~LO and Kumukah l 
Carbon Dioxide 

The concentration of atmospheric CO 2 was monitored continuously by the 

URAS-2 infrared analyzer during 198~. The instrument performed sati sfactorily 

without major problems. Preliminary results indicate that the rate of 

increase of CO 2 concentration was approximately 1.35 ppm yr- 1 for 198~. 

The weekly CO 2 flask sampling programs at MLO and Cape Kumukahi were 

continued during the year. No flasks were lost or broken during shipment 

during the year. Some special flask samples were taken during the Mauna Loa 

eruption , but because of the extensive plume over much of the island they were 

of questionable value. 

Outgassing from the volcanic caldera at the summit of Mauna Loa and from 

vents along the northeast rift caused disruptions of some of the CO2 records 

in every month of the year. As in past years, it occurred mainly between 0000 

and 0800 LST during the downslope wind regime. The frequency of the monthly 

occurrences are listed in table 2. The frequency of outgassing increased very 

markedly after the March eruption of Mauna Loa. Fume emissi ons and steam from 

one or more vents along the upper portion of the northeast rift zone were 

frequently visible. During the actual er uption , MLO as wel l as the whole 

Island of Hawaii, was frequently enveloped in volcanic plume. 

Table 2.--Monthly occurrences of outgassing from the 

volcanic caldera on Mauna Loa during 198~ 

Jan Feb Mar Apr May Jun Jul Aug Sep Oct Nov Dec 

No. of days ~ ~ 10* * 1 ~ 19 16 25 18 22 21 

Percent of days 13 1 ~ ~2* * ~5 63 52 81 60 71 70 

*Mauna Loa eruption on March 25 interrupted the CO 2 record from March 25 to 

April 28, 198~ . 

Ozone 

Total ozone in the atmospheric column was measured routinely during 

198~. In addition , the Dobson spectrophotometer was used for measuring the 

ozone profile by the Umkehr technique on 5 days per week until the automated 

Dobson went into regular service in June. 

1 ~ 

~5 

On March 12, automated Dobson No. 76 was put into service at MLO. The 

Mauna Loa eruption and other start-up problems delayed the collection of 

satisfactory data until June. Dobson observations were made during the power 

interruption using the manual instrument and a battery power source . Manual 

Dobson No. 65 was operated in parallel with the auto-Dobson i n June and July 

for a system intercomparison. In July an intercomparison was run between 

Dobson Nos. 76, 65 , and 83 . 

Surface ozone concentrations were obtained using the Dasibi UV 

photometeric instrument. Calibrations were carried out weekly . 

6 
Surface Aerosol Measurements 

The G.E. CNC operated continuously with few maintenance or other probl ems 

except for the 5-day period, February 5 to 10 , when a valve shaft froze. The 

Pollak counter was operated in the normal manner during the year. Both the 

G.E. CNC and Pollak instruments were down during the eruption power outage, 

although a few observations were taken with the Pollak using auxiliary 

power. Because of the extensive volcanic plumes , those data are of 

questionable value. 

The nephelometer operated satisfactorily from January until June, except 

for the eruption period. In June, t he signal output became increasingly 

intermittent. Various repairs were made between June and September , but when 

totally satisfactory performance was not atta ined, the unit was returned to 

GMCC Boulder in October for complete rebuilding. 

Stratospheric Aerosols - Lidar 

Lidar observations were carried out , weather permitting , on approximately 

a weekly schedule. The total number of observations during the year totaled 

37 . The stratospheric aerosol l oading from the spring 1982 El Chichon 

eruption continued the decreasing trend established in 1983 with about a 50% 

decrease between the beginning and end of the year . There were apparently no 

new injections of volcanic aerosols into the stratosphere in 198~. 

The eruptions of the local island volcanoes, Mauna Loa and Kilauea, had 

no impact on the stratospheric aerosol burden because neither resulted in 

explosive eruption activity . The power outage resulting from the Mauna Loa 

eruption interrupted the lidar observations for abo ut 2 months, and during 

this time period the components were moved to Hilo for checking and 

maintenance. 

During the summer of 198~, work supported by an EPA grant was begun to 

upgrade the MLO lidar system. This upgrade will include new optical 

components, mounting configuration, and a data acquisition system. 

Met~orology 

Meteorological measurements were continued without major problems or 

significant change in instruments during 198~ . 

Solar Radiation 

The solar radiation program consists of several components : continuous 

solar measurements using both stationary and tracking instruments; discrete 

observations on a routine, weather-permitting basis; discrete manual, highprecision observations; and calibrations and intercomparisons of instruments 

using MLO faci l ities and instruments as working standards . All of these 

activities were carried out in 198~. The Mauna Loa eruption impacted on these 

measurements to some extent through the heavy fume production both during the 

actual eruption and for some period afterwards. Periods likely to be affected 

7 
by volcanic fumes were identified and data obtained during such periods were 

flagged for special consideration. 

A normal incidence pyrheliometer, four global pyranometers with Q, GG22, 

OG1, and RG8 cutoff filters, and a diffuse Q pyranometer with shading disk 

were operated throughout the year to obtain continuous radiation measurements. The GG22 pyranometer developed a problem with condensation on the 

inside of the dome in September. When local maintenance could not bring about 

a long-term correction, the sensor was returned to GMCC, Boulder, for 

mothball ing in January 1985 (at which time it was decided to discontinue 

measurements with the GG22). A filter-wheel pyrheliometer with Q, OG1, RG2, 

and RG8 cutoff filters wa s operated to obtain discrete broadband radiation 

measurements. Transmission general ly increased slightly as the year 

progressed. 

The active solar tracker and the 32-channel DAS operated the whole year 

with only minor problems in the automated solar dome. The dome and shutter 

controllers operated reasonably well, although there were some problems with 

the dome positioning motor and controller in June and again in August. 

Instruments mounted in the solar dome included a normal incidence 

pyrheliometer, an infrared water vapor meter, a seven-wavelength sunphotometer 

(retired from operation in January 1985), a three-wavelength PMOD 

sunphotometer, and an active cavity radiometer. Overall operation was fairly 

good during the year. 

Turbidity measurements were obtained with hand-held sunphotometers J321 

(380 and 500 nm) during the early part of the year before being replaced in 

April by instruments J202 (380 and 500 nm) and J314 (778 and 862 nm) for the 

rest of the year. These two sunphotometers were used at MLO during previous 

years and were returned to MLO after maintenance and calibration. 

Skylight polarization measurements were terminated in July when an 

equipment failure could not be remedied. Measurements to that date indicated 

a return to near background stratospheric aerosol conditions following the 

significant loading caused by El Chichon in March-April 1982. 

Precipitation Chemistry 

The GMCC precipitation chemistry program continued without difficulties 

at about the same level of activity as in prior years. The MLO program 

consists of the collection and analysis of precipitation collected at five 

local sites . MLO also carries out the analysis of precipitation samples 

collected on the Island of Kauai and at GMCC observatories BRW, SMO, and 

SPO. The analysis of snow samples from SPO and rain water samples from SMO 

were 1984 additions to the existing MLO laboratory schedule. Weekly samples 

are collected at both those GMCC sites. Several cooperative programs in 

precipitation and deposition augment the GMCC program . 

Cooperative Programs 

The large number of cooperative programs at MLO continued in normal 

operation through 1984. A brief summary of some of these activities follows 

with an emphasis on the more recent additions. 

8 
A ppogram of high precision UV radiati on measurements at 7 wavelengths 

(295-325 nm) was begun in August at MLO by the SRBL. These data are important 

in assessing the potential impact of changes in the ozone layer and add 

considerable detail to the erythema (sunburn) radiation data gathered at MLO 

for a number of years by Temple Uni versi ty. 

Precipitation collection for chemical analysis continued to be an 

important area of study. One new precipitation analysis program was the 

collection of samples for beryllium 7 and 10 analysis for the ISWS. 

Collections of precipitation for organic acid analysis at the University of 

Virginia continued as did sample collections for DOE and NADP. 

Aerosol particle samples were collected on a weekly schedule using 

Nuclepore filters for the University of Maryland and quartz filters for the 

University of Arizona. Both programs used a sampler-controller which was 

activated on the basis of time of day, wind speed and direction, and 

condensation nuclei concentration. Total particle filters were also collected 

for DOE using a wind direction discriminating sampler controller. The purpose 

of these sampler-controllers is to separate sample collections according to 

upslope and downslope air masses. Downslope air should be represen tative of 

mid-tropospheric conditions whil e upslope air masses may contain vari ous 

amounts of material with a recent origin at the earth's surface. High-volume 

sample data were also taken for EPA using standard EPA methods with one 2~-hr 

filter sample taken every 12 days. This EPA observational data series began 

in 1971 although there have been some significant breaks in the record. 

Total ozone and S02 in the atmosphere were measured for AES during the 

year with a Brewer MK I spectrophotometer. The CO analyzer of the Max Planck 

Institute , Mainz , Germany , was operated throughout the year, although there 

were a number of periods of downtime due to mechanical problems. 

The SIO Applied PhYSics infrared CO2 analyzer operated without major 

problems during 1984 in parallel with the GMCC CO 2 analyzer. Flask samples of 

air from MLO and Cape Kumukahi continued to be supplied to SIO on a weekday 

basis. 

Flask sample collections were made both at MLO and at the seacoast at 

Cape Kumukahi . Flask collections at MLO were begun in 198~ for the Australian 

CSIRO. This group is analyzing the MLO samples for the 13C/ 12C ratio as well 

as f or CO , CO 2 , and CH~ . Other continuing flask sample programs include those 

of t he OGC, NCAR , SIO. A new sampling program was begun at MLO in October 

198~ when Dr. B. Huebert, Colorado College, set up a sampler for nitric acid 

and hydrochloric acid vapors . Collections are made for 2-wk periods every 3 

months by Colorado College investigators. 

REFERENCES 

Lockwood, J . P. , N. G. Banks , T. T. English, L. P. Greenland , D. B. Jackson , 

D. J . Johnson , R. Y. koyanagi , K. A. McGee, A. T. Okamura , and J . M. 

Rhodes , 1985. The 198~ eruption of Mauna Loa Volcano, Hawaii, EOS , 

66 : 169-171. -

9 
2.2 Barrow 

FACILITIES 

Operation of the NARL facility was transferred from the USGS to UIC, a 

native corporation, on October 1, putting our long-term supply of electrical 

service in question. By the end of 198~, negotiations were under way with the 

Air Force to have the DEW line station supply our power . 

The Barrow GMCC Observatory was featured in a local newspaper article and 

on the front page of the Los Angeles Times in connecti6n with Arctic Haze. A 

reporter from National Geographic Magazine visited in November. 

Starting in August, personnel were on duty at the station 7 days per 

week. An IBM PC was used to demonstrate the feasibility of transferring data 

with Boulder over the FTS phone lines. The station photocopier was purchased, 

and the lease agreement terminated, with the purchase price equal to 11 months 

rent. 

The observatory was extensively renovated in August. All rooms were 

carpeted and painted , and instruments were rearranged in conjunction with the 

CAMS installation. The roof-top blowers were removed and outlets rewired in 

June. By October the sampling room ceiling and east wall were covered with 

sound-deadening acoustic tile and an outdoor walkway was built around the 

station and between the station and garage. The garage was insulated and a 

high BTU heater installed in February. 

The GMCC housing unit received a coating of exterior foam insulation in 

August which should prevent future ceiling water damage caused by freeze-out 

of interior water vapor. A problem with the tank water liner was solved and 

the pump repaired in December. 

In August, delivery was taken on a 1983 Dodge Crewcab truck from the GSA 

fleet in Anchorage. GSA also took over the GMCC Suburban and is now billed 

for the fuel and maintenance costs of these two vehicles. The blue GMC pickup 

had a new engine installed in May . The trucks performed well in 198~ with the 

usual number of minor repairs and flat tires . The Sidewi nder ATV continued to 

be troublesome and is to be excessed in 1985. A new freight sled was built 

and the Bombi tracked vehicle was renovated in December. 

PROGRAMS 

CAMS 

On August 7-16 the Barrow Observatory became the first in the GMCC chain 

to be changed over to CAMS operation. For the remainder of the year, except 

for two power outages , a 100% data acquisition uptime was experienced . 

Problems during this initial period have been few and minor in nature. 

Several software bugs have turned up. The boxes will infrequently autorestart , and the primary tape drive will occasionally develop a write error 

and switch to the backup drive. The performance of CAMS is far superior to 

the previous ICDAS system in terms of reliability and ease of operation and 

repair. 

10 
Carbon Dioxide 

The continuous analyzer system was completely replumbed in August. The 

ground air line was removed at this time. In November, a new chart recorder 

with felt-tipped pens replaced the aging , troublesome inked chart recorder. 

A new greaseless stopcock 3L flask was introd uced to the program i n 1984 

and will someday replace the 5L flasks. 

Surface Ozone 

Surface ozone data were collected without interr upti on except f or a 2-

week period in May when the Dasi bi ozone detector and ozone generat or were i n 

Boulder for calibration and service. 

Surface Aerosols 

The G.E. CNC operated intermittently , with several long 

operation . The unit flooded s ix times in 1984 and twice had 

caused the breaker to trip after several hours of operation. 

and Pollak counter continued to perform well. 

Solar Radiation 

periods of good 

a problem which 

The ne phelometer 

Early problems with poor noise rejection at the millivolt level by CAMS 

were overcome with the additi on of a pre-amplifier board in early 1985. In 

October , an HP71 based data ac quisition system was installed to replace an 

aging chart recorder. Th is system has performed well, yielding good 

measurements at millivolt signal levels with resolution down to microvolts . 

In December, infrared radiation measurements began with the install a t ion 

of two pyrgeometers. 

Meteorology 

During the first half of the year problems were experienced with the wi nd 

direction portion of the Aerovane. With the installation of CAMS , a new 

Aerovane, a pressure transducer, two aspirated thermocouples , and a dew point 

hygrometer were put online. An intermittent frosting problem occurred in the 

dew point hygrometer as winter temperatures approached and the unit qui t 

operation in December. All other meteorological instruments performed wel l. 

COOPERATIVE PROGRAMS 

The SRBL radi a tion monitoring program was discontinued on November 19. 

A new pump system was installed in January for DOE. 

For several months during the summer , a navigat i onal antenna was operated 

100 yards north of the station by Offshore Navigation, Inc . Our support 

included use of our road for access and a small amount of 110V electricity. 

The purpose of their operation was to fix the pOSition of oil exploration 

ships in the Arctic Ocean. 

11 
Table 3. Summary of Sampling Programs at BRW in 1984 

Program 

Gases 

CO; 

Sl,.rface ozone 

t~ et ha ne 

CFC-l1 , CFC-1 2 . and N20 

Aer0501 s 

Condensation Nuclei 

Optic~ l properties 

Solar Radiation 

Global irradi ance 

Direct irradi ance 

o i I'ect i rrad 1 ance 

T~rrestrial ( IR ) adi~ lo n 

T..Jrb i di ty 

Sky documentation 

Meteorology 

Air Temperature 

Dcwpoint temperature 

Pressure 

Wi nd (speed and direction) 

Pre c ipitatio n Chemistry 

pH 

Conductivity 

Coo perative Programs 

Total surface pa rti culat es (DOE) 

Aerosol chemistry (URI) 

Global radiation (SRL) 

Ultray~olet radiati on (Temple Vniv . ) 

CO 2 , C , tJ 20 (SIO) 

Precipitati on gauge ( ASeS) 

Ca r bonaceous particles (LBL) 

Vari ous tra c e gases (oce) 

M~gnetic fields (USGS) 

15C (USGS) 

V~ri o~s tra ce gases ( NCAR ) 

1jCl 1 C (CS IRO) 

Instrumen t 

URAS-2T infrared ana3

yzer 

O.5-L glass flasks P 

O. 5-L glass flasks, through analyzer 

5-L evacuated glass flasks 

3 -L evacuated glass flasks 

Dasi bi ozone meter 

O. 5- L glass flasks 

30D- mL stainless steel flasks 

Pollak CNC 

G. E. CtlC 

Four-wavelength nephelometer 

Eppley pyranometers with Q and RGB 

f i 1 ter's 

Tracking flI P 

Eppley pyr'hellometer with Q, aCl, 

RG2, and RGB filters 

Eppley pyrgeometer 

SIJnphotometers with 380- , 500- , 778- , 

and 862-nm narrowband fllt e rs 

All-sky camera (Fisheye ) 

Thermistor 

Max .-min . thermometers 

Dewpo I nt hYervmetor 

Capacitance transducer 

Ml crobarogr'aph 

Mercurial barometer 

Bend i x Aerovane 

pH meter (samples analyzed at MLO) 

Condu ctivity bridge (sampl es anal yzed 

at MLO) 

High-volume sampler 

Hi~h-volume sampler 

6 Eppley pyranometers 

Ultraviolet radi ome t er 

5-L evacua t ed glass flasks 

Wyoming shielded pr' ecipita ti on ga....:ge 

Dichotomous sampler 

(QiJartz and l-1illipor'e ri lters) 

H!eh-vol~me filter 

Daily Mil lipore sampler 

Stainless steel flasks 

Magnetometer 

10-L stainless stee l fl asks 

3-L stainless steel flasks 

5-L glass flasks 

12 

Sampling 

Frequency 

Cont i nl.lOUS 

1 pair wk- 1 

-1 I pair wk 

pair wk- l 

-1 

pa i r wk 

Can ti nuous 

1 pair wk - 1 

1 pa ir wk- 1 

Discrete 

Continuous 

Cant i nuous 

Continuous 

Conti nuous 

Discrete 

Contin uous 

Discrete 

Discrete 

Conti~~ous 

1 day 

Cont inu(lllS 

Continuous 

Cont i nuous 

Discrete 

Cant i m:ous 

Discrete 

2 mo- I 

Cont i nuous 

( I f i Iter wk - 1 ) 

Conti nuous 

(2 f ilters Wk- 1 ) 

Co nti nuous 

Continuous 

1 pair wk- I 

2 mo- I 

Continuous (I set 

of filters wk-') 

Conti nuous 

(1 filter wk- 1) 

Con ti nuous 

(I filt er da y -1 ) 

set wk- I ( 3 flasks 

set -I ) 

s ta tion check wk- I ) 

-1 

pa i r rno 

pair wk- 1 

pair mo- 1 
2.3 Samoa 

FACILITIES 

The Samoa GMCC facility gained a significant addition in late 1984 when a 

new remote sampling building was erected adjacent to the ridge sampling 

tower. The original OGe building , in place since July 1978, and the old 

prefab building left over from the 1981 SEAREX project , were removed to make 

room the new building. 

The new building is a prefabricated structure built by the EKTO Company . 

It arrived in late October and was assembled o n site. Steve Crawford fr om the 

OGe , assisted in removal of the old OGe building and erection of the EKTO. 

One feature of the EKTO is that it is large enough (16 ' x 20 ' ) to combine 

both GMCC and OGC operations under one roof . A partition separates the 

internal space into two rooms , with separate entrances , air conditioners , and 

electrical supplies . A separate entrance for the gas chromatograph 

compartment also ensures minimum disruption from pedestrian t r affic associated 

with other GMCC programs. 

A primary reason for purchasing the EKTO structure was its noncontaminating structural materials. Flask samples obtained from the interior 

of another EKTO structure in Samoa and analyzed by the OGe for evidence of 

room contamination , exhibited very low concentration of potential 

contaminants. Additionally the SEAREX EKTO building had weathered well in the 

Samoa climate . 

Data Acquisition 

During October 1984, the Samoa ICDAS system , in place since Observatory 

operations began in January 1976 , was taken offline for the last time and new 

CAMS boxes were installed to acquire data and control GMCC equipment . Ed 

Green was at Samoa to implement the changeover . The new system went online 

easily and operated trouble free through the end of the year. 

Samoa PV Sys tem 

The Samoa photovoltaic system "officially" went online 15 February 1984 

after final testing and certification by Gary Herbert. After instrumenting 

the arrays with temperature and three-component wind sensors , a final set of 

IV curves was obtained as part of the final acceptance procedure for the 

project . The system remained online for the rest of the year . 

Although the system installation had been completed in 1983 , problems 

with the inverter and array disconnect switch delayed startup unt i l early 

1984. In October , when installation of the SMO/GMCC CAMS units occurred , a 

specially modified CAMS unit was installed for controlling the PV system. The 

PV CAMS unit was designed to control the PV system battery charging 

operations. Evidence suggested adequate insulation levels were present to 

recharge the PV system storage batteries , but getting the energy into the 

13 
batteries from the arrays was not as efficient as necessary, and net daily 

losses of battery state of charge (SOC) became evident after initial system 

startup. The CAMS controller ~nit improved the efficiency of the daily 

recharging cycle. 

The battery storage system was sized to operate the PV load for 

approximately 2 days if clo~diness prevented an adequate daily charging 

cycle. A battery charger was designed into the system to automatically come 

online and charge the batteries using commercial power if the battery 

SOC/voltage decreased to a specified level . During 1984, the charger 

a~tomatically switched on only four or five times . Altho~gh the charger was 

too small t o actually increase SOC of the batteries , it could maintain system 

operation and prevent very deep discharge of the batteries until the solar 

energy source returned and a normal charging cycle could be restored . 

SAMOA LEASE RENEGOTIATION 

Samoa GMCC Observatory property is Samoan communal land leased from the 

Iuli family in Tula village. The original lease, signed in 1974 , sti pulates a 

renegotiation of the lease every 5 years. 

The first renegotiation was conducted in 1979 by N. H. Stiewig. A second 

renegotiation occlJ"red in 1984 and was conducted by Jim Hatkins , who 'Has with 

GMCC for a fe'H years in the early 1970's and 'Has extensively involved in the 

original Samoa GMCC lease arrangement and subsequent design and construction 

of the Observatory. He arrived in Samoa 29 February and departed 4 March . 

I·/hile on the island, meetings were held 'Hith the American Samoan Government 

officials and the negotiator for the Iuli family , Salanoa S . P. Aumoaualogo , a 

High Chief from Tula Village. A negotiator for the Iuli family 'Has necessary 

because a successor had not been chosen for Chief Iuli , Togi , who passed away 

suddenly in September 1983. High Chief Salanoa was suggested as the Iuli 

family negotiator and through his efforts and Jim Hatkins , a new 5-year 

agreement was reached, through the 15th year of the current 20- year lease . An 

option to renew for 20 additional years exists . 

PROGRAMS 

GMCC Programs 

The complement of GMCC programs at the Samoa Observatory remained 

unchanged during 1984 and are listed in table 1 . 

Cooperative Programs 

A CO2 flask sampling program for Dr . Graeme Pearman , CSIRO , was initiated 

in March . A once-per-month sampling schedule will be maintained for at least 

2 years. Its purpose is to gather data concerning the CO 2 cycle . 

1 4 
Table 4.--Summary of sampling programs at SMO in 1984 

Gases 

CO2 

Program 

Surrace oz'.me 

Total ozone 

Methane 

eFe-11 I CF"C - l 2. and N20 

Aerosols 

Condensation Nuclei 

Optlc11 propertIes 

Solar R"ldi aUon 

Gl obal lr '~diance 

o I reel i rrad I arlee 

Direct irradlance 

Tur bi d i ty 

Meteorol tJgy 

Al r Temperature 

Dewpolnt temperature 

Relative humIdity 

Pressure 

Wind (speed and directiun) 

Preclplt"ltlon 

PrecipItation Chemistry 

pH 

ConductIvity 

Cooperatl ve Programs 

13 CO 2 , C , 1/20 (SIO) 

ALE project: eFe- l l , CFC-12 , 

1/20 , CHjCCl" r.Cl 4 (oce) 

ALE project: CH~ . CO , CO2 (oce) 

V~rious trace gases (OOC) 

13C, 180 , CO 2 (CSIRO) 

I 3C (USGS) 

Wet-dry deposl tlon {t~ADP} 

BJlk deposition (EML) 

Hi -Vol s"lrnpler (EML) 

HI-Vol sampler (SEASPArl Project) 

lflstrument 

URAS-2T infral'ed anil~YZer 

O.5-L elass rlasks P 

O. 5-L g\'.:35 flasks , through anCllyzer 

5-L evacu~ted glass rl<'lsks 

DaslbJ ozone meter 

Dobson spectrophotometer no. ~2 

O.5-L glass flasks 

300-mL sta i nless steel flasks 

Pollak CNC 

C. E. CNC 

Four-wavelength nephelometer 

Eppl ey pyr'cHlometcrs wi til Q ~nd RGB 

filters 

Eppley PYI'anometers wi th Q 

filters on tIlted mounts 

Eppley pyrhellometer with 0 filter 

Eppley pYI'hel iomet.er wi th 0 , OGI , 

RG2 , nnd RG8 f II tel'!) 

Sunphotome t el's with 380- , 500-, 178- , 

and 862-nm OCH','owb'lnd f i 1 tel's 

Thermistor 

Max .-mln . thermometers 

HnWOt.tle'·mu~I·<1lJh 

Thermistor' 

Dewpol nt hygl'omet er 

Hygrotherm'Jgl'aph 

Sling psychrometer 

CapaCitance transducer 

1-11 cr'obaroeraph 

Mercurial barometer 

Bendi x Aer'OV3np. 

Polyethylene f...mnel , bottle 

CornIng model 125 meter with 

semimicr'o combination e l ectr'ode 

Beckman model RC-16C meter 

5-L evacu3terl elas~ flasks 

HP56'IOA ei1S chromatograph 

Car 1 e g~~l chromatograph 

Stnlnless steel flasks 

5- L glass flasks 

lQ-L stainless steel rlasks 

HASL wet-dry collector (new 

Chemetrics , Dec 81) 

Plastic: huck~t 

Hi-Vol pump ann filter 

Hi-Vol p'JlIIp arrd fi lter with clean 

--------

15 

Sampling 

Freq..Jency 

Cant I m:ous 

I paIr wk- 1 

I p;;ir wk- I 

I pair Wk- I 

Cant I nuous 

3 day-' 

p'llrwk- 1 

pair wk- I 

Dlscl'ete 

Continuous 

Continuous 

Continuous 

Cont.inuous 

Cont 1 nuous 

DIscrete 

Discrete 

Cant 1 nuous 

1 day-l 

Cont l ~yous 

I day 

Cont 1 nuous 

Continuous 

Discrete 

Conti n uous 

ContI nuous 

Discrete 

Cant 1 ~~ous 

I day 

day-I (GHCC); 

I wk- I (NADP) 

day-I (CHCC); 

wk- 1 (tIADP) 

-I 

pa \ r wk 

h3 h- 1 

set wk- I 

(3 flasks set-I) 

1 set mo- 1 

2 paIr mo- I 

Wk- I , wet; 

2mo- l , dry 

mo- I 

wk- I 

wk- I 
2.~ South Pole 

FACILITIES 

Amundsen-Scott South Pole Station is the most remote of the four GMCC 

Observatories. The South Pole station is situated at the south geographic 

pole on the polar plateau at an elevation of over 2, 835 meters. The average 

yearly temperature is -~9°C. Due to its unique environment and remoteness, 

South Pole station is only accessible during the Austral summer by aircraft 

from about 01 November until about 10 February. All resupply and replacement 

of personnel must be made during this period, with the possible excepti on of 

an air-drop in mid-winter (June). The station is isolated from the outside 

world from February through October. 

Consi deri ng the number of proj ects carr i ed out by the GMCC program, 

equipment performance was exceptional. Other than minor equipment failures, 

the problems were few, and remedied quickly. At year's end, all programs were 

online and operating properly with two exceptions . The NOAA GC was offline 

until new standard gas arri ved and albedo pyrgeometer was offline until a 

replacement dome arrived. Both programs were reinstated shortly after Pole 

openi ng. 

All GMCC and cooperative projects are located in the Clean Air Facility 

(CAF). Snow buildup around the CAF continues to be a major problem and a 

gr ow ing concern for GMCC programs. Stack icing, air intakes plugged with 

blowing snow, and direct line of sight for total ozone and solar observations 

are immediate problems, and many more will arise if the CAF is not raised in 

the near future. 

During March 198~ major improvements in distribution of station power 

reduced overall noise levels and virtually eliminated power brownouts. In 

early Mayall GMCC electronic instrumentation was integrated into the CAF 

isolation transformer. 

PROGRAMS 

Table 5 lists the sampling programs carried out during the 1983-8~ 

season. 

Gas Sampling 

The CO 2 program required a minimum number of repairs and/or modifications 

during the course of the year. The Dobson worked well all year and remained 

in calibration with no noticeable drift. Continuous surface ozone readings 

were taken with the Dasibi ozone monitor, and no major problems were 

encountered. The gas chromatograph and HP integrator worked flawlessly the 

entire year. 

16 
Table 5.--Summary of sampling programs at spa in 1984 

Program 

Surface ozone 

Tota} ozone 

Methane 

CFC-II I CFC-12, and N20 

Aerosols 

CondensatIon tluclei 

Optical properties 

Solar Radiation 

Global spectral lrradlance 

Turbidity 

Albedo 

Terrestrial (IR) radiatIon 

Total water vapor 

Meteorology 

Air Temperature 

Snow temperature 

PressW"e 

Wind speed/direction 

Cooperat i ve Programs 

CO2 , 13C • N20 (SID) 

Total surface partic~lates 

(DOE) 

Aerosol physical properites 

(SUNYA) 

Carbon aerosol (LBL) 

Various trace gases (DGC) 

PiC (NOAA/ARL 

Snow ael dl ty (NOAA/ARL) 

CH4' CO (NCAR) 

l-'1C/ 12C lIaOH samples 

(USGS) 

AtmospherIc Tracer EXp. 

(Los Alamos Nat. Lab,) 

Cosmic Dust Collection 

(Unlv, of Plttsbo,.lrgJ:ld 

Interhemispheric 'jel' c 

(CSIRO) 

Irl5trument 

URAS-2T Infrared analyzer 

0 . 5-L glass flasks p3 

0.5-L glass flasks , through analyzer 

Dastbl ozone meter 

Dobson spectrophotometer no. 80 

0.5-L glass flasks 

300-mL stainless steel flasks 

Gas chromatograph 

Pollak CNC 

G. E. eNC 

Four-wavelength nephelometer 

Eppley pyranometers with Q, CGI, and 

RG9 filters 

Eppley pyrheliometer with Q, OGI, RG2, 

and RG8 f 11 tel's 

S,mphotometers wi th 380-, 500-, 77B-, 

and B62-nm narrowband f 11 tel'S 

Eppley pyranometers with Q and RG8 

filters , downward-facing 

Eppley pyrgeometers, upward- and 

downward-facing 

Infrared solar hygrometer 

Platinum resIstor 

Platinum reSistor . 5 cm 

Capac! tance transducer 

Microbarograph 

MereU!' I al barometer 

BendIx Aerovane recorder 

5-L evacuated glass flasks 

HIgh-volume sampler 

Pollak CNC wIth diffusion battery 

Nuclepore filters 

HIgh-volume sampler 

Stainless steel flasks 

10-L stainless steel cylinder 

3,000 psi spheres 

125-mL Nalgene flasks 

Baseline gas chromatograph 

Alu'TIi nurn flasks 

Gas bubbler 

CH4 detector 

CosmIc dust collector 

Flasks 

17 

SamplIng 

Frequency 

Continuous 

1 pall' (2 wk)-l 

I pall' (2 wk)-I 

Conti~Vous 

3 day 

I pall' wk- 1 

pall' wk- I 

pall' Wk- I , summe~i 1 pall' 

mo • wI nter 

2 analyses/wk- I 

Discrete 

Continuous 

Continuous 

Continuous 

Discrete 

Discrete 

Conti nuous 

Conti nuous 

Discrete 

ContI nt,;ous 

Continuous 

Continuous 

Continuous 

2 times/day 

Continuous 

2 mo- 1 (3 flasks 

sample-I 

Continuous 

(I filter wk- l ) 

Discrete 

Discrete 

Continuo~l 

Twice mo 

(3 fl~lks 

set ) 

1 mo- 1 

(2 cylinders 

sample- 1 ) 

500 psI day-I 

Weekly 

Dally 

WeekI y 

20 days/month 

3-60 day 

per lods 

Continuous 

2 Flasks/month 

Length of Record 

Jan 74-present 

excl. Nov 18-

Nov 79) 

Jon Bt-present 

Nov 79-present 

Jan 76-present 

Dec 63-present 

1984 

Jan 17-Dec 19 

Jan BO-present 

Dec B3-present 

Jan 74-present 

Jan 74-present 

Jan 79-Dee 79; 

Jan Bl-present 

Feb 711-present 

Jan 77-present 

Jan 74-present 

Jan 82-present 

Har B3-present 

Summer 

Mar 77-present 

Apr B3-present 

Dec 75-present 

Feb BO-present 

Jan SO-present 

1957-present 

May 70- present 

Jan 711-present 

!lov B3-present 

Jan B2-present 

19BO-present 

Jan BI-present 

1972-present 

1982- present 

Apr B3-present 

Apr B3-present 

S~rr.er 83 to 

present 

Summer 83 

present 

SiJlTlmer 83 

present 

Summer 83 

present 
Surface Aerosols 

The Pollak performed extremely well this year and comparisons with the 

G. E. CNC were generally very good . The G. E. CNC also performed well for the 

entire year with the exception of two short problem periods. Hith small 

changes in concentrations it followed the Pollak closely; however , large 

variations in concentration caused the G. E. CNC to require recalibration . 

Solar Radiation 

Installation and data acquisition began in March f or the new IR upwardand downward-viewi ng pyr geometers . The replacement of the battery supply with 

DC power supply for both pyrgeometers reduced vo l tage variat i ons to less than 

0 . 001 V. 

With the exception of data gathered by the solar infrared hygrometer i n 

November and early December , the remainder of the solar rad i ati on equi pment 

performed very well . 

During the summer several major problems occurred to the nephelometer . 

In the last week of December one channel went to zero and all recovery 

techniques would not bring it back again . This was determined to be a short 

to ground caused by the multiplexer/digitizer signal input board . Repairs 

were completed at the end of January . 

,rom ,ebruary through May there were numerous memory losses for one of 

more channels for the nephelometer . The pr oblem was eventually diagnosed and 

the random memory crashes were eliminated. 

Meteorology 

In December a new meteorological tower was constructed 300 feet f r om t he 

CA, at grid 110 degrees , the southeast boundar y to the clean a i r sector . On 

18 January t he Bendix-,riez Aerovane was mounted on the new tower a t ~ feet , 

height of the trace gas stack intake. The addition of this and other 

meteorological instr uments was a joint project with A. Hogan of SUNYA to 

determine low level wind shear , vertical wind speed , and low level tem perature 

gradi ent . 

Between January 18 and 23 , Tom De,oor examined the temperature 

measurement system at the sPa . The spa a i r temperature measured approximat ely 

3°C cooler than the temperature measured at the s pa Heather Station. The 

sensor installation of t he two sensors was similar and could not account for 

the temper ature di f ferences. All el ectronic and sensor pr oblems wi th the GMCC 

equipment were repaired and adjustments were performed using a new DoC 

temperature source and the - 62 . 67°C sensor t est plug . As a result , good 

agreement between the two temperature channels was achi eved ; however , both 

channels now read appro ximately 2°C warmer than the official temperature at 

the stati on meteorological off ice . 

18 
ICDAS 

No problems were encountered with the minicomputer, voltage regulator, 

tape drive, or clock. At the beginning of the year an input board on the MUX 

shorted and caused the loss of one channel of data input from the 

nephelometer, and several problems existed with the teletype. 

During the course of the year , frequency variations due to large 

electrical power requirements during welding caused over 30 ICDAS crashes. 

After transfer of the ICDAS system to an isolated power transformer, the ICDAS 

system wa s less susceptible to crashes; however , this was not always the 

case . Any time welding operations occurred , ICDAS and electronic 

i nstrumentation had to be checked. 

COOPERATIVE PROGRAMS 

The majority of the cooperative sampling programs listed in table 5 

experienced no major difficulties during the course of the year. 

In December , two Gill Aerovanes were installed on the new met tower at 13 

and 84 feet . Unfortunately , however , numerous problems were experienced 

throughout the year with the 84-foot Aerovane. 

The NCAR gas chromatogr aph and its supporting systems experienced several 

problems during the year. When the station opened , the 5 volt regulator was 

faulty and w~s replaced . Carbon monoxide could not be analyzed because the 

instrument was not sensitive enough . In February , the flame ionization 

detector failed because the collector connecti on was corroded. The repair 

lasted one month and fai l ed again . A second attempt to repair the same 

problem failed. A new flame ionizati on detector was received on the midwinter airdrop, and after i nstallation , the gas chromatograph was back on 

l ine . 

1 9 
3. AEROSOLS AND RADIATION GROUP 

3.1 Continuing Programs 

SURFACE AEROSOLS 

The GMCC aerosol monitoring program continued during 1984 as in previous 

years. Condensation nucleus (CN) concentration and aerosol scattering extinction coefficient (asp) were measured continuously at BRW , MLO, SMO , and SPO. 

A G.E . automatic CNC operates continuously and a Pollak CNC provides da ily 

calibration pOints at each station. A four-wavelength nephelometer at each 

station continuously measures asp at 450-, 550-, 700- , and 850-nm wavelengths. 

Figure 1 shows daily geometric means of asp and CN concentration at the 

GMCC stations for 1984. Angstrom exponents calculated from the fourwavelength light scattering data are shown in the upper portions of the 

graphs. Only CN concentrations are shown for MLO because of major problems 

with the MLO four-wavelength nephelometer during 1984. Monthly geometric 

means of the entire data record for each station are shown in fig. 2. Monthly 

geometric means for 1984 for BRW , MLO , SMO, and SPO are tabulated in table 

1. Monthly geometric means for 1983 for MLO are also included in table 1 

because they were omitted from the GMCC annual report for 1983. 

The BRW data in fig. 1 show elevated asp values in excess of 10-5 m- 1 in 

the springtime, typical of the well-known Arctic Haze . This regular annual 

cycle is apparent ~n t~e BRW long-term record shown_in ~ig . 2 with monthly 

means exceeding 10 5 m 1 in the spring and below 10 b m 1 in the summer. The 

BRW CN record shows a more variable semiannual cycle with maxima usually 

occurring in March and August, and minima usually occurring in June and 

November. 

The MLO CN data shown in fig. 1 are typical for Mauna Loa and are most 

likely representative of the background troposphere for this region of the 

atmosphere. The long-term record of as in fig. 2 shows an annual cycle with 

a maximum in April-May which is caused gy the long-range transport of Asian 

desert dust in the upper troposphere to the vicinity of Hawaii. 

The SMO asp and CN data continue as in previous years with no significant 

annual cycle or long-term trend . Bodhaine and DeLuisi (1985) presented a 

detailed analysis of the Samoa data set. 

The SPO CN data show a strong annual cycle with a maximum greater than 

100 cm- 3 in the austral summer and a minimum of about 10 cm- 3 in the winter. 

The asp data show a cycle dominated by events in the austral winter. These 

events are caused by the transport of seasalt in the upper troposphere from 

stormy regions near the coast to the interior of the continent. An analysis 

of the SPO data set and case studies of the winter seasalt events were presented by Bodhaine et al. (1986). 

20 
AlROOOI. DATA roR BARROW 

JAN rrlI WAR APR WAY JUN JUI. AUe SIP OCT NOV DEC 

-I, 44¥f:'I-JI~1 1M~1 J dl 

i 

. !\ [0 A l d. I ~I 

<-

~ .. <. 

"':;;:' . ,", .:r-i/ ~~. IIAi '\ 'M .. ~ ~ 1\ I' 

, ,IH I' 

, 

II I ~,l\ , ,~I 

)~ J(' I~ I~~ ~ ,~ \ 1~'Vi \ IA 1 ~MJ • ~ II 

-

T 

T 

, 

, 

i 

~I 

, 

, 

, 

-

..l- · 

-

UROSOL DAtA R WA LOA 

.aN n:B WAR APR WAY JUlI' JUL AUC S!P OCT NOV DD: 

~i l I I I I I I I I ~,I \J 

r, , 

,fr, ,11JJJ [.W ~ l~.LI ~V 114 iJ1 N'. l,f'lI1l 

fiT 

~~--=-=-~=-- -~~-~_M_m= __ 

I 

, 

, 

L___ -------',""-.---------- .-------__ 'IlO"""----________ .J 

<-

~: <. 

i '. ~T 

• 

.s, 

, 

.sAEROSOL DATA FOR SAIo40A 

JAN rEB IolAR APR WAY JUN SVL AUe SO' OCT NOV DEC 

11.- l&tLJ~ J~L~~I J 

, 

T 

.1 • •• JIM. ~ ~ f; .M .M! 1\1. JI' .~ III I'" -, T 

, 

\V ~ ~ 1'Ifr r'tt- I lJ W 1.1\ V' :V .r\ ft· '""'" I 

JAN f1lI WAR APR WAY JUN JlJl. AUG SEP OCT NOV DEC 

AEROSOl. DATA FOR 9)UTH POU: 

.-

=- • ~-'. 

T 

, 

SAN n:u IU.R APR },(AY )UN JVL AUG SI;P ocr NO\' DEC 

"I ~~ ,ILl " I ' ~~~:;~&j' ~~I , 

E 

~, 

• 

.s • -.~ \ 

I~ J 1 II{ b ki d "~ ~ -' iJ .' :~ .... v 

, 

, , i .. ,- ~'. .~ " 

, 

, 

§-

z 

.3-

A J u'" ",,11 II/ 

Ii' Mt ~ J" 

""'" JAN Ym WAR APR WAY JUN IUL AUG S1'P OCT !iOV DOC 

Figure 1.--Daily geometric means of asp and eN data at BRW. SMO , and SPO , and 

eN data at MLO for 198~. For each station , eN concentration lower is shown as 

a solid line. asp data (middle) are shown for ~50 (do tted), 550 (sOlid) , 700 

(dashed), and 850 nm (long-dashed) . Angstrom exponents (upper) were 

calculated from ~50- and 550 -nm (dotted) , 550- and 700-nm (solid), and 700-

and 850 -nm (dashed) asp data . 

21 
Mauna loa , 

I~ • If, i' iM I IA 

-\ t\t fL\- ."\ -" -\ l ~ 

E 6 b~ 

3 - 3 7 

5 

5 

~\ 

~ n 77 n ~ ~ ~ ~ ~ ~ 

Yur 

$omoo 

Jlmm±p n 77 n ~ ~ ~ ~ ~ M 

Year 

. 

3 2 

t- ." IA VI ..jc -'" "'" -"'\ ~ vv 

7475767778 798)8182 83 6-l 

Yur 

75 76 77 78 19 80 81 Yur 82 83 84 

Figure 2 .--Monthly geometric means of asp and CN data for the entire 

data record, as in fig . 1. The straight dashed lines are leastsquares linear trend lines . 

SOLAR AND THERMAL RADIATION 

Direct and global broadband solar radiation monitoring at the four basel in e observatories continued throughout 1984. The measurement programs which 

make up the basic solar radiation program at all four sites are given in table 

2. 

Certain additional radiation monitoring projects are carried out at the 

GMCC obser vatories . Table 3 lists the additional radiation measurements at 

each observatory. 

All data acquired from projects listed in tables 2 and 3 are either 

routinely edited and archived or made ava ilable on request if feasible. The 

GMCC ARM staff processes, interprets, and publishes the data as applicable to 

present research interests, some of which are discussed later. 

As in previous years , the GMCC traveling standard pyranometer and 

pyrheliometer were operated for a peri od of several to many days, side-byside, with station instruments at each station. The traveling standards are 

calibrated on a yearly basis at the NOAA Solar Radiation Calibration Facility 

in Boulder. Data quality assurance checks are performed daily by observatory 

personnel. Starting in 1985, daily comparisons of measured broadband solar 

data and clear sky model calculations will be made at each observatory . A 

comparison of the clear-sky model performance versus the historical GMCC solar 

data base is given later in this report . 

22 
Table 1.--Monthly geometric means of eN concentration (cm- 3) and asp 

(m- 1) at 450, 550 , 700, and 850 nm for MLO during 1983 and for 

BRH, MLO, SMO, and SPO during 1984. 

BRW 198~ 

Gil 

'5p(~5D) 

'sp(550) 

'5;>(700) 

'sp(850) 

MLO 1983 

GN 

'sp(~50) 

'sp(550) 

'sp (700) 

'sp(850) 

MLO 1984 

Gil 

°sp(li 50) 

°sp(550) 

'sp(700) 

'sp(850) 

SMO 198~ 

Gil 

'sp(~50) 

'sp(550) 

'sp (700) 

'sp(850) 

SPO 198~ 

GN 

'sp(~50) 

'sp (550) 

'sp (700) 

'sp(850) 

Jan reb Mar Apr I~ay Jun Ju\ Aug Sep Oct Nov Dec 

398 952 673 '101 ~56 273 776 761 139 156 70 173 

1.89-5 1.57-5 1.86-5 1.61-5 

1.76-5 1.40-5 1.65-5 1.~~-5 

1.24-59.20-61 . 10-59 . 87-6 

9.22-6 6.51-6 8 .01 -6 7.30-6 

1.23-5 2 . 76-6 2 . 21 - 6 2.43-6 3 .59-6 6.52-6 5.~3-6 1.60-5 

1.03-5 2.1~-6 1 8~-6 2. 12-6 3.1~-6 5.73-6 .71-6 1.50-5 

6 . 39-6 1.26-6 1.26-61.61-62.29-63.97-63.25-6 1.09-5 

~.~~-6 9.45-7 9.25-7 1. 25-6 1.75-6 2.99-6 2.39-6 8.36-6 

251 338 

1.56-6 1.06-6 

1.18-67.97-7 

9.99-7 6.58-7 

5.95-7 3.71-7 

152 

8 .92-7 

7.93-7 

6.96-7 

~ .14-7 

201 

1.59-6 

1.35-6 

1.17-6 

8 . 66-7 

292 272 

1.37-59.61-6 

1.27-5 8.53-6 

1.25-5 7.82-6 

1.28-57 . 87-6 

117 

6.34-7 

~.09-7 

2 . 30-7 

1.39-7 

111 

6 .00-7 

3.89-7 

2.2~-7 

1. 63-7 

283 3~2 334 308 3~3 375 ~51 318 

4.81-7 

3.17 -7 

2.28-7 

1 • 5~-7 

2.12-6 ~.3~-6 1 .64-6 

1.75-63.52-6 1.37-6 

1.35-62.92-61.16-6 

9.53-72.19-69 . 13-7 

1 .54- 6 9 . ~ 3-7 

1.3~-6 8 . 82-7 

1.27-68 . 87-7 

1.10-6 5 .5 !1-7 

6.~0-7 8 .73-7 

5 . 07-7 6 .55-7 

57-7 5.35-7 

3.03-7 3.65-7 

187 

3.13-6 

2 . 70-6 

2 . 11-6 

1 .5~-6 

82 

2~8 211 

1 0~ -5 1 .0~-5 

1.01-5 9.~5-6 

1 .02-5 9 . 00-6 

1.09-5 9.33-6 

320 193 

175 177 

1 . !j 1-5 1 . 72-5 

1. ~1-5 1.76-5 

1.50-5 1 . 91-5 

1.65-5 2 . 11-5 

126 

6.69-7 

4. 55-7 

2 . 73-7 

2.18 - 7 

43 25 18 

3 . 36-7 

2.77-7 

1.75-7 

1.14-7 

~0-7 1.89-7 

1.8'-7 1 . 62-7 

I . 1 2-7 9.76-8 

7.60-86.76-8 

317 

22' 

1 .~ 1-5 

1 • ~2-5 

1 .52-5 

1.67-5 

276 

282 

1.57-5 

1 . 5 11-5 

1.60-5 

1.71-5 

235 

29~ 

1.53-5 

1. '7-5 

1 . ~5-5 

1. ~7-5 

238 

1 . 59-5 

1.55-5 

1.57-5 

1.6'-5 

14 18 43 116 

3.38- 7 '.27-7 4.75-79.00-7 

2 .81-73.65-73 . 69-77 . 27-7 

1 . 80-72.38-7 2 . 59-7 ~.99-7 

1 .1~ 7 1.70-7 1 7~-7 3.73-7 

19~ 179 

1.19-7 ~7-7 

9 . 15-81.86-7 

7 .03-8 1 . '0-7 

5.02-8 1.06-7 

212 

235 

1.25-5 

1.20-5 

1 . 20-5 

1. 2~-5 

138 

4.82-7 

3.~9-7 

2 .02-7 

1. 43-7 

150 

192 

1.75-5 

1.79-5 

1.85-5 

2.13-5 

III 

3.39-7 

2.37-7 

1.39-7 

7.52-8 

A compact exponential format is used for such that 1 .89-5 ~ 1.89 x 10- 5 , 

All observatory programs remained basically unchanged during 1984 with 

the following exceptions. 

In September a new albedo instrument support rack was installed at the 

South Pole. This greatly improved leveling capability of the mounted instruments. Leveling of the albedo instruments is critical during times that they 

are faced up for comparison with the fixed upward-facing pyranometer and 

pyrgeometer . It is believed that the new albedo rack is too low to obtain a 

representative reflectance from the snow surface . Plans are to raise the 

reflectance measurement height to about 10 feet in 1985. 

An experimental pyranometer designed to prevent the deterioration of the 

RC8 filter dome in tropical environments was taken offline at Samoa after it 

was determined that it produced erroneous results. A protective clear dome 

intended to protect the Rc8 glass led to overheating of the instrument . 

23 
In late 1984 the GMCC field data acquisition system, ICDAS, was replaced 

by the new CAMS. Conversion to CAMS and the preamplifiers was completed by 

early 1985. 

Table 2.--GMCC basic radiation monitoring measurements 

Instrument 

Tracking pyrheliometer 

Pyranometer (Quartz) 

pyranometer (RG8) 

Filter wheel pyrheliometer 

OGl 

RG2 

RG8 

Spectral sun photometer 

Quanti ty 

Measured 

Direct solar 

Global sky 

Global sky 

Direct solar 

Direct solar 

Direct solar 

Direct solar 

aerosol optical 

depth 

Havelength 

0.28-3 . 0 ~m 

0 . 28-3 . 0 ~m 

0.695-3.0 ~m 

0. 28-3. 0 ~m 

0 . 530-3.0 ~m 

0.63-3.0 ~m 

0.695-3 . 0 ~m 

380 , 500, 778 

862 nm 

Table 3.--GMCC radiation measurements specific to individual observatories 

Location 

South Pole 

Mauna Loa 

Barrow 

Instrument 

RG8 tracking pyrheliometer 

pyrgeometer 

Inverted pyrgeometer 

Inverted pyranometer 

Shaded pyranometer 

Solar IR hygrometer 

Solar IR hygrometer 

Absolute cavity 

PMOD/GMCC sun photometer 

OGl pyranometer 

Pyrgeometer 

Inverted pyrgeometer 

Inverted pyranometer 

RADIATION CLIMATOLOGY AND MODEL COMPARISON 

Quantity 

Measured 

Direct sun 

Sky infrared 

Surface infrared 

Surface reflected 

Diffuse sky 

Precipi table H20 

Precipitable H20 

Direct solar 

Continuous aerosol 

Optical depth 

Global sky 

Sky inf rared 

Surface i nfrared 

Surface reflected 

Ha velength 

0.695-3 . 0 ~m 

4. 0- 5 . 0 ~m 

4.0-50. ~m 

0. 28-3 . 0 ~m 

0.28-3.0 ~m 

1.06, 1.13 ~m 

0 . 88 , 0 . 94 ~m 

All 

380 , 500 , 

778 nm 

0.530-3 . 0 ~m 

4. 0-50 . 11m 

4.0-50. 11m 

0.28-3.0 ~m 

A computationally efficient physical mathemat i cal model for direct and 

global solar flux in the atmosphere developed by Bird (1982) was adapted to 

model solar flux at the four GMCC observatories. The model calculates direct 

and global solar flux as a function of location, elevation , time, precipitable 

24 
water vapor, total ozone , aerosol scattering and absorption, surface albedo, 

and extraterrestrial flux. Computed daily flux totals for an entire year were 

compared to 8 years of observed daily total global flux for each GMCC site. 

The 8 years of data used are for 1977 through 1983, edited for unacceptable 

data, and archived at NCDC as hourly integrals as described by Dutton et al. 

(1985) (fig. 3). Only days where the edited record is complete between 

sunrise and sunset are used. The observations are from continuous measurements (1 per second) during all sky conditions. The atmospheric constituent 

climatology used in the model for each observatory, was compiled as a monthly 

average of observations of precipitable water, total ozone and spectral 

aerosol optical depth. Aerosol absorption was held fixed at .02, and surface 

albedo was determined appropriate for each station. The extraterrestrial flux 

was set at 1368 W/M 2 , but adjusted for the earth's orbit. Figure 3 shows 

daily totals of extraterrestrial, modeled, and observed global solar flux for 

each GMCC observatory. 

BRW DAILY RADIANT EXPOSURE 

~~r-------------------------------' 

e~~~~~~~~~~ Ii 7 10 II 12 

MONTH 

SPD DAILY RRDIANT EXPOSURE 

L-_____________________ __ 

MLO DAILY RADIANT EXPOSURE 

~~, , --------------------------------

.'-. , 

. . -.-." 

·· •. c·· 

" .. ". "':" -., .. :,<:.~·f .. -><?!11: 

Ii I )0 11 U 

I10NTH 

SMO DAILY RADIANT EXPOSURE 

~~r-----------------------------__; 

e ~ ~"r--_ 

f ~ :: :d':y ;, .,,: ,.<'7~~f~;H::~<J ~..; 

< 

0 

~"! 

! 0 

~ 

. 

. 

··· ·::;,~:·?j;.:~-\::t:~·- " 

. , "'NTH 10 11 12 

Figure 3.--Plot of daily totals of solar radiant exposure on a horizontal 

surface for each observatory. Uppermost smooth curve is the extraterrestrial 

value, the scattered pOints are observed values for 1976-1983 , and solid line 

near the upper limit of the observation is the modeled clear-sky value using 

the Bird model described in the text . 

25 
Since the observed values in fig . 3 contain the influence of clouds , but 

the modeled values do not , the model represents only completely clear days or 

the upper limit of the observed data . Considering the good agreement between 

the modeled and the observed data , it is important to point out that there was 

no tuning or other connection between the two except for the absolute 

calibration reference of the observed data and the calibration of the 

extraterrestrial value used in the model . 

Present and future work comparing the solar model to GMCC data will 

include refinement of radiati vely active constituent climatologies , exami -

nation of annual and anomalous variability in the data , examination of direct 

and diffuse components , and developi~g cloud climatologies. 

SOUTH POLE ALBEDO 

Starting in late January 1982 , continuous measurement of the surface 

albedo has been made by GMCC at the South Pole . During this period , se veral 

adjustments have been made to the measurement apparatus, but the general 

measurement strategy remains the same . One Eppley global pyranometer faces up 

and the other with the same filter faces down wi th occasional periods when 

both are faced up when the calibration of one is normalized to the other. 

Measurements were originally made with three spectral filters , OG1, RG8 , and 

Quartz , but since 1983 with only two, RG8 and Quartz. Initial results show a 

daily average quartz albedo of 0 . 93 for overcast conditions to 0 . 82 for clearsky conditions. 

LIDAR 

The historical lidar data record that began in the fall of 1974 at MLO 

has been analyzed for certain climatological features. With the exception of 

fig . 4, all figures shown i n this section have been smoothed . Figure 4 shows 

I~ 

IO ~ 

YERR 

Figure 4.--0ptical th i ckness (. = 694 nm) vs time of stratospheri c 

aerosols at Mauna Loa observed by lidar . 

26 
a plot of· lidar optical thickness vs time. The beginning of the plot shows 

the decaying stratospheric aerosol from De Fuego that erupted 14 October 

1974 . Foll owing De Fuego , a rather quiescent period ensued until the Mystery 

Cloud was observed in January 1982, followed by the immense signal from El 

Chichon which erupted in March and April 1982. Observations during the 

quiescent period implied a lower threshold value of 0.002 optical thi c kness 

for stratospheric aerosol. Interestingly , during the years 1

f

77-1980, annua l 

stratospheric aerosol loading profiles (optical thickness km- ) showed no 

maximum near 20 km. 

Figure 5 shows the altitude of the peak scattering ratio , i . e . one plus 

the backscattering mixing ratio of aerosols to gas , for the entire lidar 

record. Of note here are the low maximum-backscattering altitudes of De 

Fuego , some other volcanic activity not widely separated in time viz., St. 

Helens (18 May 1980) , Ulawun (7 October 1980), Alaid (27 April 1981), Pagan 

(15 May 1981) , and Mystery Cloud (early Jam:ary 1982). EI Chichon stands out 

strikingly , reaching a peak altitude of 27 km . 

~ 

• a:: . 

If') 

>< 

a: 

::E: 

N 

28 

27 

26 

2S 

24 

23 

22 

21 

20 

19 

18 

177,\ 75 T1 7B 79 00 81 82 

YEAR 

Figure 5 .--Altitude of the peak scattering ratio (Rayleigh + 

Aerosol)/Rayleigh vs time, observed by lidar at Mauna Loa . 

Figure 6 shows the altitude of the median optical mass. Interestingly, 

the mystery cloud median optical mass was the lowest and the El Chichon cloud 

was very high. 

Figure 7 shows the 2/3 width of optical mass centered at 1/6 above and 

1/6 below the entire lidar optical mass profile . Note the thin layering of 

the t wo most significant stratospheric clouds De Fuego and El Chichon during 

the earliest stages of these events . Note also , the broad layering during the 

quiescent period. 

27 
~ 

" ~ 

ac 

~ 

~ 

;C 

~ 

0 

>-< 

~ 

I 

~ 

27 

~ 

~ 

24 

23 

22 

21 

m 

19 

18 

17~ ~ ~ TI n ~ ~ 81 82 83 

7.5 

7.0 

6.5 

6. 0 

5.5 

5.0 

4.5 

4.0 

3.5 

3.0 

YEAR 

Figure 6.--Altitude of the median optical mass of stratospheric 

aerosol profile (km- l ) observed by lidar at Mauna Loa. 

~~ ~ ~ TI n ~ ~ 81 82 W ~ 

YEAR 

Figure 7.--The 2/3 central wi dth of optical mass of stratospheric aerosol profile (km- l ) observed by lidar at Mauna Loa. 

Table 4 shows exponential diminut ion rate constants for volcanic clouds 

over Mauna Loa. The reciprocal of the constant T* represents the time for a 

volcanic cloud to diminish to lie of its optical thickness . Data sources are 

ei ther the Mauna Loa transmission obser vati ons or lidar obser vatio ns. Note, 

that as a cloud ages, its diminution rate gets smaller. 

28 
Table 4.--Diminution rate (exponential) constant for volcanic clouds 

over Mauna Loa 

Years Volcano T*(yr l ) Source 

1965-1966 Agung 1 .0 Trans 

1965-1969 Agung 0.5 Trans 

1975-1976.5 DeFuego 0.91 Lidar 

1982 (Apr-Dec) El Chichon 1.70 Lidar 

1983 El Chi chon 0 . 78 Lidar 

1984 El Chi chon 0. 55 Lidar 

1982-1984 El Chichon 1 .04 Lidar 

3.2 References 

Bodhaine , B. A., and J. J. DeLuisi , 1985. An aerosol climatology of Samoa . 

J . Atmos. C_hem ., in press . 

Bodhaine, B. A., J. J. DeLuisi, J. M. Harris, P. Houmere, and S. Bauman , 

1986 . Transport of chemical species to the South Pole. Tellus , in press. 

DeLuisi , J., T. DeFoor , K. Coulson , F. Fernald , and K. Thorn , 1984: Lidar 

observations of stratospheric aerosol over Mauna Loa Observatory : 1974-

1981 . NOAA Data Report, ERL ARL-4 , NOAA Environmental Research 

Laboratories, Boulder, CO , 107 pp. 

DeLuisi, J., T. DeFoor, K. Coulson , F. Fernald , and K. Thorne, 1985: Lidar 

observations of stratospheric aerosol over Mauna Loa Observatory: 1982-

1983. NOAA Data Report, ERL ARL-5, NOAA Environmental Research 

Laboratories, Boulder, CO , 78 pp. 

Harris, J. M. and E. C. Nickerson (ed) , 1984: Geophysical Monitoring for 

Climatic Change No. 12, Summary Report 1983 , Environmental Res. Labs , 

Boulder , CO , 184 pp. 

Wagner, A. J., 1985: The climate of spring 1984 - An unusually cold and stormy 

season over much of the United States, Monthly Weather Review, 113, No . 1, 

Jan. 1985 , 149-169 . 

29 
4. CARBON DIOXIDE GROUP 

4.1 Continuing Programs 

CONTINUOUS ANALYZERS 

Continuous CO 2 measurements by in situ NDIR analyzers at the four GMCC 

stations (BRI<, MLO , SMO , SPO) continued in 1984. May 1984 marked the 10th 

anniversary of measurements by GMCC at MLO. The complete record of 

provisional monthly mean data for the continuous analyzers is presented in 

fig. 1 and in table 1. The eruption of the Mauna Loa volcano in late March 

resulted in over a month ' s loss of data. There has also been a significant 

increase in CO2 variability at MLO since the eruption due to outgassing by the 

volcano. The mean year-to-year difference from 1983 to 1984 for the four 

stations was 1.55 ppm (using an interpolated value of 346.3 ppm for April at 

MLO) , which is slightly higher than the mean CO 2 global growth rat e of 1. 5 

ppm/yr since 1976 , and is due to an anomalously high difference of 1. 9 ppm for 

BRI< between 1983 and 1984. 

Data acquisition procedures remained the same for most of 1984 , until the 

new CAMS data acquisition units were installed . The changeover f r om ICDAS to 

CAMS occurred in August at BRI< , in October at SMO, and in November at MLO and 

SPO. Some changes in data processing with CAMS occurred , which include 

computing hourly means by compensating for any changes in drift and 

sensitivity of the NDIR analyzer , and by calibrating the working standard 

gases at weekly intervals using a non-linear method discussed by Komhyr et al. 

(1985). A description of the CAMS design and of the CO 2 CAMS operation can be 

fOund in GMCC Summary Report No. 12 (Harris , 1984, pp . 69-72) . 

The in-house calibration of CO2- in-air reference gases for GMCC continued 

in 1984. Two-hundred fOurteen tanks were calibrated during the year. All 

calibrations are traceable to the GMCC secondary standards whi ch have been 

calibrated manometrically and by NDIR measurements by C. D. Keeling at SIO . 

;: 

"-"-

N 

0 

u 

m 

'" 

m 

'" 

m 

'" 

m 

,," 

",0 

SHO 

SPO 

\1 

no 'c''''''"''~:;;''''''-"-;-;''''''';-'-;;'''''''~'';-;'-;-' "',;-;,,:;c, "',,,,,,;;;:,-'c,:;c,,:;;,~,;;;:,,;;:,-,-;-:,,;;:,,c-'c:,,:;c,,~,,;;;: .. '" 

YEAR 

30 

Figure l--Provisional selected 

monthly mean CO 2 concentrations from 

continuous measurements at BRI<, MLO , 

SMO and SPO . Values are in ppm wi th 

respect to dry air (x81 mole 

fraction scale). 
Table 1.--Provisional selected monthly and annual mean CO 2 concentrations 

(ppm relative to dry ai r-X81 mole fraction scale) for continuous 

measurements at BRl-I , MLO , SMO and SPO. 

Year Jan Feb Mar Apr May Jun Jul Aug Sep Oct Nov Dec Annual 

mean 

BRW 

1973 322 . 0 323 . 4 327.8 332.7 333.5 

1974 336 .5 336 . 0 336. 7 337.1 336 . 9 335.9 328 . 7 323.5 324.2 328 . 8 332 . 0 335 . 2 332 . 6 

1975 336 . 8 336 .6 337. 1 337.7 337 . 9 335.4 330.1 324 . 4 324 . 6 329.2 334 . 3 336.5 333 . 4 

1976 337 .0 336.7 337 . 7 338 . 0 337 . 8 336. 8 331 .0 323 . 5 325.1 329.8 334 .1 336 . 6 333 . 7 

1977 336 .8 336.9 338 . 2 339 . 2 339 . 4 337 . 7 330.1 325 . 4 326.8 332 . 0 334 . 7 338.8 334 . 7 

1978 339 .1 340.2 341.5 341 . 0 340.8 339 . 4 332 . 6 327.7 327.4 332 .1 338 . 8 339.4 336 . 7 

1979 340 .1 34 1. 3 342 .5 342.4 342 . 9 342 . 0 333 . 6 327.7 329 . 3 333 . 1 338.1 341.5 337. 9 

1980 34 1. 9 342.4 343.4 343 . 3 343 . 3 342.6 337 . 3 331 . 8 331.4 337 . 9 340. 5 342 . 6 339 . 9 

1981 344.3 345 . 5 344 . 6 345 . 8 346 . 8 344 . 4 338 . 2 331 . 8 333 . 3 338.8 342.2 344 . 9 341 . 7 

1982 345. 8 347.2 348.3 348 . 4 348 . 0 345.7 339 .2 333.2 333 .2 337. 9 342 .1 344 . 5 342 . 8 

1983 347 . 5 347 . 0 348.1 3'18 .1 348.3 347 .0 340 . 4 333 . 8 335 . 5 340 . 6 346 . 5 346 . 8 344.1 

1984 351.0 350 .7 350 . 0 349.8 350 .7 348 . 3 341 . 3 335. 9 338 .3 342.2 345.0 348 . 5 346.0 

MLO 

1973 

1974 333 .1 332 .1 331 .1 329 . 1 327 .4 327 . 3 328 .2 329 . 6 

1975 330.6 331.4 331. 9 333.2 333 . 9 333 . 4 331 . 9 330.0 328 .5 328 . 4 329 . 2 331. 0 331 .1 

1976 331 .6 332.6 333 . 6 334 . 7 334 . 7 334 .2 333 .0 330. 8 329 . 0 328.6 330 . 2 331 . 6 332 . 0 

1977 332 .7 333.2 334 .9 336. 1 336 . 8 336.1 334.8 332 . 6 331. 3 331 . 2 332.4 333 . 5 333 . 8 

1978 334 . 7 335 .2 336 . 5 337.8 338.0 338 . 0 336 .4 334 . 5 332.5 332.3 333.8 334 . 8 335.4 

1979 336 . 0 336 . 6 337 .9 339 . 0 339.1 339 . 3 337 . 6 335 . 7 333 . 8 334.1 335 . 3 336.8 336 . 8 

1980 337 .8 338.3 340.1 340.9 341.5 341 .3 339 . 4 337. 7 336.1 336.1 337.2 338 . 4 338 . 7 

1981 339 . 3 340 .4 341.7 342.5 343 . 0 342 . 5 340.9 338 . 7 337.1 337 . 1 338.5 339.9 340.1 

1982 340.9 341.7 342 . 7 343 .7 344 . 3 343.4 342.0 340.0 337.8 338.0 339.2 340 . 6 341.2 

1983 341 . 4 342.7 343 . 0 345 . 3 345.9 345 . 4 344 . 2 342 . I 340.1 340.2 341. 4 343.0 342.9 

1984 343 .6 344.5 345.1 347. 3 346 . 6 345 . 0 342 . 7 340.9 341 .1 342 . 8 344 . 3 344.2 

SMa 

1973 

1974 

1975 

1976 332 . 4 331. 9 33 1. 3 33 1.2 330 . 6 331. 3 331 .1 331.1 331 . 3 331. 5 331. 9 331 . 9 331 .5 

1977 331 . 9 332.0 332.1 332.2 332.8 332.7 332 . 2 333 . 1 332.9 333 . 3 

1978 334.7 335 .2 335.4 335. 1 335 . 3 335 . 0 335 .7 335. 6 

1979 336 . 2 336.0 336.6 335 .9 336 . 0 336 . 4 336 . 3 336 . 3 336 . 6 336 . 6 336 . 9 

1980 337 . 5 337 . 6 337.9 337.3 337 . 7 338 . 0 338 . 3 338 . 3 338 . 2 338 . 1 338 . 5 338 . 9 338 .0 

198 1 339 . 0 339.3 338 . 9 339 .6 338 . 9 339.2 339.0 339 . 2 339 . 2 338 .9 339 . 5 339 . 8 339 . 2 

1982 340.4 340.4 340.4 340.3 339 .9 340.0 340 . 5 340 .4 340 . I 340. 0 340 .2 340 .2 340 . 2 

1983 340 . 0 340. 5 340 .8 340.6 341 .1 341. 6 341 . 9 341 . 9 341 .9 342 .1 342 . 4 342 . 6 341. 4 

198 4 342 . 9 343 .2 343.1 343.3 342 . 3 342.6 342 . 9 343 . 0 343 .2 343 . 1 343 .1 343.7 343 . 0 

spa 

1973 

1974 

1975 329 .1 328.8 328 . 5 328.3 328.6 328.6 329.4 329 . 8 330 . 1 330 . 3 330 . 2 330.2 329.3 

1976 330 .1 329 . 8 329.6 329.6 329 .7 329 . 9 330 . 3 330.7 331 .0 331 .1 331 . 1 331 . 1 330.3 

1977 330 .9 330 . 3 330 . 3 330 . 6 33 1.0 331 .4 331.8 332 . 2 332 . 7 333 . 0 333 . 0 332 . 7 331 .7 

1978 332.6 332.4 332.3 332.5 333 . 0 333.3 333 . 8 334 . 4 334 . 9 335 .0 334.9 334 . 7 333.7 

1979 

1980 336 .1 336.0 336 . 0 336 .2 336 . 6 336.9 337 . 4 337 . 7 337 . 9 338 .1 338 .0 338 . 0 337 .1 

1981 337 . 8 337 . 8 337.9 337. 9 338. 1 338 . 3 338 . 7 339 . 0 339 . 2 339.1 338 .9 338 . 5 338 . 4 

1982 338 . 5 338.6 338.4 338 . 6 338.9 338.9 339 .2 339.6 339 . 9 339 . 8 339 . 5 339 . 2 339 .1 

1983 339 .7 339 . 5 339 . 5 340.0 340.4 340 . 5 341 . 0 341. 6 341.7 341 . 8 341 . 8 341. 7 340 . 8 

1984 34 1. 8 341. 7 341. 4 341 . 4 34 1. 5 341. 7 342 .0 342 . 7 343 . 1 343 . 4 343 .2 343 .0 342 . 2 

31 
FLASK SAMPLE CO 2 MEASUREMENTS 

The purpose of the GMCC Flas k Sampling program is to measure the global 

distribution of atmospheric CO2 concentration with a greater spatial 

resolution than is practical by in situ monitoring . Collecting whole air 

samples in glass flasks for subsequent analysis in the GMCC laboratory in 

Boulder is a cost-effective way to obtain CO 2 concentration data from a global 

network of remote sites. The informati on obtained in this way is used to 

locate regional scale sources and sinks of CO 2 and to study the global carbon 

cycle , both directly and through carbon cycle models . 

In 98 ~, samples were collected once or twice per week at the 2~ sites 

shown in fig. 2 . The sampling and analytical procedures have been described 

by Komhyr et al. (1983) and Komhyr et al. (1985) . In 198~ , flask sampl ing was 

begun at Christmas Island in the equatorial Pacific Ocean and at Cape Grim , 

Tasmania . The Christmas Island site fills a major gap in our network coverage 

between Guam and Samoa in the Pacific Ocean. This site was added to the 

net work through the cooperation of C. D. Keeling at SIO . The sampling at Cape 

Grim is a cooperative effort with G. Pearman and P. Fraser of the Austral i an 

CSIRO. Initial indications are that Cape Grim is a much better location for 

CO2 sampling at this latitude than the site at Kaitorete Spit , New Zealand . 

After a sufficient period of overlap , sampling at the New Zealand site may be 

terminated due to interference by local vegetation, agricultural activity , and 

proximity to anthropogenic sources in Christchurch . An additional benefit of 

sampling at Cape Grim is the opportunity for intercomparing data with another 

prominent CO 2 measurement program. Intercomparisons of this sort are useful 

in monitoring and improving the sampling methodology and comparability of 

measurements made by different groups. 

· S 

I 

i 

I j 

I 

I , 

Figure 2.--Locations of GMCC flask sampling network sites in 198~ 

32 
The first year (1983) of samples from Halley Bay, Antarctica was received 

in Boulder in 1984. The data appear to be of high quality and provide 

valuable information concerning CO 2 gradients in the Southern Hemisphere. The 

sites at which samples were collected in 1984 are listed in table 2 . 

Code 

AMS 

ACS 

AVI 

AZR 

BRW 

CBA 

CGO 

CHR 

CMO 

COS 

GMI 

HBA 

KEY 

KPA 

KUM 

MBC 

MLO 

NWR 

NZL 

PSA 

SEY 

SMO 

SPO 

STM 

Table Z.--GMCC CO 2 flask network sampling sites during 1984 

Station 

Amsterdam I. 

Ascension 1. 

St . Croix, VI 

Terceira I. , Azores 

Barrow , AK 

Cold Bay , AK 

Cape Grim , Tasmania 

Christmas 1. 

Cape Meares, OR 

Cosmos , Peru 

Guam, Mariana I. 

Halley Bay, Ant. 

Key Biscayne, FL 

Kitt Peak , AZ 

Cape Kumukahi, HI 

Mould Bay, Canada 

Mauna Loa , HI 

Niwot Ridge , CO 

New Zealand 

Palmer Station, Ant. 

Mahe I ., Seychelles 

Cape Matatula, Am. Samoa 

South Pole, Ant. 

Station M 

Lat i tude 

(deg) 

37.95S 

7.92S 

17 . 75N 

38.75N 

71 . 3ZN 

55 . Z0N 

40.68s 

2 .00N 

45.00N 

1 Z. 12S 

13.43N 

75.67S 

25.67N 

32.00N 

19.52N 

76 . 23N 

19 . 53N 

40.05N 

43.83S 

64 .92S 

4.67S 

14.25S 

89.98S 

66.00N 

Longitude 

(deg) 

77.53E 

14.42W 

64 . 75W 

27.08w 

156 . 60W 

162.72W 

144.73E 

157.30W 

124.00W 

75 . 33W 

144.78E1 

25.50W 

80 . 17W 

112.00W 

154.82W 

119.33W 

155 . 58H 

105.63W 

17Z . 63E 

64 . 00W 

55.17E 

170.57W 

24.80W 

2.00E 

Elevation 

(m) 

150 

54 

3 

30 

1 1 

25 

94 

3 

30 

4600 

2 

o 

3 

2095 

3 

15 

3397 

3749 

3 

10 

3 

30 

2810 

o 

In 1984 -6000 flasks were analyzed for CO 2 concentration. Of these -4000 

were from the flask network and the remainder were from cruises or were test 

flasks used to monitor the operation of the analytical apparatus. As 

described in Harris and Nickerson (1984) , many of the network flasks are also 

analyzed for CH4 concentration by gas chromatography. This project is 

described in the next section of this report. 

The 1983 flask data have been reprocessed to take into account drifts in 

the concentr ations of the flask analysis reference gases and analyzer nonlinearity . These data are essentially final pending recalibration in 1985 of 

the GMCC secondary standards at the HMO CO 2 Central Laboratory at SIO. The 

1984 flask data have not yet been reprocessed and should be considered 

provisional. The annual mean CO Z concentrations for the network are 

summarized in table 3. 

33 
Table 3.--Annual mean atmospheric CO 2 concentrations (ppm relative 

dry air--X81 mole fraction scale) for the flask network sites 

to 

StHlon 196& 1969 1970 \911 PHZ 197) 197' 1975 1976 1917 "" 1979 '980 19&1 19&2 1,8) "" 

u., • • • • • • • • , 1335.91 ))1.8 H9.3 339.' )1\ .1 O'Z.21 

'" , • • • • • • • • • [nT.]) ]38.8 )l9.7 31 0.7 3_2.6 )').7 

'" , , , , , , , • , , • Jl7.1 B9.6 )10._ JI O.9 )'Z.O !~1.2 

'" , • • , , , , , • , , , ))8.' H9.'> )~1 .2 )1).0 )H,' 

." , • , In.' ))C.2 3]2.0 lB .• H).O 313.9 BS.:J 336.6 337.7 )10.2 ]11.5 ]12.1 )",0 3'5.-

'" , • , , , , • , • , , H7.8 )39. ! 3=1.3 )11.9 )1),' )15.3 

CO. , , , , , , , , • , , , , , , , ]12.0 

"" • , , , , , , , , , , , • • , , )n.8 

CI'IO • , , , , , , , , • , , , , ]1\ .2 )IZ.9 ]",8 

no , , • , , , , , , • , , , 339.7 , , • au , , , , , , , , , • • H7.7 3'0.0 ]H.2 )1' ,0 )IZ.1 )".2 

'" , , • , , , , , , , • • , , • 3" o • J=:!.,> 

K~I , , , , , 310.7 (1)1,1] , ))2.7 ))5.2 lH.7 H8.' 0=0.2) )IZ.O )11.6 31).- )15.1 

~, , , , , , , , , 332.3 ))~. = ]]5.7 131· • H9.3 3'0.- )".2 )12.5 )".1 

~!C • , , , • , , , , , , , ]10.3 ):1.9 ]'Z.5 )').1 )15.6 

~~O • , • , , , , , , , , 3)1.3 , , , , , .l..O , on.a] 325.Z , , , , , 332.1 3)3.6 ])5.2 US.1 ])8.9 )10. ~ 31\ .0 )12.5 )').9 

"'" !13.1 )2t,l )25.6 325.2 ]26.3 330.2 [33 1 .0] , ))2.1 3):. ~ 335.7 Bl.O ]]5.1 339.9 3-0.9 ]tl. , )".6 

'" , , , , , , , , , , , , , , • )'0.7 )'2. 1 

'" , , • , , , , • , , 13).9 BS.2 (337 .51 )10.0 3)9.6 )tl.O ]12.7 

'" • , , , , , , • , , , • H9.1 ]'0.1 )~0.5 ]IO.! ]u.O 

"" , , , • , (HO.2] ]]0.8 ]]0.7 Bl.~ H2.! 31'.3 3]6.0 3l&.1 m.3 3~0.' 311. , )'].0 

'" , , , , , , , 129.' 330.2 331.S ])].7 33S.S H6.7 H!.5 3)9.3 110.S )12. 1 

'" , )2_.0 326._ )26.9 321.6 , , , , , , , , , , , , 

"" , , • , , • , , , , , , JII.9 3~1. 7 1~2.6 3n.! 

HOl., (J • nl.otler or Inttrpgl.Ud pgLnu l on.-II.lr or tOld n .. Wr or poLnu, () • InccapLn. fur. 

Several events occurred in 1984 which affected the data records f or some 

sites. Problems in shipping procedures resul ted in flask shortages and, 

therefore, gaps in sampling at Seychelles. This was solved by air freighting 

a large suppl y of flasks to the site so that delays in mail service could be 

tolerated. At Halley Bay it was discovered that during the austral wi nter , 

the sample taker changed the location of sampling which reSulted in sampling 

grossl y contaminated air. Fortun ately , the sampl es collected before and after 

\Vi nter , and two sampl es collected during the Winter, were collected properly, 

and have enabled thf' calculation of an annual mean concentration. At 

Amsterdam Island, also during winter-over , the sample taker experienced some 

personal problems whi ch resulted in several large gaps in the record and some 

doubts about the techniques used in collecting the samples that were taken . 

This was followed by a summer season during which a new station was 

constructed accompanied by more gaps in sampling. Thus, the annual mean 

calculated for 1984 at Amsterdam Island is somewhat uncertain pending further 

examination of all the data. At Palmer Station, also during Winter-over, the 

samples were collected through a manifold connected to an outside sampling 

stack. It appears that in August 1984, the manifold may have developed a leak 

allowing room air to contaminate the samples; however, most of the Palmer 

Station record is good and it was not difficult to eliminate the obviously 

contaminated samples. 

The annual mean CO 2 concentrations for 1981-1984 are plotted vs. latitude 

in fig . 3. It is clear that the network is improving in its ability to define 

the latitude gradient . Christmas Island is especially crucial in determining 

location and magnitude of the local maximum in CO2 concentration near 5· N. 

Also the addition of Halley Bay and Cape Grim are confirming the suggestion of 

a local maximum between 40· S and the South Pole. The quality and resolution 

of this data provides a very good set of constraints for assessing the ability 

of various models to simulate the global carbon cycle and transport of CO2 in 

the atmosphere . Also note in fig. 3 the suppression of the equatorial maximum 

during 1982 . Gammon et al. (1984) have suggested that this effect was due to 

reduced upwelling of CO 2-rich deep water in the equatorial Pacific during the 

ENSO event of 1982-83 . Figure 3 shows a partial recovery of this feature in 

1983 and a complete recovery in 1984, again more clearly defined by the data 

from Christmas Island. 

34 
'" 

'" 

, .. 

'" 

'" ,.. 

m 

,., 

, .. I m 

~ ,., 

,., 

w 

,., 

m 

,., 

,., 

,., 

m 

m 

KIVl llllllu:.£ &AA.DICfit 

It .. 

• un 

In, 

1111 

; ; , lllT llUD( • 

figure 3 .--Annual mean CO 2 

concentrati ons vs. latitude 

for the GMCC flask Sampling 

NetHork. Key Biscayne 

(26 °N ) has not been used in 

draHing the curves. 

-, 

-, 

COZ PPI'VYEAA Grice rU:;SI< IIET;';ORK 

1999 1981 19B1 J 994 

Figure .-- Globally averaged CO 2 

growth rate calculated from the 

GMCC Flask Network data. 

The global mean annual growth rate calculated quarterly from the flask 

network data is plotted in fig ~. It was suggested by Gammon et al . (198~) 

that the decrease in the growth rate observed during 1982 was also a result of 

the unusually intense ENSO event . The rebound of the growth rate in 1983 to 

unusually high values of -2 . 0 ppm/yr is consistent with the results of 

Bacastow (1976) . In 198~ the growth rate has returned to a value of -1.5 

ppm/yr , more typical of the mean value over the past decade. 

Plans for the flask network in 1985 include possible termination of 

sampling at New Zealand; initiation of sampling at Shemya Island, Alaska; 

Alert , N.H.T., Canada; Midway Island; and South Georgia Island; and continued 

studies on the use of gr easeless stopcock flasks. The 1983 and 198~ flask 

data will be finalized and archi ved with HMO and with DOE/CDIC . 

FLASK SAMPLE METHANE MEASUREMENTS 

The measurement of atmospheric methane in air samples collected from the 

NOAA /GMCC C02 flask network continued through 198~ . These measurements were 

begun in 1983 as a cooperative program between CSIRO , NOAA/GMCC and OGe (see 

GMCC Summary Report No. 12, 1983 , pp. 163-165) . During 198~ there were 22 

active sites in this globally distributed flask sampling network, and these 

are indicated both in fig . 2 and table 2. 

35 
Results obtained at two of these sites (South Pole and Mould Bay) from 

the beginning of the program through to the end of 1984 are shown in fig. 5 . 

Data from the South Pole illustrates clearly the features found at all sites 

south of Samoa , with a smooth seasonal cycle and an average long-term increase 

of approximately 1% per year. These measurements represent the first reported 

observation of a complete seasonal cycle of atmospheric methane at the South 

Pole. The long-term growth rate, as well as the phase and amplitude of the 

seasonal cycle are highly consistent with results from several years of 

measurements reported by Fraser et al. (1984) for the site at Cape grim in 

northwest Tasmania. 

""" 

'>' ! 1100 

"'" 

lo4ould Boy (IoISC) 

Sovth Pole (SPO) 

1983 

. . . . . , . . 1984 

Figure 5.--Atmospheric methane at SPO 

and Mould Bay , Canada. Square symbols 

represent individual flask measurements 

and are normally the mean of two 

replicate determinations. The cross 

symbols indicate values which are not 

believed to represent background 

conditions. The fitted lines are cubic 

splines (Reinsch , 1967), and are fitted 

to only those data considered to be 

background values. 

The results from Mould Bay illustrate that at sites in th e Northern 

Hemisphere there is a more complex seasonal variation, a larger amplitude, and 

a difference in phase of the seasonal changes to those seen in the Southern 

Hemisphere. Nevertheless, the long-term growth rate found at the northern 

sites is similar to those measured at sites in the south. Another feature 

apparent from the data shown here is the significant l atitudinal gradient , 

averaging an 8% difference in concentration between these two sites during 

thi s per iod. 

A complete description of this program and 2 years of data from all sites 

is reported by Steele et al. (1985) . 

4.2 Special Projects 

INTRODUCTION 

In addition to in situ CO 2 monitoring at the four baseline observatories 

and the flask sampling network, the CO 2 Group undertakes special projects 

which are deemed appropriate to meeting overall program objectives. These 

projects involve field measurements intended to supplement or expand on the 

data from our existing sites and the development and evaluation of CO 2 

measurement technology. Also, studies are undertaken to analyze and interpret 

the CO 2 data sets and to investi gate various aspects of the global carbon 

cycle and atmospheric transport of CO 2. Several activities of this type which 

occurred in 1984 are described in this section. 

36 
MEASUREMENTS OF CO 2 AND CH4 BY GAS CHROMATOGRAPHY AT MAUNA LOA OBSERVATORY 

In 1983 the GMCC CO 2 Group received two gas chromatographs constructed by 

R. Weiss of SIO. These instruments are designed to measure CO 2 concentration 

with a precision comparable to that of non-dispersive infrared analyzers, and 

are also capable of measuring CH4 (Weiss, 1981). After laboratory tests of 

the precision, linearity and accuracy were performed, a chromatograph was 

installed at MLO in March 1984. The chromatograph operated successfully and 

data were collected until the eruption of Mauna Loa on 25 March 1984. Because 

components of the chromatograph system are susceptible to damage during power 

failures, it was decided not to restart the chromat ograph until regular line 

power (as opposed to generator power) was restored to the o bservatory. The 

chromatograph was restarted in September 1984, and ran successfully through 

the end of the year . 

The objective of this project is to compare the gas chromatographic to 

the NDIR method of CO 2 monitoring at a baseline observatory. The frequency of 

volcanic outgassing of CO 2 during 1984 has made this comparison somewhat 

difficult. Since the GC makes six discrete measurements each hour, whereas 

the NDIR analyzer makes essentially continuous measurements, it is unsatisfactory to compare the two results during periods of highly variable CO2 concentration. Figure 6 shows a comparison of hourly means during 4 days in 

October chosen for a lack of volcanic activity and a CO2 concentration showing 

little short-term variability. This comparison suggests an offset of -0.1 ppm 

between the two measurements with a scatter (10) of -0.14 ppm. The 0.1 ppm 

offset may be due to inaccuracies in the concentration values assigned to the 

reference gas tanks used by each system. This will be investigated further 

after the GMCC secondary standards are recalibrated at SIO, and any drift 

corrections are applied to the assigned tank values. In general, the 

agreement between the two methods looks quite good. 

An added advantage of the GC method is the simultaneous measurement of 

CH 4 , an infrared absorbing gas of considerable interest with respect to 

climate change (see , for example, Ramanathan , et al., 1985). As discussed in 

Harris and Nickerson (1984), and elsewhere in this report, GMCC in cooperation 

with OGC and CSIRO has been measuring atmospheric CH 4 concentration in samples 

from the CO 2 flask network since 1983. The MLO GC CH4 data are useful in 

looking at the nature of the variability observed in the flask sample data. 

Figure 7 shows daily means calculated from the high frequency discrete samples 

of the MLO GC superimposed on the one-sample-per-week-flask record . 

First, it is interesting to note the excellent agreement between the in 

situ and flask sample measurements, especially considering that the flask 

sample measurements are made with a different type of chromatograph . 

Secondly , it is clear from the in situ measurements that the day-to-day and 

week-to-week variability in atmospheric CH 4 exhibits structure which is likely 

related to atmospheric transport and the action of sources and sinks. In the 

flask record, variations of this frequency are manifested as scatter since 

samples are only collected once each week. 

37 
fJl 

W 

MLO GC - IR .• r---.----~----------.--------~ (~) 

. .. 

3 a f------------'----'-'-'-·7· -'----'.-'-",,--1 ~ , > 

~ 

f-

...J 

W 

Q 

-.' ~-----------------.~----~ 

MU," • 0.07 PPM 

STO OtV • D.1l FPII 

OCT 19U 

.h ...n,n- .n. .rflf 

9 10 

'fh- ,n 

-0.\ -0 .2 0 0.2 0._ 

C02 (OHC[NHATlUH 

Figure 6.--Comparison of CO 2 

measurements by the NDIR 

and GC methods at MLO. 

a) Differences between GC 

and NDIR hourly means for 

7-10 October. b) Histogram 

of the differences . 

185er::;:..:::..;= Mauna Loll. ______ --__ ~--~ __ __.::.=.;.::.::.:.; 20N 15614 

Issa 

1750 

> ! 1729 

~ 

1659 ~ 

:z: 

u 

160a 

1550 

Isea JI'I'I fa 1ft! _ r«T J\.N 1U. l'I.IIO $(P OC'T PIOV lICe 

1984 

Figure 7 .--Comparison of in 

situ (solid line) and flask 

measurements (squares) of 

atmospheriC CH 4 at MLO . 

The continued operation of the MLO GC during 1985 will enable a more 

thorough evaluation of the method for measuring CO 2 and will provide a record 

of CH 4 concentration which will nicely complement the flask sample record . 

SHIPBOARD MEASUREMENTS OF ATMOSPHERIC CO 2 

In 1984 the CO 2 Group continued to collect flask samples aboard 

occasional oceanographic cruises. The purpose of this project is to make 

detailed measurements of atmospheriC CO 2 (and CH 4) concentrations over large 

regions of the earth ' s surface to assess the ability of the limited number of 

stations in the CO 2 flask network to determine the global distribution of 

atmospheriC CO 2, The results from cruises in 1982 and 1983 have generally 

supported the representativeness of the flask network , while demonstrat ing 

that the network is not able to locate steep latitudin al gradients or resolve 

the variati on of CO 2 with longitude (Bodhaine and Harris . 1983; Harris and 

Nickerson , 1984) . 

38 
The cruise tracks for two sampling programs completed in 1984 are shown 

in fig . 8 . The Long Lines expedition aboard the R/V KNORR took place in 

October 1983 and Janua ry 1984 in the equatorial and South Atlantic Ocean. The 

cruise of the NOAA R/V DISCOVERER covered the equatorial and South Pacific 

Ocean during February through May 1984. 

Figure 8.--Long Lines Expedition October 

1983 and January 1984 (-) and the 1984 

DISCOVERER cruise (-.-). The solid 

circles show the locations of the GMCC 

Flask Network sites. 

The CO2 concentrations determined from the flask samples collected during 

the Long Lines expedition are plotted vs. latitude in fig. 9. The plotted 

points represent averages of pairs of simultaneously collected flasks or, when 

the two members of a pair differ by more than 0.5 ppm , the lower value is 

plotted. For this cruise 15 of the 40 pairs failed to meet the 0.5 ppm 

criterion , with most of the bad pairs occurring during the first leg (October 

1983. Also plotted in fig . 9 is a curve showing the CO 2 concentration 

interpolated from a zonally averaged CO 2 latitude day-of-year surface obtained 

from the flask network for the dates and latitudes covered by the cruise 

track . This surface is obtained by smoothing the data from the CO 2 flask 

network to produce a representation of the variation of atmospheric CO 2 with 

latitude and time. 

'" 

'" 

! 

8 

] 

; 

• • •• 

•• b-oii6~.ooo-ib:J..~.-.~~.~.Jl.-._o .. a_-.-. Q_Q,~ 

. . 7 1 

Figure 9 .--Flask sample CO 2 data vs. 

latitude for the Long Lines 

Expedition. The dashed curve represents 

the CO 2 concentration interpolated in 

time and latitude from the smoothed 

distribution of atmospheric CO2 calculated from the Flask Network 

data. 

39 
As seen in fig. 9, the agreement between the Long Lines flask sample data 

and the CO 2 latitude day-of-year surface is rather good . On the first leg of 

the cruise, the flask data are variable and tend to lie above the curve. This 

may be due to sample collection problems resulting in contaminated samples 

(most of the samples were bad pairs) or there may actually be high local 

concentrations of CO2 over this area of the Atlantic. The proximity of the 

African continent suggests the possibility of biospheric effects contributing 

to the variability. On the second leg, the agreement between the cruise 

samples and the curve is excellent indicating that SOuthern Hemisphere air is 

well mixed and the assumption of zonality in constructing the surface is 

valid. 

The samples from the DISCOVERER cruise are similarly compared to the CO 2 surface in fig. 10 . Again the agreement with the curve is quite good. The 

data between 10-20 0S tend to lie above the curve while those from 20-30 0S are 

below the curve . This suggests the possibility that a steeper gradient of CO2 concentration was sampled on the cruise than is detected by the network. From 

~0-600s the agreement of the cruise data with the curve is excellent, again 

demonstrating the well-mixed nature of the atmosphere in the Southern 

Hemisphere. 

! 

IIlSCovt.JlOO lSi. 

.. , ',- /a.~Il.o~~o·· 

o c.. 0 0° o.Q/~ 0 ,110'--- 0 

o 0 8 . .Q~·o "'I "8.'-"_' ___ --- ", 

m Il-.-_____ _ . 

T , 

UlTlTUD£ 

Figure 10 .--Flask sample CO 2 data vs. 

latitude for the DISCOVERER 198~ 

cruise. 

in fig. 

of this 

The dashed line is as described 

9, for the dates and latitudes 

cruise. 

The samples collected on these two cruises provide further evidence for 

the representativeness of the CO 2 flask sampling network. The assumption of 

zonal averaging used in constructing the smoothed surface is also supported, 

particularly for the SOuthern Hemisphere. The data from both cruises 

demonstrate the existence of regional effects (near Africa and in the 

equatorial Pacific) which may not be detected by the network. 

198~ OCEANOGRAPHIC ACTIVITIES ABOARD DISCOVERER 

The Carbon Dioxide Group participated in the CO 2 DynamiCS Cruise aboard 

the NOAA Ship DISCOVERER during 198~. The Weiss-design gas chromatograph was 

loaded aboard the ship in Seattle prior to the 1~ February departure on Leg 

1. The equipment was set up by Tom Conway and Lee Waterman while the ship was 

in Honolulu, 23-27 February. Lee Waterman operated the program on Leg 2 

(Hawaii to Tahiti) and Leg 3 (Tahiti to American Samoa). On the return track, 

~O 
the monitoring program was operated by Marilyn Roberts (PMEL) from Pago Pago 

to Honolulu, and by Glen Frick (NRL) from Honolulu to Seattle. The ship's 

track is shown in fig. 8 in connection with the description of shipboard flask 

sampling activities. A total of 1,256 hours of atmospheric air and 1,259 

hours of air equilibrated with surface ocean water CO 2 measurements were 

obtained between 28 February and 6 May. 

The 1984 monitoring program aboard the DISCOVERER was identical in most 

respects to the mode of operation aboard the AKADEMIK KOROLEV on the SAGA 

Expedition (GMCC Summary Report No. 12, 1983). Noteworthy differences are (1) 

a single atmospheriC intake located at the bow of the ship was used for all 

measurements; (2) the surface ocean water was pumped from an intake located in 

an underwater observation chamber in the bow of the vessel; and (3) more 

frequent surface water temperature measurements were obtained than was 

possible on the Soviet ship. Preliminary results are graphically depicted in 

figs. 11 and 12. Each point represents the mean of all measurements of 

equilibrated air made over one degree of latitude. A correction has been 

applied to remove the increase in CO 2 concentration of the equilibrated air 

caused by warming the water in the transmission line between the seachest and 

the ship's laboratory. The mean atmospheriC CO 2 concentration is represented 

by a straight line and is intended to be a reference level for illustrating 

the CO 2 undersaturation and supersaturation in the ocean surface waters. 

DISCOVERER 198<1 

'" 

.. '" • 

~ 

N 

a 

u '" • 

". 

'" ~ ~ ~ ~ g ~ • ~ ~ g - • LAT Cdeg] 

Figure 11 .--pC02 along 

track at 150 0 W long . 

~ • ~ ~ " 

" 

N to S 

.. 

• 

~ 

N 

a 

u 

• 

". 

.,. 

'" 

'" 

'" 

DISCOVERER 1984 

Figure 12.--pCOZ along S to N 

track at 170 0 W long. and Honolulu 

to Seattle. 

Figure 11 depicts the results for 18 February to 29 March from Hawaii to 

Tahiti and then to nearly 57°S , the track being mostly along 150 0 W 

longitude. The equatorial supersaturation feature is usually observed as 

rising abruptly to a region of maximum values, then declining abruptly to near 

equilibrium , Harris and Nickerson (1984) . This time it has a shoulder between 

-5 0 S and -20 0 S, the approximate latitude of Tahiti. This shoulder disappears 

at 170'S longitude on return leg to Seattle , 29 March to 9 May (f i g . 12). 

While north to south , the KOROLEV track shows the equatorial supersaturation 

feature shifted uncharacteristically southward by -5° , the other three 

crossings made in 1983-84 bear close similarity. Likewise , on all four 

tracks, the surface ocean is undersaturated for most of the time between -45°N 

41 
and -57 OS (see fig. 92 and 93, Harris and Nickerson 1984). Both the KOROLEV 

and DISCOVERER results , when compared with the SIO "Downwind" and "Monsoon" 

expeditions data, show the major features of the CO 2 distribution in the 

surface waters of the Eastern Pacific Ocean remain unchanged even as the 

atmospheric CO 2 continued to increase . For example, while the atmospheric CO 2 level has increased about 25 ppm in the past quarter century, the equatorial 

surface waters have maintained the 90-100 ppm supersaturation originally 

observed in 1957 (Keeling et al., 1965 ) indicating an uptake of industrial CO2 and a rapid adjustment to maintain the status quo. These observations support 

the conclusions of Takahashi, et al. (1982) and Roos & Gravenhorst (1984), 

concerning similar adjustments in the surface waters of the North Atlantic 

Ocean. 

RESULTS FROM A TWO-DIMENSIONAL CARBON CYCLE MODEL 

The GMCC Carbon Cycle Model was designed to serve the interests of the 

GMCC effort in CO 2 research . It is focused largely on time scales of a year 

to a few years , on a global scale, and on having time resolution of 1 day. It 

is designed to provide comparison CO 2 concentration time series for specified 

locations and to develop (by comparison with CO 2) observations of the globalscale properties of the atmospheric reservoir of the global carbon cycle. 

The model is two-dimensional , and has transport/diffusion as originally 

developed by Machta (1974). Spatial resolution is 20° latitude bands and land 2- km layers . Coeff i ci ents were adj usted from Macilta' s original val ues to 

reproduce spatial distribution of CFC-ll . A two-layer ocean simulation was 

added to the model , where the upper (mixed) layer has a depth that varies 

seasonally throughout the year . Ocean carbonate chemistry was that of 

Bacastow (1981), and the dissociation constants are as given by Weiss (1979) 

and Mehrbach et al . (1973). Salinity and alkalinity data were obtained from 

GEOSECS and TTO experimental data , and ice cover of the oceans data were 

obtained from the World Data Center in Boulder , Colorado. Wind stress and 

water temperature data were obtained from the literature (Hellerman , 1967; 

Defant, 1961) . A theory of ocean-air exchange of CO 2 by Kerman (1984) was 

used to calculate CO2 fluxes for the model. 

One of the most innovative parts of the model was the use of carbon 

fluxes as calculated from the global biospheric models of E. Box (University 

of Georgia , Athens ; personal communication, November 1983) . Fossil fuel 

sources were obtained from the data of Rotty (1982) . Carbon 13 as well as 

total carbon 'were considered by the model. Biospheric fractionat i on was that 

of Keeling (1973) , oceanic fractionation was that of Siegenthaler and Munnich 

(1981), and fossil fuel isotopic data were obtained from Tans (1981). 

The general resulr~ of the model gave pole-to-pole CO2 differences of 3.4 

ppm and pole-to- pole 0 C differences of 0.35 . The airborne fraction for the 

conditions of the base case was 51% , and the annual increase was 1 . 5 ppm for 

CO 2 and -0 . 096 ~ermi 11 e for 01 3C. (See the GMCC 1984 Annual Report for a 

discussion of 01 C). 

The overall results of the model are shown in figs. 1 and 2. In these 

figures , the CO 2 and 013C values are plotted vs . DOY and latitude . Good 

general agreement with observations of CO 2 from the GMCC flask network was 

found. 

42 
Specific applications of the model have been made to answer questions, 

evaluate global estimates, and compare with questionable observations . 

Following are three examples of such applications. In examining these , one 

must remember that the model used to answer the questions is limited in 

dimension and represents only one approach to simulating the carbon cycle . 

Figure 13.--Model CO 2 concentrations 

atmospheric CO 2 at sea level vs. 

latitude and day of year. 

• 9 

.1 

Figure 14.--Model 613C values for 

atmospheric carbon at sea level vs. 

latitude and day of year. 

Example 1. Annual Fluctuation of CO 2 - What does it say about the biospheric 

activity in the latitudes north of 50 0 N? 

From even a casual examination of fig. 13, the overall pattern of CO 2 concentration vs. time and latitude, the largest fluctuations of atmospheric 

carbon dioxide concentration occur in the latitude band of 50 o -70 o N. A 

logical question may be asked: Does the maximum biospheric activity also 

occur in this same latitude band? 

The answer may be seen in terms of absolute change of carbon mass in the 

sea level box of the model for each of the latitude bands used. The causes 

for carbon mass change in the atmosphere are (in this model) anthropogenic 

sources, biospheric exchange , air-sea exchange, and atmospheric transport/ 

diffusion. These changes are depicted in terms of bar graphs for each month 

of the year along with the net change for three latitude bands : 50 o -70 o N (fig. 

15) and 10o -30 o N (fig . 16) . For the latitude band 50 o -70 oN we indeed see that 

the net change follows the biospheric change except for the months of May and 

September. In April, there is a considerable biospheric carbon change 

accompanied by almost no change in the net atmospheric carbon concentration. 

The two largest producers of atmospheric carbon change are the biospheric 

exchange and transport/diffusion . Anthropogenic carbon input is next in 

importance, followed by air/sea exchange. When we compare the biospheric flux 

at latitude band 10 o -30 oN with that of latitude band 50 o -70 o N, we see that 

there is a much larger flux of carbon into and out of the biosphere farther 

south. This contrasts to the equally much larger concentration changes for 

the more northern location , as shown in fig. 14. Again the net carbon change 

43 
1.2 ,---------------------------------~ 

co 

~ 

5 0 . 0 

'" C) 

"-

tn 

W 

U 

fr: 

:::J 

C) 

if) 

u ~ 8IOSPII[R[ D Irl{JUSTRY ~ OCEnll I>SSI OlrrUSION CJ TOft\.. 

-1.2 

J 11 A II J J A 

1I0NTH 

5 0 N o 

Figure 15.--Monthly carbon sources for latitude band 2 (50 0-70 0N). 

The net carbon source is a sum of the biospheric, industrial 

(anthr opogenic ) , and oceanic sources and diffusive flux. 

if) 

z 

C) 

fa: 

'" '" 

f1. 2 

5 0 .0 

'" C) 

"-

V> 

W 

U 

'" :::J 

o 

tn 

u 

-1.2 

BIOSPl1[R[ Cl ]tlDU5TRT ~ OCUlI! ~ DlfrUSION CJ TOTAl 

J r M A M J J A SON 0 

11 nNTH 

Figure 16.--Monthly carbon sources for latitude band 4 (10 0-30 0N). 

The net carbon source is a sum of the biospheric, industrial 

(anthropogenic) , and oceanic sources, and diffusive flux. 
in the atmosphere is much smaller than the change of carbon from the biospheric flux. The biospheric and transport/diffusion carbon changes are of 

roughly the same size, followed by air-sea exchange, and last by anthropogenic 

input. The total change of atmospheric carbon in the southern latitude band 

is larger than that in the northern latitude band. The difference in the 

resulting atmospheric concentrations comes about from two factors: the smaller 

amount of land and ocean area in the latitude band 50 0-70 0N than in the 

latitude band 10 0-30 0N (almost a factor of one half); and probably more 

important , the mixing of the CO 2 into the atmosphere . In the far north the 

vertical mixing is far less effective than it is farther south. In effect, 

the CO 2 is mixed into a smaller volume of air in the far north than it is in 

the south . The overall effect is then to create very much larger 

concentration differences from smaller absolute changes of atmospheric carbon 

mass . 

Another example of the profound effect of the vertical mIxIng and smaller 

area of a latitude band , is the large concentration fluctuation in the 

latitude band 70 0-90 0N, which results from a relatively small change of 

atmospheric carbon mass. The strongest influences in carbon change in this 

farthest northern latitude band is air-sea exchange and diffusion. The small 

net change is thus not a biospheric signal in this latitude band as much as it 

is a transported signal from farther south, along with an oceanic CO 2 

modification. 

Example 2. Change of annual CO 2 increase by change of ocean-a ir exchange 

As discussed in the interpretation of the Pt . Barrow CO 2 data in this 

volume, in the El Nino year of 1982 the annual increase of CO2 in the air was 

significantly smaller than in the previous 2 years and , in the year following 

the El Nino the annual increase of CO 2 was larger than normal. The GMCC CO2 

Group set out to determine whether the GMCC Carbon Cycle Model would duplicate 

the anomalous 2 years of annual increases by making changes in the sea surface 

temperature at differing latitudes and by changing the wind speeds at 

differing latitudes in a similar way to that observed during the El Nino 

occurrence. Table 4 gives the details of the alteration of the model for 

three runs in addition to the base case . As is shown for the year of the El 

Nino, the changes to the base case for all three runs were that the sea 

surface temperature of the equatorial latitude band (10 0N-l00S) was increased 

by 1° and the wind speed for the same latitude band was decreased to 75% of 

its base case value. At the other latitude bands , sea surface temperature was 

decreased by 1°. For the year following the El Nino, the three runs were 

changed as follows: (1) the equatorial latitude band SST was decreased to 

0.5° above the base case , the wind speed was increased to 125% of the base 

case, and the conditions at the other latitudes were restored to these of the 

base case ; (2) the equatorial SST was restored t o the base case along with the 

winds and the SST at the other latitude bands ; (3) the equatorial SST and 

winds were restored to those of the base case , along with the SST for the 

other latitudes except for 30 0-70 0N and 30 0-70 0S. Winds at other latitudes 

were changed as shown in the table. 

45 
Table 4.--Alterations of the model for El Nino 

condi tions and condi tions 1 year later 

1st Year 2nd Year 

Change Equat. Change Change Equat . Change Hind 

equat. winds SST equat . winds SST at 

SST at other SST at other other 

( °C) latitudes (OC) latitudes lat itudes 

Base 0 0 0 0 

case 

Ri..!n +1 0 . 75 -1 +0.5 1. 25 0 

Run 2 +1 0 .75 -1 0 0 

Run 3 +1 0 .75 -1 0 -0 . 5' 1.5 

(70°-30°) 

Nand S 

'Value is for 30 0 -70 0 N and 30 0 -70 0 S. At all other lati tudes , the change is 

O. 

Results of the changes on the model ar e given in table 5. The base case 

gave an annual CO 2 increase of 1.5 ppm yr- l . For the ,,1 Nino (1st) year , the 

disturbed model (Runs 1-3 ) gave a much smaller annual increase of 0 . 6 ppm 

yr- l . For the first two disturbed r uns in the year following the El Ni no 

year, the increase went to 2 . 0 and 1.9 ppm yr- 1 For the third disturbed run , 

the increase was only 0.5 ppm yr- l 

Although this simple simulation cannot be claimed as an accurate 

description of the complex El Nino phenomenon , it does pOint to t he air- sea 

CO 2 exchange as being a strong possibility in explaining some of the El Nino 

effects . 

Table 5.--Results of making the changes shown i n Table 4. 

1 s t year mean 2nd year mean 

ann ual increase annual increase 

(ppm) (ppm) 

Base Case 1.5 1. 5 

Run 0.6 2 . 0 

Run 2 0 . 6 1 . 9 

Run 3 0 . 6 0 . 5 

46 
Example 3. Are there any strong indicators that the biosphere is contributing 

to or taking away from the global CO 2 reservoir? 

This question, of course , will be answered by long-term monitoring which 

will offset year-to-year changes in CO 2 concentration growth in the 

atmosphere. The evidence that we can look at before that long-term record is 

available is complicated with short-term effects and possibly inadvertent 

noise . One normal indicator of such a contribution of the biosphere (positive 

or negative) is the mean annual increase . When we compare data on mean annual 

increase with the model value for annual atmospheric CO 2 increase, we get 

comparable results. Figure 17 shows that the mean annual increase of CO 2 for 

t he model falls well within one standard deviation of the mean for BRW and SPO 

CO 2 data for 1974-1982 . 

Likewise , in comparing the decrease of 613C values , the model shows 

general agreement with the data presented by Friedman (personal communication) . The annual decrease of 0 . 096 is somewhat larger in magnitude than 

that of Mook et al . (1983). 

Since the model has a balanced biospheric exchange budget , the above 

general agreement would not point to any obvious biospheric source or sink . 

It must be pOinted out , however , that the present model will not be suitable 

for long-term comparisons with the data because it does not have deep ocean 

Annual 

Increase 

(ppm) 

3 

2 

o 

r 

fI 

Eq 

Latitude 

-<>- Column mean 

-Sea level 

-r 

+-

--

PI. 

Barrow 

Figure 17 .--Annual increase of atmospheric CO 2 concentration 

in the model for sea level and columnar mean . The mean and 

standard deviation of annual processes observed at SPO and 

BRW for 1974-1982 are shown . 

47 
circulation , an important component in a long-term carbon cycle model . It 

should also be pOinted out that apparent agreement may also be fortuitous and 

that yet- unspecified mechanisms may have great importance for the short-term 

cycling of CO 2 , 

LABORATORY INTERCOMPARISON 

A program was started in 1984 by GMCC in cooperati on wi th WMO in or der to 

assess the agreement between laboratories around the world making CO 2 

measurements . A set of three CO 2-in-air reference gas tanks was prepared in 

1984 and sent to SIO for initi al calibration . Starti ng in 1985 , these tanks 

will be circulated to over 15 participating laboratories around the world 

where each laboratory will determine the amount of CO 2 in each tank. A 

compar i son of the results will indicate the level of agreement between 

different laboratories . 

Bacastow , R., 1981. 

Cycle Modeling , 

95-101 . 

4. 3 References 

Numerical evaluation of the evasio n factor . . I n Carbon 

SCOPE~, B. Bolin (ed.) , John Wiley and Sons , New Yor k , 

Bacastow, R. B., 1976 . Modulation of atmospheric carbon dioxide by the 

Southern Oscillation . Nature 261 :116-118. 

Defant , A. , 1961 . Phys. Oceanogr. Vol . 1, Pergamon Press , New York. 

Fraser , P. J., M. A. K. Khalil , R. A. Rasmussen , and L. P. Steele , 1984 . 

Tropospheric methane in the mid-latitudes of the Southern Hemisphere. J. 

Atmos. Chem . 1 : 125-135. 

Gammon, R. H. , W. D. Komhyr , L. S. Waterman , T. J. Conway , K. H. Thoning , and 

D. Gillet t e , 1984 . The 1982/83 ENSO event : the response of the global 

atmos pheric CO 2 distribution . Preprints , Conference on the Scientif i c 

Applicatio n of Basel i ne Observations of Atmospheric Composit i on, November 

7- 9 , 1984 , Aspendale , Australia. 

Har ris , J . M. and E. C. Nickerson (eds.), 1984 . Geophysical Monitoring for 

Climatic Change , No . 12 : Summary Report 1983 . NOAA Environment al Research 

Laboratories, Boulder , CO . 184 pp. 

Hellerman , S., 1967 . An updated view of the wind s t ress on the wor ld ocean. 

t10n. Weather Rev . 95 : 607-616 . Cor rigenda 1968 , ibid 96 : 63 - 74. 

Keeling , C. D., 1973. The carbon dioxide cycle : Reservoi r models to dep i c t 

the e xchange of atmospheric carbon dioxide with oceans and land pl ants. 

Chemist ry of t he Lower Atmosphere , S. I . Rasool (ed . ) , Plenum Press , New 

Yor k , 251 -330-.---

Keeling , C. D., N. H. Rakestraw and L. S. Haterman , 1965. Carbon dioxide i n 

surf ace ocean waters of the Pacific Ocean : 1 , Measurement s of the 

distri bution . J. Geophys. Res . 70 :6087-6097 . 

48 
Kerman , B., 1984. A model of interfacial gas transfer for a well-roughened 

sea . ~ Geophys . Res. 89:1439-1446. 

Komhyr , W. D., L. S. Waterman, and \L R. Taylor, 1983. Semiautomatic 

nondispersive infrared analyzer apparatus for CO 2 air sample canalysis . 

~ .Geophys . Res . 88(C2):1215-1322. 

Komhyr , W. D. , R. H. Gammon, T. B. Harris, L. S. Waterman, T. J. Conway, W. R. 

Taylor , and K. W. Thoning , 1985. Global atmospheric CO 2 distribution and 

variations from 1968-1982 NOAA/GMCC flask sample data. J. Geophys. Res. 

90(D3) :5567-5596 . -

Machta , L., 1974. Global scale atmospheric mixing. Turbulent Diffusion in 

Environmental Pollution, F. Frenkiel and R. E. Munn (eds.), Academic 

Press , New York , 33 56. 

Mahrbach , C., C. Culbertson, J . Hawley , and R. Pytkowicz, 1973. Measurement 

of the apparent dissociation constants of carbonic acid in seawater at 

atmospheric pressure. Limnol . Oceanogr. 18:897-907. 

Mook , W. G., A., M. Koopmans , A. F. Carter, and C. D. Keeling, 1983 . 

Seasonal, latitudinal , and secular variations in the abundance and 

isotopic rati os of atmospheric carbon dioxide: 1, Results from land 

stations . ~ Geophys . Res. 88(C15):10,915-10,933 . 

Ramanathan, V. , R. J . Cicerone , H. B. Singh , and J. T. Kiehl, 1985. Trace gas 

trends and their potential role in climate change . J. Geophys. Res . 

90(D3):5547 - 5566 . 

Reinsch , C. H. , 1967 . Smoothing by spline functions. Numerische Mathematik 

10 : 177- 183. 

Roos , M. and G. Gravenhorst , 1984 . The increase in oceanic carbon dioxide and 

the net CO 2 flux into the North Atlantic . J. Geophys. Res. 89 : 8181-

3193 . 

Rotty , R., 1982 . Distr ibution of and changes in industrial carbon dioxide 

production . Rep . ORAU/IEA-82-2(M), Oak Ridge Associated 

Universities/Institute for Energy Analysis , Oak Ridge, TN , 23 pp. 

Siegenthaler , U., and K. 0 . Mlinnich , 1981 . 13C/ 12C fractionation during CO 2 transfer from air to sea . Carbon Cycle Modeling , SCOPE~ , B. Bolin , 

(Ed . ) , John Wiley and Sons , New York , 249-257 . 

Steele , L. P., P. J . Fraser , R. A. Rasmussen , M. A. K. Khalil , T. J. Com-lay , 

A. J. Cr awfor d , R. H. Gammon , K. A. Masarie , and K. W. Thoning , 1985 . The 

global di stribution of methane in the troposphere . Submitted to J . Atmos . 

Chern . 

49 
Takahashi, T., D. Chipman, T. Volk , 1982 . Geographical , seasonal and secular 

variations of the partial pressure of CO2 in surface waters of the oceans: 

the results of the North Atlantic TTO program. Proceedings of CO 2 Research Conference , Berkeley Springs , WV, 19-23 September 1982 , CONF820970 , U. S. Dept. Energy, Washington, D.C. 

Tans , P. , 1981 . 12C/ 12C of industrial CO 2, Carbon Cycle Modeling , SCOPE~ , 

B. Bolin (ed . ) , J . Hiley and Sons, New York , 127-129 . 

Weiss, R., 1974 . 

non- ideal gas . 

Carbon dioxide in water and seawater ; The solubility of a 

Mar . Chem . 2:203-215. 

Weiss , R. F., 1981. Determinations of carbon dioxide and methane by dual 

catalyst flame ionization chromatography and nitrous oxide by electron 

capture chromatography. J. Chromatogr. Sci. 19 : 611-616 

50 
5. TRACE GASES GROUP 

5.1 Continuing Programs 

TOTAL OZONE 

Routine 

during 1984 

(Table 1). 

cooperative 

the N\~S. 

total ozone observations were made with Dobson spectrophotometers 

at 14 stations that comprise the U.S. total ozone station network 

Of the 14 stations, 4 are operated by GMCC personnel; 3 are foreign 

stations; 3 are domestic cooperative stations; and 4 are operated by 

Table 1.--U.S. Dobson ozone spectrophotometer station network for 1984 

Station Period of record Inst. No. Agency 

Bismarck, NO 01 Jan 1963-present 33 NOAA 

Caribou, ME 01 Jan 1963-present 34 NOAA 

SMO 19 Dec 1975-present 42 NOAA 

Tallahassee, FL 02 May 1964-present 58 NOAA; Fla. State Univ. 

Nashville, TN 01 Jan 196 3-present 79 NOAA 

SPO 17 Nov 1961-present 80 NOAA 

Wallops Is, VA 01 Jul 1967-present 86 NOAA; NASA 

Huancayo, Peru 14 Feb 196 4-present 91 NOAA; Huancayo Obs. 

Fresno, CA 22 Jun 1983-present 94 NOAA 

Boulder, CO 01 Sep 1966-present 61 NOAA 

Poker Flat, AK 06 Mar 1984-present 63 NOAA; Univ. of Alaska 

MLO 02 Jan 1964-present 76 NOAA 

Perth, Australia 30 Jul 1984-present 81 NOAA; Aust. Met. Dept. 

Haute Province, France 02 Sep 1983-present 85 NOAA; Obs. Haute Pray. 

Daily 1984 total ozone amounts applicable to local apparent noon, for stations in the U.S. Dobson instrument ne twork, have been archived by the World 

Ozone Data Centre, 4905 Dufferin Street, Downsview, Ontario M3H5T4, Canada, in 

Ozone Data for the World. Table 2 lists provisional monthly mean total ozone 

amounts for 1984 for the NOAA observatories and cooperative stations. 

51 
Table 2.--Provisional 1984 mean total ozone amounts (milli-atm-cm) 

Jan Feb i'1ar Apr Hay Jun Jul Aug Sep Oct Nov Dec 

Bismarck, ND 351 377 391 371 364 340 315 298 304 290 300 310 

Caribou, ME 363 390 428 407 379 360 343 332 321 304 324 315 

SHO 254 254 249 254 258 262 262 260 265 265 270 276 

Tallahassee, FL 312 309 325 340 341 334 330 326 301 284 280 271 

Boulder, CO 329 348 366 36 1 328 321 304 299 290 303 296 297 

Poker Flat, AK 431 423 419 368 328 307 301 291 

MLO 249 273 264 301 290 277 277 274 269 262 244 246 

Nashville, TN 326 358 374 381 369 355 347 333 310 293 305 274 

SPO 304 216 271 303 

Perth, Australia 337 322 341 324 311 294 

\lallops Is, VA 338 352 367 371 361 343 326 317 300 282 293 275 

Haute Province, 373 360 400 38 1 40 1 366 326 330 320 300 296 312 

France 

Huancayo, Peru 258 258 250 252 242 238 248 255 259 259 258 252 

Fresno, CA 317 331 345 365 333 344 319 311 298 297 287 309 

NESDIS has designated a select set of 16 Dobson instrument stations whose 

total ozone data will be used for validation of SBUV ozone data obtained aboard 

the NOAA F satellite (and similar satellites to be flown in the future). The 16 

select stations are shown in Tahle 3. In a cooperative endeavor, with funding 

provided by NESDIS, NOAA/GMCC has agreed to maintain the Oobson instruments at 

these sites highly accurately calibrated. Calibrations of each instrument will 

be performed at intervals of 3 to 4 years. The calibrations will be performed 

relative to primary standard Dobson instrument No. 83 which is maintained as the 

world total ozone standard by NOAA/GMCC in Boulder, Colorado. 

Table 3.--Select NESDIS Dobson instrument stations 

Arosa, Switzerland 

Boulder, USA 

Edmonton, Canada 

Goose Bay, Canada 

Huancayo, Peru 

Haute Province, France 

Invercargill, New Zealand 

Mauna Loa, USA 

Melbourne, Australia 

New Delhi, India 

Perth, Australia 

Poker Flat, USA 

Pretoria, South Africa 

Sapporo, Japan 

Tateno, Japan 

Varanasi, India 

As part of the calibration effort, NOAA/GMCC personnel conducted an international comparison of Dobson ozone spectrophot ometers , sanctioned by the l;MO, 

and hosted at Melbourne, Australia by the Australian Bureau of Meteorology, 

52 
November 19 to December 8, 1984. Countries, instruments, and scientists that 

participated in the comparisons are shown in Table 4. Instruments 105, 112, and 

116 are operated, respectively, at Melbourne, New Delhi, and Tateno. Earlier in 

the year (August), R. D. Grass spent 3 weeks in Melbourne training Australian 

technicians in optically aligning, calibrating, and operating Dobson spectrophotometers. At that time major optical adjustments were performed on instruments 

111 and 115. 

Table 4.--International Dobson spectrophotometer comparison participants 

Country Instruments Participants 

Australia 105, 111 , 115 J. Easson, D. Jenkins, 

S. Townsend 

India 112 K. Chatterjee 

Japan 116 R. Kajihara 

New Zealand 82 E. Farkas 

USA 83 R. Grass, \, . Komhyr 

Work was performed on several other Dobson instruments during 1984. New 

Zealand (Invercargill) Dobson instrument No. 17 was rebuilt and re-calibraten 

after having been in a flood. Boulder instrument No. 61 was re-calibrated. And 

instrument No. 81, that had been on loan to Australia, was re-called early in 

1984, automated, calibrated, and re-installed at Perth, Australia in July for 

total ozone and Umkehr observations. 

OZONE VERTICAL DISTRIBUTION 

In late 1984, funding was obtained from NESDIS to conduct ozonesonde observations at 3 stations and Umkehr observations at 5 stations to obtain atmospheric O7.one vertical distribution data for validation of SBUV ozone data 

obtained aboard the NOAA F satellite. The ozone sonde observations are made with 

balloon-borne ECC (electrochemical concentration cell) instruments (Komhyr, 

1969), and the Umkehr observations are made with automated Dobson spect rophotometers (Komhyr et ai., (985). 

Weekly ECC ozonesonde flights began at Boulder, Colorado, and Hilo, Hawaii, 

in January 1985. The sounding program was expanded later in 1985 to include 

observations at Edmonton, Alberta, in a cooperative endeavor with the Canadian 

Atmospheric Environment Service. 

53 
A list of the automated Umkehr observatories, operating in 1984, is given in 

Table 5. Stations yet to be implemented are: Huancayo, Peru (l2°S, 76°W); 

Pretoria, South Africa (16°S, 28°E); and Lauder, New Zealand (45°S, 170 0 E). 

Table 5.--Automated Dobson spectrophotometer Umkehr observatories 

Station Lat. , Long. Date observation began 

Boulder, Colorado USA 40 0 N, 105°W 1-14-82 

Haute Province Observatory, 

France 44°N, 6°E 9-02-83 

Mauna Loa Observatory, USA 20 0 N, 156°E 3-12-84 

Perth, Australia 32°S, 116°E 7-26-84 

Poker Flat, USA 65°N, 148°W 3-05-84 

Tests on ECC ozonesondes were continued in 1984 to assess their performance 

in the troposphere and at altitudes between 30 and 40 km. Eight ECC sondes were 

flown in March 1984 (Hilsenrath et a1., 1985) from Palestine, Texas, aboard a 

balloon gondola carrying, also, Canadian and NASA Wallops Island ECC sondes, 

as well as UV ozone photometers from Harvard University, NOAA/AL, NASA/JSC, and 

NASA/GSFC. Additionally, ECC ozonesondes were flown at Palestine in March and 

October 1984 aboard a University of Minnesota balloon gondola that measured 

water vapor and ozone with a mass spectrometer. 

Results of comparison ECC soundings made to nearly 40 km altitude in 

September 1983 at Aire-Sur-L'Adour, France, during the MAP/GLOBUS campaign are 

shown in Figure 1. Total ozone amounts deduced from the ozone profiles were 265 

and 266 milli-atm-cm, respectively, for instruments 4Al031 and 4Al042. The 

total ozone amount measured that morning with Dobson spectrophotometer No. 85 at 

Haute Province Observatory, located 470 km to the east, was 371 milli-atm-cm. 

:0 

.s 

5 

10-

20-

• 50 , 

• • 

0. • 100 

200 

500 

Sept. 24, I!lS) 

-- 4"1031 

••••• - . ,,10H 

5 

-<0 

35 

-JO 

-10 

-5 

10 

Oz.one Pallial Pressure (nb) Ozono Mixing Rallo (ppmv) 

Figure 1.--0zone profiles measured by 

a pair of ECC sondes in Air-Sur-L'Adour, 

France, during the Map/Globus Campaign. 
SURFACE OZONE 

The four-station GMCC surface ozone network operated throughout 1984. All 

of the station Dasibi ozone monitors were compared with the network standard 

instrument during the year. The return of Dasibi meter serial number 1316 from 

South Pole allowed for correction of data from this location back through 1981. 

The monthly mean data (Fig. 2) presented here supercede previously published 

results. Analysis of the surface ozone data through 1984 was completed with 

particular attention given to secular trends in the data. To investigate the 

long-term tre nds, seasonal cycles were removed from the monthly means by 

subtracting monthly normals to give the anomalies shown in Fig. 3. Included in 

Fig. 3 are least squares linear regression line fits to the data, along with 

calculated slope and 95% confidence intervals, in percent ozone change per year. 

10 · 

5~~~~~~~~~~~~ 

30 -

25 -

20 

15 

10 -

5 

0 

30 

25 -

20 

15-

10 

5· 

0 

73 

spo 

" B N 77 N n ® 81 ~ a M 

YEAR 

Figure 2.--Monthly mean surface ozone 

pressures at the GMCC observatories 

obtained from measurements with ECC 

ozone meters ( ••••• ) and Dasibi ozone 

monitors ( ). 

55 

,;;-

~ 

< 

~ 

0 

Z 

< "-

~ 

w 

:; 

< 

0 • 

Z 

< 

w 

Z 

0 

N 

0 

W 

U 

~ ~ 

~ 

~ 

,,'r-~~-'- '''-----''-'T --~-'r--r- "'_.,-

II· HRW 

6 • 

· . 

-, - -, 

-m 

6 MLO 

• 

1 

0 .. 

-1 

-. 

-6 (I 37:tO.61)% y, _1 

-. 

• SMO 

1 

0 .............. 

-, 

-. 

-6 

• SPO 

1 

-1 . 

-.. 

-6 ' , 

13 14 IS 16 11 78 19 GO 81 82 83 8C 

YEAR 

Figure 3.--Surface ozone anomalies 

(departures from monthly normals) at 

the GMCC observatories. Solid lines 

are linear least squares fits to the 

data. The printed values are linear 

trends with 95% confidence intervals, 

in percent per year. 
The significant increase at BRW is a summer and autumn phenomenon, while at 

MLO the positive growth rate is strongest during the winter but still significant during the spring. In the Southern Hemisphere the overall decreases are 

not significant hut a significant negative trend does appear during the summer 

months at hoth 51-10 and SPO. 

Based on the general circulation model calculations of Levy et al. (1985), 

it appears that the winter and spring ozone rise each year in the troposphere at 

MLO is associated with the large buildup in ozone over the North Pacific. This 

strongly suggests that the long-term increase in tropospheric ozone since the 

late 1970' s during these months may be tied to circulation changes and the subsequent altered transport by the circulation. Evidence for such circulation 

changes in the vicinity of Hawaii has been presented by Namias (1985). The role 

of anamolous circulation patterns may be evident in the very high surface ozone 

amounts observed at MLO in 1983 coinciding with the particularly strong ENSO 

event. 

At Barrow during 1984 both the highest (November) and lowest (April) monthl y 

means were recorded in the 12 years of observations. As can be seen in Fig. 2 

the January-May 1984 period ozone amount (18.6 nb) was well below the 12-year 

normal (24.8 nb). In 1984, both February and April had the lowest values 

recorded for the months, while October and November had the highest values 

measllred for those months. Departures from normal of this magnitude are most 

likely associated with anomolous circulation patterns. 

STRATOSPHERIC WATER VAPOR 

Ten stratospheric water vapor profiles were obtained in Boulder in 1984. 

Two sound ings were also obtained at Laramie, \,yoming in November as part of the 

data validation program of the SAGE II satellite measurement system. 

Stratospheric mixing ratio profiles for the soundings in Boulder in 1984 are 

shown in Fig. 4. The lower stratospheric spring minimum in mixing ratio is very 

pronounced as seen especially in the April sounding. 

As noted last year (Harris and Nickerson, 1984) the annual cycle in water 

vapor at 50 mb is small and thus this level is particularly useful in monitoring 

long-term chang es. It has been no ted prev iously (Mastenbrook and Oltmans, 1983) 

that there appears to be a relationship between tropical stratospheric winds and 

water vapor at 50 mb at mid-latitudes of the Northern Hemisphere. This relationship is observed in Fig. 5 where the smoothed water vapo r and tropical winds 

are shown as the top and bottom curves, respectively. Also shown are the total 

ozone at Mauna TAa which exhibits a marked quasi-biennial oscillation (OBO), and 

temperatures near the tropopause and in the stratosphere at Ponape (7°N). The 

eruption of El Chichon in 1982 does not appear to have greatly altered the QRO 

wind oscillation at Ponape but had a marked effect on the temperature. The temperature increase at 100 mb appears to be especially pronounced. Based on the 

previously noted relationship of low water vapor mixing ratios associated with 

westerly tropical stratospheric winds it might have been expected that 1983 

would have been a year of relatively lower water vapor amounts. In fact they 

are not much different from the 1982 and 1984 levels. This may be a confirmation of the role of the tropopause in the tropical western Pacific in 

56 
• < . · 'Q ~A" 111 ' .. H~Il'T l,."lf'" .n"1 1,,.11 &'1 S:""I!'1 , ;:~~?o; 11~~~"'i : 'nO 'I'~ 1.'<0'"11'1 

} 

• ) I 

f-

• 

· 

.. 1/ I 

.. \ I "\ I 

"- "-

I ~ 1 ( 

1"--- 1\ " -- \ 

-. , , \ ~ • , , , , , , 

Figur e 4.--Profiles of stratospheric mass mixing ratio in ppm at Boulder, 

Colorado for 1984. Numbers a l ong the top of the plot for the first water 

vapor profile ar e volume mixing ratios in ppm. 

- C./fll..0 • VC ,~ .. , 

) Iv II 

· I'll ~- v '" -::;; :::;;:::; 

; \ 

- ' .... ,.,l , " , "" 1\ !\ , 

\ ~ (' - f\ 

· v ~ 'v \J J\ { , 

, 

, 

· """ ,~ ''''''" "" 1\ " j 

· 

/" ", ~ 

V \.. r '- .", v , 

· f\ ,-, '" T(J .. ~n "" " I,U · 

\ f' I ~ V 1/\ II \ 1/'\ 17 \] \J -'\ , 

"m , r '" "'" ". 

1\ 1\ (\ ( r\ - 1\ (I 1\ · I- +- \ V \ 

-

, 

' j\J ~ I V 

.. , , I I I I .. M "M "" , .. ,. " ,. .. . " " .. " ... "'" Figure 5.--Smoot hed anomalies of wate r va por , ozone, t empe r a ture and 

wind s. 

57 
controlling the flux of water vapor into the stratosphere. Because of the high 

tropopause temperatures in the western Pacific the temperature of air entering 

the st ratosphere would be warmer and moister than normal, thus counterbalancing 

the expected QBO effect on stratospheric water vapor over Boulder. 

HALOCARBONS AND NITROUS OXIDE 

Pair flask air samples continued to be collected weekly at BRI~, NWR, MLO, 

and SMO, during 1984; and biweekly at SPO during January, November and December 

1984. Sample analyses, for CCI 3F, CCI 2F2, and N20 concentrations continued to 

be made on a gas chromatograph in Boulder. From 1 January through IS October 

1984, a Shimadzu mini-2E gas chromatograph was operated at SPO, with CCI 3F, 

CCl 2F2 and N20 analyses made twice weekly. During October, calibration gas in 

cylinder 3081 was inadvertently lost, so that measurements could not continue. 

A new r efe rence gas tank (No. 3083) was sent to SPO in early November, but did 

not arrive there until late December. 

An addit lonal Shimadzu mini-2E gas chromatograph was procured and set-up in 

Boulder for training and as a spare instrument. A power supply, temperature 

controller, and electrometer assembly were also procured and sent to SPO as 

spare parts. 

With the eruption of Mauna Loa volcano and the subsequent loss of power at 

MLO, the sample collection location was transferred to Mauna Kea observatory 

during April 1984. 

CCI]F, CCI 2F2 , and N20 data for 1973 to 1979 were archived in 1984 at the 

National Climate Data Center in Ashville, NC. A NOAA Technical Report (Thompson 

et al., 1985) describes in detail the sampling and analysis program since its 

inception in 1973, and presents all as well as selected data. 

Selected CCl3F, CCl 2F2 , and N20 data for 1977 through 1 September 1984, for 

the NOAA/GMCC baseline stations and Niwot Ridge (NWR) , Colorado, are shown in 

Figs. 6, 7 and 8. Solid lines fitted to the data are least squares linear 

r eg ressions. Errors associated with indicated growth rates are 95% confidence 

intervals. All concentrations shown are expressed in the Oregon Graduate Center 

CCI3F, CCI 2F2 , and N20 calibration scales (Rasmussen, 1983). Results for N20 

are tentative, since analyses of the air samples for N20 may have been adversely 

influenced by atmospheric CO 2 , The extent of the C02 interference has yet to be 

determined. 

January 1 CCl 3F and CCl2F2 concentrations for 1978 through 1984, derived 

from the linear regression analyses, are shown in Table 6. Because the growth 

rates of these two trace gases has remained nearly constant in recent years, the 

Northern Hemisphere/Southern Hemisphere annual concentration differences for 

CCl 3F and CCl2F2 have decreased by about a factor of 2 during 1978 to 1984. 

Preliminary analysis of the data have yielded a best estimate atmospheric 

life-time for CCl3F to be 79.9 year, and that for CCl 2F2 94.8 years. Taking 

into account systematic errors in estimates of release rates of these halocarbons, and systematic and random concentration measurement errors, the 

atmospheric lifetimes for CC13F and CCl 2F2 are calculated to range from a minimum of 35 years to a maximum of ~ years. 

58 
V1 

'" 

"','---, __ --r---~::~"-__ --__ --,___, "'C'" '" '" 1M .. ' .. ~ 160 ...... "':r."'~...--~ I~ D • 

120 1 9.29:t 0.16 PP1V/YR 

!~~~ NWR 

'" 

"'1 ,

:::: ,, ~~~ 2M ,,, j 961 :I: 0032 I>Prv/yR 1 

., "'Leo b: 220 

!h 200 § u.. l,,, eo .. ~,,-~-..p.- 140 .~ 9.5" * 0.\6 r>PTVfYR ,,, '240 " SMO 

~;: ~ .. :. 180 • '. 

160 . " . • 

,,, ~==;:=;:=;:::=::::IO=.O=~'='=. :5="'=<V~/="'=~ ,,, 

260 1 

240-1 SPa 

;: 

:~ ..... . 

.... 

~ 

~ 

," 

140 ~ . '<).37 ± 1.00 pprvjYR 

I~ 77 n n M 81 82 8J ~ 

Figure 6.--Selected CC1

3F data 

obtainerl from chromatographic 

analyses of pressurized air 

samples collected in pair 

flasks. 

~2°1 SRW 

'" ~-.:..~ ., '" , .. JOOJ 

'" 16.12 .t O.~O pprV/YR 

'" 

~2°1 NWI'l 

'" '" '" '" 11

.61 J:. 0.62 pprvjYR 

'" 

S' "'-0 4'0 

h: J80 

12:.- J40 ,;: '" 

. .... ~~-/."#-' 8 '" . "".i,:,;r~~- . " .... '" 1<190:1: 0 

20~ . .J7 pprv/YR 

5"0 

'" "'l JOO .. 

~~. - 1 2tD 

220~ .. 17.55:1: 0.2l PPTV/yR 

420i SPO 

,., '" 

'" 

'" va, 

1<='. III 61 t 1.25 Pf'rv!yj;I 

, 77781'i8081828J84 

Figure 7.- -Selected CC1

2F2 data 

obtained from chromatographi c 

analyses of pressurized air 

samples collected in pair 

flasks. 

», 

J20 1 BRW 

'" '" I ~ ... ; :~ .~: ,,~""" '.-' 

,go 

280 1 0.95 t 0.07 PPBV/YR 

m 

"T~ ,. 

'" ..I .... ..:....;p.:~:~ 

,go 

280 1 !.19:1: 0.15 PPBV/YR 

m 

no 1 ~lO f 'lOj 9: JOOH~': .... :.: .::~:'~.;.4~ z 290 .. 

2110 J 12 "to. 

J20 SMO . --"~ · 

'" '" .~.i.kc"" .~. .. ..~ ... ,,:_.,;:;, ... ...,,;~ ,go 

1110 1 1.52 * 0.10 PP8V!YR 

JJO I ' 320 SPO 

'" 

JOO 

J .. . . .... l r ,go 

280 I l06 * 0.1' PI>Ov<m 71 7e 79 M 11 1 e2 8J e. 

Figure 8.- -Tentative, selected 

N20 data obtained from chro-

matographic analyses of pres-

surized air samples collected 

in pair flasks. 
Table 6.--CCI 3F and CCl 2F2 Northern Hemisphere, Southern Hemisphere, 

and Global concentrations* in PPTV 

Year N.H. S.H. Globe % Diff: NH-SH 

1979 281. 5 ± 1.1 264.5 ± (6. 1) 273.0 ± (3.6) 6.2 

1980 297.4 ± 1.0 282.3 ± (5.2) 289.8 ± (3.1) 5.2 

1981 313.4 ± 0.9 300.0 ± (4.2) 306.7 ± (2.6 ) 4.4 

1982 330.1 ± 1.0 317.2 ± (3.3) 323.7 ± (2. 2) 4.0 

1983 346.2 ± 1.1 335.0 ± (2.5) 340.6 ± (1.8) 3.3 

1984 362.9 ± 1.2 352.3 ± 1.8 357.6 ± 1.5 3.0 

1978 154.2 ± 0.8 145.0 ± 1.0 149.6 ± 0.9 6.2 

1979 163.6 ± 0.7 155.0 ± 0.9 159.3 ± 0.8 5.4 

1980 173 .4 ± 0.6 165.0 ± 0.8 169.2 ± 0.7 4.9 

1981 182.6 ± 0.5 175.0 ± 0.8 178.8 ± 0.7 4.3 

1982 192 .2 ± 0.4 184.9 ± 0.7 188.6 ± 0.6 3.9 

1983 201.8 ± 0.5 194.9 ± 0.9 198.3 ± 0.7 3.5 

1984 211.0 ± 0.6 205.0 ± 1.5 208.0 ± 1.1 2.9 

*Concentrations are given for 01 January of each year, derived from least 

squares linear regression fits to the data. Indicated unce rtainties are 95% 

confinence interval measurement errors. 

5.2 References 

Harris, J. M., and E. C. Nickerson (eds), 1984. Geophysical monitoring for 

climatic change, No. 12: Summary Report, 1983. NOAA Environmental Research 

Lahoratories, Boulder, CO, lR4 pp. 

Hilsenrath, E., J. Ainsworth, A. Holland, J. Mentall, A. Torres, W. 

Attmannspacher, A. Bass, Ii. Evans, Ii. Komhyr, K. Mauersberger, A. J. Miller, 

M. Proffitt, D. Robbins, S. Taylor, and E. Weinstock, 1985. Results from 

the balloon ozone intercomparison campaign (BOIC). In Atmospheric Ozone, 

Proceedings of the Quadrennial Ozone Symposium held in Halkidiki, Greece, 

3-7 September 1984, D. Reidell, Dordrecht, Holland, 454-459. 

Komhyr, W. D., R. Tl. Grass, R. D. Evans, R. K. Leonard, and G. H. Semeniuk, 

1985. Umkehr observations with automated Dobson spectrophotometers. In 

Atmospheric Ozone, Proceedings of the Quadrennial Ozone Symposium held in 

Ha lkidiki, Greece, 3-7 September 1984, D. Reidel, Dordrecht, Holland, 

371-375. 

Komhyr, W. D., 1969. Electrochemical concentration cells for gas analysis. 

Annales de Geophysique 25(1):203-219. 

Levy II, H., J. D. Mahlman, W. J. Maxim, and S. C. Liu, 1985. Tropospheric 

ozone: the role of transport. Journal ~ Geophysical Research 90:3753-3772. 

60 
Mastenbrook, H. J., and S. J. Oltmans, 1983. Stratospheric water vapor variability for l~ashington, DC/Boulder, CO: 1964-82. Journal ~ Atmospheric 

Science 40(9):2157-2165. 

Namias, J., 1985. Remarks on the potential for long range forecasting. 

Bulletin ~ the American Meteorological Society 66:165-173. 

Rasmussen, R. A., and J. E. Lovelock, 1983. The atmospheric lifetime experiment; 2. Calibration. Journal of Geophysical Research 88:8369-8378. 

Thompson, T. M., W. D. Komhyr, and E. A. Dutton, 1985. Chlorofluorocarbon-II, 

-12, and nitrous oxide measurements at the NOAA/GMCC baseline stations ( 16 

Septemher 1973 to 31 December 1979). NOAA Technical Report ERL 428-ARL-8 

124 pp. 

61 
6. ACQUISITION AND DATA MANAGEMENT GROUP 

6.1 Continuing Programs 

STATION CLIMATOLOGY 

Introduction 

The interpretation of measurements of trace gases, aerosols and 

atmospheric turbidity, including an assessment of the influence of local 

pollution sources , requires the measurement of ancillary meteorological 

variables including wind direction, speed, station pressure, air temperature 

and moisture content. Where appropriate, common, off-the-shelf 

instrumentation was chosen and WMO-recommended exposure standards were used . 

Table 1 contains the serial number and altitude or elevation of each 

instrument as of December 1984. At this time the new instrumentation control 

and monitoring system (CAMS) had been installed at each station . 

With the installation of the CAMS to manage the meteorological data, a 

number of changes were made to the measurement and reporting of meteorological 

conditions. Specifically a second thermometer was added at the top of the 

sampling tower to measure the gradient in the boundary layer. At those sites 

where a representative temperature gradient can be measured, BRW , MLO and SPO, 

this measurement will be used with the surface wind to determine the bulk 

Richardson Number. On request, the CAMS also supplies a complete listing of 

the hourly average values for the previous 24-hr period. This is used in 

conjunction with a daily observation to monitor data quality. A CAMS system 

was installed in BRW in August, SMO in October, SPO and MLO in November . This 

period also marked the end of a 2-year project to recalibrate all the sensors 

in the network. The serial numbers reported in table 1 represent new or 

recalibrated instrumentation. The listing of sensors in the GMCC Summary 

Report for 1983 (Harris and Nickerson, 1984) describes the complement of 

sensors as they were up to the time the CAMS were installed With one 

exception, platinum resistance thermometers (Yellow Springs Inst. Co . ) were 

used at SPO throughout 1984 . 

Hourly average values, scaled in metric units, are processed, checked for 

quality and reported for each measurement listed in table 1. The values are 

stored on microfiche and magnetic tape. The microfiche listings are organized 

by station, date, time and variable . The files are usually available 6 to 9 

months after the end of the year. 

Barrow 

A description of the Barrow site, its surroundings, and climatology can 

be found in previous GMCC Summary Reports. Wind roses of the hourly average 

resultant wind direction and speed are presented in 16 direction classes and 4 

speed classes. The wind rose for 1984 shows significant deviations from the 

1977-1983 period average (fig. 1). The predominant wind direction is 

northeasterly for 1984 as opposed to north-northeasterly for the longer 

term. At the same time, easterly winds (NE -SE) occurred 50% of the time in 

1984 as compared with 61% for the previous 7 years. This is consistent with 

deviations observed in 1983. The main differences are in the relatively large 

occurrence of winds in the northeasterly and southwesterly direction. 

62 
Table 1.--GMCC meteorological sensor deployment 

Sensors 

Primary Wind 

Aerovane* 

Station Pressure 

Pressure 

transducert 

Mercury barometer 

Air Temp. A 

Lineari zed 

thermistors' 

Air Temp. B tt 

Linear i zed 

thrmistors 

Air Temp. C 

L1near 1 zed 

thermistors 

Dew Poi nt Temp. 

Dew point 

hygrometerH 

BRW 

serial 

No. 

576 

2366 

641 

2 

4 

7162 

elev 

(m) 

16.7 

9 

2.5 

15.3 

N/A 

2.5 

serial 

No. 

931 

MLO 

elev 

(m) 

8.4 

109 3397 

278 3397 

10 1 .6 

11 1.6 

N/A 

182 1.6 

serial 

No. 

782 

752 

8 

7 

9 

592 

SMO 

elev 

(m) 

13.7 

30 

30 

9 

2.3 

I ~ 

2.3 

I ~ 

9 

SPO 

ser i al 

No. 

585 

1 1 7 

703 

704 

836 

N/A 

'Aerovane, serial no. 141, Bendix, Inc . Environmental Science Div., 

Baltimore , MD. 

elev 

(m) 

12.2 

2841 

2841 

2.0 

" 

23.2 

-0 . 1 

tPressure transducer , serial no . 1201F1B , Rosemount , Inc. Mineapol i s , MN. 

IThe altitude of the instrument above MSL is reported . 

~Linearized thermistors, serial no . 44212 , Yellow Springs Inst . Co . , Yellow 

Springs, Ohio . 

"Platinum resistance thermometers , SIN 139AP, Yellow Springs Inst . Co., 

Yellow Springs, Ohio. Installed in a naturally ventilated radiation shield 

no. 43103C , R. M. Young Co ., Traverse City, Michigan . 

t t This thermometer is positioned at the top of the local sampling tower to 

facilitate an estimation of boundary layer stability . 

IIThiS thermometer is used to measure the air temperature under the 

photovoltaic arrays . 

~~General Eastern model no. 1200 ASP , General Eastern Instrument Co ., 

Watertown, Massachusetts, an E.G. & G. model no. 911 , E.G. & G. Newt on, 

Massachusetts at SMO. 

63 
Referring to table 2, the deviation from the NE direction occurred primarily 

during the winter and spring months . In 1984, 17% of the wind speeds were 

equal or greater than 10 ms- 1 in comparison to a long-term average of about 

9%. The maximum wind speeds in August, September, October and December 1984 

equal or exceeded the previous 7-year average. The December 1984 value of 

24 . 8 ms- 1 is almost equal to the 25.0 value measured in December 1983. 

il .. 'kkS-,\ 

19B-; 

II 

\ 

I 

111-'0 r Rt:Q 

B,\RRQII" 

77-83 

\I 

;\::> '·""T::.(II -

- ~ ... ~ ~ 

c ... ::! ~ s . , 10 

'o ! ~ 10 

N '11'[:->0 ROSE 

f: I 

I 

Figure 1.--Wind rose of surface winds for BRW for (left) 1984 and (right) 

1977-1983. The distribution of the sesultant wind direction and speed are in 

units of percent occurrance for the year and 7-year period, respectively. 

Wind speed is displayed as a function of direction in three speed classes. 

The winter and spring of 1984 was significantly colder than normal. The 

average temperature for January was 11°C below the average for the previous 7 

years. A new minimum of -48°C was reported. In February the average was 13° 

below the station average and a newall-time record minimum temperature of 

-50°C was reported. The all-time minimum reported at the NWS station in 

Barrow is -49°C. The warmest temperature reported in February was only 

-24°C. March through June were also significantly below normal. This 

condition in BRW is consistent with a substantially colder than normal spring 

observed over the continental U.S . (Wagner, 1985) . The average temperature 

for the year was almost 4°C below normal. For the first time, table 2 

contains the dew point measurements. All frost pOints have been converted to 

dew pOint. Too many periods of prolonged outages due to instrumentation 

problems have precluded the inclusion of this data in the past. The average 

pressure for the year was 1015.9 mb which is 2.7 mb above the 7-year 

average. 

64 
Table 2.--BRW 1984 monthly cl imate summary* 

Jan ro. ~a{' 'pe ~Jay Jw> JuJ 'U, 5" Oct Uov Joe 1984 

Prevailing ' ... ind )IE SW :~E SW 5S .... :;E SW W , ENE :IE :::IE liE direction 

Average wind 7.1 6.1 6. 8 5.6 6.S 5. 7 5.8 6. , 6.6 8. 7.8 7.5 6.8 

speed (1'1 5- 1 ) 

MaxImum wl~d 

(m 5- 1) 

17 1 J 15 1 J 1 J '1 12 • 8 • 9 

" 

20 25 25 

speed t 

01 recti on of 'J 229 70 76 222 1 ~9 2" 2'; 7J 73 50 262 262 · ... indt :deg.) 

A'/erage station 1015.3 1019.8 1022.9 :0Il:i.6 lO ~ 3. 5 1 0' ~ 6 1')09.8 1>. .. J9·3 1015 . .; . )1 S . .: 1015.7 1015.8 1015.9 pressure (mOl 

'1axlmum pressuret 1039 10111 1037 1031 1026 1025 1021 1028 1031 IOU3 1033 1039 10113 

(mo) 

MInlmu:n pressuret 999 1001 1012 1002 1003 I~Ol! 99:' 988 99J 997 989 98' 98' 

(mo) 

Average air -31.1 ,0 -39.2 -30.2 -26.8 -11.7 -1.5 -1. 0 2.2 -0.7 -8.7 -22.5 -25 . 9 -16.8 

ter.lperature (ec) 

Haxlm~~ temperaturet -22 -2' -IJ -12 -J 5 5 1 J 9 2 -9 -5 1 J ( ·e) 

Minimum temperaturet -" -50 -" -'2 -J2 -6 -5 -J ., -22 -JJ -J6 -50 

( Oe) 

Average dew point -J7 -'5 -J9 -J6 -21 -10 -10 -1 -1 -10 -2J -27 -22 

temperature (oC) 

Haxl!!:um dew polntt -" -JJ -21 -22 ·11 -1 -1 8 5 0 -9 -6 8 

temperature ( °C) 

Mlnlrnu!1I del.' polntt -" -50 -'7 -'? -" -15 -16 -1 J ·6 -22 -JJ -J6 -50 

temperature (oC) 

'Instrument heights: wind, 17 m; pressure, 9.5 m (HSL); air and dewpolnt temperature, J m. Wind and temperature 

Instruments are on a tower located 25 m northea:3t of the main bUilding. 

tMaximum and minimum values are hourly averages. 

Mauna Loa 

A description of the MLO site and its climatology can be found in 

previous GMCC Summary Reports. The wind distribution for the period 1977-1983 

(fig. 2) shows a greater frequency of occurrence of southerly winds than would 

be expected from synoptic-scale flow analysis. The effect of the Mauna Loa 

volcano is to redirect stronger, predominately easterly or westerly winds 

aloft, down the slope with a more southerly component. The wind distribution 

for 1984, also shows pronounced deviations with southeasterly direction winds 

occurring in excess of 24% of the year compared to a long-term average of 

about 12%. At the same time the remainder of the southerly components show a 

lower percentage of occurrence than in the longer-term average. The 

distribution of wind speed in four classes in 1984 was similar to the 7-year 

averages. The greatest occurrence of higher winds was in March when 19% were 

equal to or greater than 10 ms- 1 This indicates a series of storms occurring 

in March when most of the southwesterlies are observed . Unlike 1983 when no 

spring storms were reported at MLO and no rain fell between January and March 

1984 a few storms were experienced and a modest amount of precipitation was 

reported in each of the winter and spring months, see table 3. Otherwise the 

average values for wind, pressure, temperature and humidity for the year were 

very close to normal. Bear in mind that in most respects average values are 

not representative of median values due to the bimodel distribution of wind, 

temperature and humidity, dependent upon the time of day or wind direction . 

65 
\1,\1,;:\,\ LOA 

198.; 

IV 

.I~D SPEED(II S) 

_~"9 ~ 

c:::::J~' IO 

c:::J 15 I 10 

WJ:\O ROSE: 

E 

s I 

~1'\ U;\A LO,\ 

77-83 

IV 

• I~O SPITD(1oI. S) 

_ ~i ~ 

c:::::J~"S IO 

c:::J ., I 10 s 

• 

WJND ROSE 

.,SD nll~ 

, 

Figure 2.--Wind roses of surface winds for MLO for (left) 1983 and (right) 

1911-1983. The distribution of the resultant wind direction and speed a re in 

uni ts of percent occurrance for the year and 1-year period . respectively. 

Wind speed is displayed as a function of direction in three speed classes . 

Table 3.--MLO 1 98~ montlhly climate summary* 

Jao Feb l~ar Apr May Jun Jul Aug S'p Oct Nov O,c 19811 

Prevailing o .. ind SE SE SSW SE SE SE SE SE SE SE SE SE 

direction 

Average .... ind 5.3 5.9 6.1 5.2 5.6 ".3 3.6 3. 2 U ".9 5.6 ".9 

speed (m s-l) 

:1aXimum wind '" 13 15 15 '" 15 11 " '" '" 15 

speedt (m s-l) 

Direction of max. 205 195 197 ,"2 13" 131 13" ,"5 135 122 136 131 ... indt (deg . ) 

Ave:-age station 680.9 680.3 681.5 682.2 682.5 681.7 682 .1 681 .7 682.7 682 5 678.6 681.6 

pressure (mb) 

MaXimum pressuret 685 683 686 686 686 685 686 685 686 685 683 686 

(lOb) 

Minimum pressuret 675 676 674 679 680 679 079 679 680 680 675 67' 

(mb) 

Average 311' ". " '.7 6.9 7. , 10.2 7.7 8.7 7. , 7. , 6. 2 ". 3 6.9 

temperature ( Ge) 

Maximum temperaturet 13 '" 17 18 19 15 18 18 18 '" '" 19 

( Ge) 

Mlnlmun temperaturet -2 -3 0 -1 -1 3 0 -3 -3 

( Ge) 

Average dewpolnt -10.0 -15 . 7 -16.5 -11.0 -111 . 8 -7.1 -8 . 2 -6.7 -5.8 -5.0 -5.0 -9.9 

temperature ( Oe) 

Maximum dewpointt 6 5 5 5 8 8 8 8 8 8 5 8 

temperature ( Gel 

MInimum dewpolntt -29 -32 -36 -33 -34 -33 -33 -28 -31 -25 -21 -36 

temperature (Oe) 

Precipitation (mm) 10 7 9 6 0 10 27 17 " '0 35 183 

-Instrument heights: wind, 10 m, pressure . 3397 m (MSL); air and de .... polnt temperature, 1. 6 m. Wind ,nO temperature 

sensors are located approxImately 15m south .... est of the maIn buIlding on a tower. Pressure sensors or. located In 

the observatory building . 

tMaximum and minimum values are hourly averages. 

66 
Samoa 

Southeasterly winds (ESE-SSE) occurred only 58% of the time in 1984 

compared to an average of 63% for the 1977-83 period. This is an even more 

pronounced decrease when compared to the 72% occurrence in 1983. Part of the 

deficit in the occurrence of southwesterlies was made up by an increase in 

northwesterlies (NVlVI-NNVI) of 18% over the long-term average of 11%, fig. 3. 

The increase in northwesterly wind occurrence is primarily in the first 4 

months of the year and in December. Northwesterly winds occurred a 

significant proportion of February, March and December to constitute the 

prevailing direction for the month, table 4. The unusually high occurence of 

northerly winds in February and March is caused by the presence of the 

intertropical convergence zone (ITCZ) in the vicinity of Samoa for much of the 

period. The ITCZ is not usually found this far south. During the remainder 

of the year the trade wind directions prevail. The average wind speed for the 

year is about 1 ms- 1 above normal, beginning in May and continuing throughout 

the year . The May monthly average wind speed equals or exceeds the long-term 

average for the individual month. This increase coincides with the thinning 

of the vegetation on the eastern extent of Lauagae Ridge. The prevailing 

easterlies would be affected the most. There also appears to be a slight 

shift in the prevailing direction from SSE to SE . A storm in December 

established new maximum wind speed, 19 ms- 1 and low pressure readings, 990.8 

mb for that month. No significant deviations from normal temperatures were 

reported during the year. The 2.7 m of precipitation reported in 1984 was 1 m 

more than that reported in 1983. 

The exposure of the meteorological instrumentation at SMO is 

significantly different from that at other GMCC stations. Since February 

1977 , the anemometer has been located at a height of 13.7 m on a sampling 

S,\ \lO,\ 

\98-1 

II 

\ W['\O ROS~: 

• 

SAMOA 

77-83 

IV 

WI1>D SPEED(II 5) 

_ ~' 5~~ 

c::=::!~' S<LO 

,-----, . , I 10 

N \\"ISO ROSE 

S 

Figure 3 .--Vlind roses of surface wind for SMO for (left)1983 and (right) 1977-

1983 . The distribution of the resultant wind direction and speed are in units 

of percent occurrance for the year and 7-year period, respecti vely . Hind 

67 
Table ~. --SMO 1 98~ monthly cl imate summary 

Jao feb :-'Iar- Ap, I-Aay Juo Jul Aug Sep Oct Nov Dec 198!1 

Prevailing wind SE NW 'IW SE SE SE SE SE SE SSE SSE 11".1 SE direction 

Average Oiind 2.8 2.9 2.9 3. 5 6.6 ~peed {m s-I 8.6 7. 5 5.6 5.7 6. , 5. I 5.0 5· 3 

~aximum.llnd 13 13 10 II 16 

speedt (m 5- 1) 

13 13 12 I' I' 19 19 

Direction of ~ax. 313 326 313 I" 139 .... lndt (des· ) 

1'9 149 136 1'9 155 6 327 327 

Average station 1000.1 999 . 9 1000,11 1001 . 8 1002 . 6 1002.9 

(rnb) 

1003.5 1003.2 100). 5 1002.7 1001.6 997 . 0 1001 . 6 pressure 

Maxlltum pressuret ICOIl 1003 1005 1005 1006 1007 

(rob) 

1008 1009 1008 1007 1005 10011 1009 

Minimum pressuret 991 99' 996 997 999 998 

(nb) 

1000 998 998 998 999 991 991 

Average air 26.6 27 . 7 27 . 2 27.7 27 . ) 26 . 5 25.7 25 . 8 26 . 1 26.0 26 . 8 27 . 1 26 . 1 temperature (ac) 

HaxlmuC) temperaturet 30 32 31 31 29 30 29 29 30 30 31 35 35 (OC) 

Minimum temperaturet 23 23 23 " " (OC) 

2' 23 23 23 22 22 23 22 

Average dewpoint 211.9 25 . 1 25.1 25 . 6 25.2 

temperature ( DC) 

Maximum dewpolntt 28 29 29 28 29 

temperature (OC) 

Minimum dewpolntt 22 22 23 23 22 tempera ture (oe) 

Precipitation (mm) '" 105 30S 19' 162 I II 6' '6 35' "0 13' 613 2692 

tInstrumen t heights: w{nd, 111 m; pressure, 30 m (HSL ) ; air and dewpolnt temperature, 9 m. Wind and teL'lperature sensors located atop Lauagae Ridge, a distance 110m northeast of the station. Pressure sensors are located in the station. tMaxim~~ and minimum values are hourly averages. 

tower atop Lauagae Ridge. In this location the shape of the bluff displaces 

the prevailing trade winds from the southeast to a more southerly direction, 

but there are no major obstacles to the winds from the westerly direction as 

there was at the previous location on the pOint. Temperature is measured at a 

height of 9 m on the same tower. Dew point temperature is measured at the 

same elevation. Station pressure is measured in the main building located 

about 100 m west of the sampling tower. During April 198~, a significant 

amount of vegetation was removed from the bluff to the east of the sampling 

tower. The immediate result of this cleanup was to increase the air flow 

across the upper half of the sampling tower. The missing dew point 

temperatures are the result of instrumentation failure . 

South Pole 

Foll owing a year when the wind speed seldom exceeded 10 ms- 1 , 198~ showed 

a return to normal with 2.5% of the winds reported to be equal or in excess of 

10 ms- 1, fig.~. This is in comparison to the 7-year average of 3. 5%. The 

absence of winds from the contaminated grid southwesterly directions (S 

through W), that make long-term sampling of trace atmospheric constituent 

possible, is clearly illustrated, occurring only 7~ hours in the year . The 

prevailing wind in every month is from the grids northeast quadrant . At the 

spa grid, north is defined as being along the prime meridian. The full extent 

of the austral winter, often termed a iOcoreless winteriO on the Antarctic 

Plateau is evident by the fact that for 8 months of the year the monthly 

average temperature is below the annual average . Regardless , the average for 

198~ of -~7.7° C is the warmest in the past 8 years. 

68 
SOL'TH POLE 

1984 

\\ 

'I "D :;-PI:t.l)(W S) 

_ "'~ '-5 ... 

(::=:J ... ~ lI S 10 

. S l 10 

I: 

s 

SOt.:TH POLE: 

71-83 

IV 

I I"D SPE£D(II '5) 

_ ... ~ · S<."t 

r:::=:l ... , '5' 10 

o S~10 

WJ\"O RO~E: 

I: I 

S 'II I .. D rfltQ 

Figure 4.--Wind roses of surface winds for SPO for (left) 1983 and (right) 

1977-1983 . The distribution of the resultant wind direction and speed are in 

units of percent occurrance for the year and 7-year period, respectively. 

Wind speed is displayed as a function of direction in three speed classes. 

Table 5.--SPO 1984 monthly climate summary* 

J" Feb Mar Ape ~ay Juo Jul Au, Sep Oct Nov Dec 19811 

Prevailing wind ""E N ::NE E NE £Sf: mlE NNE IWE E NIlE N mlE 

direction 

Average .... lnd U 4.7 ' . 6 '.5 5.8 '.3 7. 5 5.6 6 . 1 3.9 '. , '.2 5.0 

speed (m ,,-1) 

MaximUl'l ;.rind 8 10 9 8 13 9 " 11 1 J 9 8 11 

speedt ( m ,,-1) " 

DirectIon of max . 11 357 7 12 20 128 18 8 12 3'J 339 J59 18 

.... indt (deg. ) 

Average station 692 .3 683 .8 679 .11 679.7 683 2 676.2 674.7 617.7 675 .11 612.9 680.7 693.9 680 . 8 

pressure (mbl 

Maximu:n pressuret 707 699 698 691 10' 696 69' 691 697 683 690 703 707 

( mb) 

Min imum pressuret 679 666 666 666 669 659 66' 660 665 663 670 677 659 

(mb) 

Average air -28 . 5 -39. 0 -50 . 0 -5 8 .6 -511.1 -62 . 9 -53·0 -58.11 -55 . 0 -51.11 - 35 . 9 -22.5 - 1'7 , 7 

te1:lperature (Oe ) 

Maxi:num temperat-uret ·22 '19 ·28 ." '35 ." ·J8 " 5 .JJ -3 u ·27 ." ." 

(OC) 

Min imum temperaturet '3' ·57 ·63 ·68 ·69 ·75 ·67 ·12 ·12 ·66 '50 '32 '75 

( oC) 

-Instrument heIghts: wInd , 12 m; pressure, 28111 m (MSL) ; .Ie temperature, 2 m. The anemometer "d thermometer are 

located on a tower 100 m grid ESE of CAr . Pressure measurements are made inside CAf. 

tMaxlmum and minimum values are hourly averages . 

69 
DATA MANAGEMENT 

ICDAS Operation 

With regard to the operation of ICDAS in 1984, the major event of 

consequence was the interruption to the supply of power at MLO. For 29 days 

in April, the power was off. Generator power was implemented near the end of 

April. For the remainder of the year MLO experienced ICDAS failures that 

accounted for 96 hours . The ICDAS at BRW was decommissioned during the 4th 

week of July to allow renovations of the station interior. CAMS was started 

August 9, 1984. Early in the year BRW experienced 214 hours of down time 

caused by tape drive failures. For the remainder of the year only 24 hours 

were reported. Samoa reported 73 hours of ICDAS down time during the first 

quarter of 1984 and none until the unit was replaced by CAMS, October 15, 

1984. While brownouts continue to plague the SPO GMCC measurements causing 

intermittent interruptions to the data flow, longer-term outages were avoided. 

CAMS Testing and Deployment 

At the beginning of the year the software for the Aerosol and Solar 

Radiation (ASR) CAMS and Meteorology and Ozone (M03) CAMS was complete , but 

for the most part untested. The software to operate the carbon dioxide CAMS 

was incomplete at that time. Due to excessive transmission lengths between 

the ozone monitoring instrumentation and the CAMS in Samoa, it was decided to 

implement an RS-422 port which required software changes and further 

testing. No further hardware changes were made. A complete listing of the 

subcomponents that make up CAMS can be found in Summary Report No. 12 (Harris 

and Nickerson, 1984). Most of the serious bugs in the software were located 

and corrected by late spring. The testing of the four CAMS, (a spare unit is 

maintained at each station) for BRW was begun in May and the units were 

certified and shipped at the end of July. The new CAMS's were installed 

without difficulty the first week in August. Testing of the 4 CAMS destined 

for SMO began with the removal of the BRW set. This phase was completed 

without difficulty and the units were sent to SMO the end of August . The 

installation in SMO was completed during the second week of October . 

A third set of CAMS were installed for testing with the removal of the 

SMO unit. The electronics were removed at the end of September and shipped to 

SPO. The enclosures were sent during the previous austral summer to avoid 

shipping delays common at the beginning of the session. The remaining period 

from October through mid-November was used to test the four CAMS for MLO . The 

installation at SPO was hindered by missing compcnents, specifically 

connectors to attach the printer. As a result it was not possible to complete 

the installation of the ASR CAMS. Parts arrived a couple of weeks later and 

the installation was completed by the staff early in December. The C02 and 

M03 CAMS began operation at SPO during the 3rd week of November. The CAMS at 

MLO were installed during the 4th week of November. Two problems arose during 

this installation. The first involved the accurate acquisition of voltages 

from the CO 2 analyzer. It was solved by increasing the gain for the analogto-digital converter. The second involved a faulty memory board in the M03 

CAMS which was causing certain files not to be written to tape and, therefore, 

inhibiting tape recording of all data. The problem was not correctly 

diagnosed and corrected until the end of December. It resulted in the missing 

70 
of data for the weekends in December. Due to noise problems, it was necessary 

to add preamplifiers to the solar radiation channels , later in the year. This 

changeover was not completed until early in 1985. 

Figure 5 .--Photographs of the CAMS installation in BRW , showing both the M03 

and ASR CAMS on the left and the C02 CAMS on the right. 

6. 2 Atmospheric Trajectories 

Descriptions of various atmospheric trajectory programs developed within 

GMCC have appeared in previous summary reports (Bodhaine and Harris , 1982 , pp. 

71-74; Harris and Bodhaine , 1983 , pp . 67-75; Harris and Nickerson, 1984, pp. 

73-80). This section describes trajectory work done during 1984, including 

improvements made to the isentropic model and an example comparing isobaric 

and isentropic trajectories f or an AGASP case study . 

Table 6 lists most of the isobaric trajectories produced in GMCC in 

1984 . Another year (1983) was added to the MLO and SMO climatologies , and 

many trajectories were produced f or Arctic locations in support of AGASP 

(March and April 1983). Several years of trajectories were provided for 

precipitation chemistry studies at various sites . A problem in the system for 

producing trajectories in the Southern Hemisphere was finally traced to a 

switch of tapes for the Northern and Southern Hemispheres. Once the problem 

was solved , we were able to produce trajectories in the Southern Hemisphere 

for the CSIRO conference (Katherine and Cape Grim, Australia). To prevent a 

recurrence of the same problem, a hemisphere flag was added to the identification array for each record. 

Most of the trajectories produced in GMCC are isobaric; that is, the 

winds are traced along surfaces of co nstant pressure. The isentropic model 

developed during the past 2 years traces the winds on surfaces of constant 

71 
Table 6.--GMCC Trajectories Calculated in 1984 

Des ti nat ions 

Amsterdam Island 

Katherine, Australia 

Cape Grim, Australia 

SMO 

Western Mediterranean 

Bermuda 

Car i bou, Mai ne 

MLO 

1,hi te Face Mountain, New York 

Hong Kong 

Miscellaneous Arctic locations 

Equatorial Pacific cruise 

North Atlantic cruise 

Korolev cruise 

Dates 

1981-1983 

1980-1983 

1982-1983 

1983 

1982-1983 

1983 

1979-1983 

1983 

Summer 1983 

1979-1980 

Spring 1983 

1982-1983 

1983 

1983 

potential temperature, approximating adiabatic flow. This is a kinematic 

model that does not account for moisture or diabatic effects. We use the 

isobaric trajectories for most of the production work because they only 

require the wind data on the selected pressure surface , whereas calculation of 

isentropic trajectories requires height , temperature , and wind data at all 

mandatory levels because this type of trajectory may travel across several 

mandatory pressure levels . The programs that produce isentropic trajectories 

are also considerably more complex and costly to run. For these reasons , 

isentropic trajectories , at least for the time being , are used on a case study 

basis only . The AGASP example shown later demonstrates that in certai n 

situations isentropic trajectories are quite useful because , compared with 

isobaric trajectories, they give more information about heights of transport 

and source areas. 

Two main improvements were made to the isentropic model during 1984 . The 

first improvement extended the lower limit of the isentropic surface from 850 

to 1000 mb. To find the location of the isentropic surface when it falls 

between 1000 and 850 mb, we need to know the temperature at 1000 mb (T1000 ) . 

Since NMC does not provide 65 x 65 grids of temperatures at 1000 mb (only the 

wind and height information), we used a slightly different form of the 

following equation for Zj ' the height of the isentropic surface: 

72 
c 

Z +-E i g (1) 

where zi is the height of the mandatory pressure level below Zj' c p is the 

specific heat of dry air at constant pressure, g is the acceleration of 

gravity, Ti is temperature at the mandatory pressure level, Tj is the 

P K 

temperature on the isentropic surface , IT = (1000) , P is pressure (mb), 

and K is ~ or = 0.286, where R is the gas constant for dry air at constant 

p 

pressure. Eq. (1) is derived by integrating the hydrostatic equation fr om 

height zi' 

Since we have T850 and the heights at 850 and 1000 mb, we solve (1) for 

T i to get a good approximation of T1000 based on the thickness of the layer 

and the temperature at 850 mb: 

ITi)[(Zj 

.L 

TjJ + 

IT . 

1 (IT. - - z. ) c + T. IT. ln 

J 1 P J 1 IT. 

T. J 

1 IT. 

IT. ln 1 - + IT. - IT. 

J IT . J 1 

J 

where Ti = T1000 , Tj = T850' zi = z1000 (height at 1000 mb), and Zj = z850' 

(height at 850 mb). 

The second improvement to the isentropic program was the capability to 

produce forward trajectories, which could be used to investigate transport of 

pollutants or tracers from a known source. Figure 6 shows a forward 

trajectory computed for 71.32°N, 156.67°W, a location in the Ural industrial 

region of the U.S.S.R. Note that the 275-K "A" trajectory that departed on 9 

March 1983 at 0000 GMT arrived at BRW after five days of travel. The start 

location for the forward trajectories was chosen because it corresponded to 

the position 5 days back on the 275-K back trajectory shown in fig. 7. Note 

that the forward A trajectory in fig. 6 agrees well with the corresponding 

back trajectory in fig. 7 as it should. This transport to BRW occurred during 

the AGASP experiment and is discussed in detail next. 

The advantages of isentropic trajectories over isobaric ones are 

emphasized by comparing the isentropic trajectories for 1~ March 1983 at 0000 

GMT (fig. 7) to the isobaric trajectories for the same time (f ig. 8). Figure 

8 shows the 850-, 700-, and 500-mb tl'aje0tories (Harris, 198~) during an AGASP 

haze event. These levels were chosen because Schnell and Raatz (198 ~) f ound 

that the densest aerosol concentration during the event was located between 

800 and 600 mb. The 700- and 500-mb trajectories show transport over the Ural 

region after looping around from Central Europe and beyond. The la-day 

endpoints are arbitrary and do not indicate the source of the haze event. 

73 
Figure 6.--Forward 275-K isentropic 

Trajectories from 71.32°N , 156 . 67°W 

on 9 March 1983 at 0000 and 1200 GMT. 

With isobaric trajectories such as these , we can only surmise that industrial 

areas anywhere along the tracks could have contributed to the haze . Figure 7 

shows the isentropic trajectories for this case arriving at BRW along the 

270 - , 275-, and 280-K isentropic s urf aces . The heights and pressures upon 

arrival at BRW were the following : for 270 K, 1. 8 km and 807 mb ; for 275 K, 

2 . 4 km and 742 mb; and for 280 K, 3. 2 km and 665 mb . These heights roughly 

bracket the level of highest aerosol concentration mentioned previously. The 

important informati on added by these isentropic trajectories is the 

termination of each ba ck trajectory marked in fig . 7 . Because the isentropic 

surfaces are domed , as each trajectory is traced back from BRH , it rises about 

100 mb towards the pole then descends to the boundary layer where the 

trajectory terminates (spec ifically, the endpoint of the next trajectory 

segment would fall below 1000 mb , hence is undefined . ) The termination point 

is an estimate of the source r egion for air traveling to BRW along the 

isentropic surface. 

74 
, 

'280_ 

215-+ 

O"'uox 

O=27S( 

6=280 ( 

! ",'W 

./ 

I~·E i 

.I 1&o·W 

, 

Figure 7.--BRW isentropic trajectories arriving 14 March 1983 at 

0000 GMT on the 270- , 275-, and 280-K 

",,'w 

Figure 8.--BRW isobaric trajectories 

arriving 14 March 1983 at 0000 GMT 

on the 850-, 700-, and 500-mb 

isentropic surfaces. 

6. 3 References 

Bodhaine, B. A. , and J. M. Harris (eds . ) , 1982. Geophysical Monitoring for 

Climatic Change , No. 10 : Summary Report 1981. NOAA Environmental Research 

Laboratories, Boulder, CO , 158 pp . 

Harris, J. M. , 1984 . Trajectories during AGASP. Geophys. Res. Lett. 11(5): 

453-456. 

Harris, J. M. , and B. A. Bodhaine (eds.), 1983. Geophysical Monitoring for 

Cl imatic Change, No . 11: Summary Report 1982. NOAA Environmental 

Research Laboratories , Boulder, CO , 160 pp. 

Harris, J. M., and E. C. Nickerson (eds.) , 1984. Geophysical Monitoring for 

Climatic Change, No . 12: Summary Report 1983. NOAA Environmental 

Research Laboratories, Boulder , CO, 184 pp . 

Schnell , R. C., and W. Raatz , 1984. Vertical and 

of Arctic haze during AGASP: Alaskan Arctic. 

369-372. 

horizontal characteristics 

Geophys. Res. Lett. 11(5): 

Wagner, A. J. , 1985. The climate of spring 1984 - An unusuallly cold and 

stormy season over much of the United States. Mon. Weather Rev. 113:149-

169. 

75 
INTRODUCTION 

7. DIRECTOR'S OFFICE 

7.1 Continuing Programs 

PRECIPITATION CHEMISTRY 

Richard S. Artz 

Air Resources Laboratory, NOAA 

Silver Spring, MD 20910 

Rout ine and special precipitation chemistry measurements continued at the 

GMCC sites of MLO and SMO and at the regional sites. Samples were also measured appro ximately tWice-monthly at SPO and BRH. Special studies continued 

at MLO using the ion chromatograph for anion analysis for the six-site network, and plans were undertaken to purchase an additional Dionex ion chromatograph to measure cations and possibly organic acids. The Hashington, D.C. 

network Has terminated. 

BASELINE MEASUREMENTS 

The five-site special network on the island of HaHaii and a sixth site on 

Kauai continued to operate on approximately a weekly schedule . (Site locations are discussed in previous GMCC reports.) As seen in fig. 1, three of 

the stations (Kumukahi , MLO and K~lani Mauka) show strong concentration increases in March or April, probably caused by highly acidic small black 

particles in the precipitation samples caused by volcanic eruption . The 

October peak at 22 Mile Site cannot currently be explained. Agreement for S04 

at Halai Hill and Kauai, sites with s imilar elevation and orientation to the 

trade Hinds, was very good throughout the year although Halai Hill values Here 

routinely about 1 ° lleq/1 higher . 

The normal trend of decreasing S04= concentration with elevation was not 

seen in 1983 except for during the winter months. However , the removal of the 

seawater component yielded the typical result where S04= is quite constant for 

all five sites , with the exception of the very high spikes attributed to 

volcanic acti vity (fi g . 2). 

At MLO and SMO three independent pH measurements have been made for 

several years and as explained in previous GMCC reports, the GMCC H+ val ues 

should be highest in concentration, followed by NADP field val~es, and f inally 

NADP laboratory values. MLO val ues were not plotted due to a limited data 

set. HOHever , SMO values indicate that wh ile the e xpected trend Has found for 

January through May and December, intervening months were not in the expected 

order (see fig. 3). 

Precipitation values for the six-stati on Hawaiian network are shown i n 

fig. 4. While 1984 was wetter than 1983 for all sites , both 1983 and 1984 

·.ere much drier than normal. 

Snow sample da ta for BRW and SPO are shown in fig. 5 . 

samples high in sulfate at BRW (probably sea-salt sulfate) + - Hand S04 - tend to be less than 20 lleq/1. 

76 

Except for a few 

concentrations of 
~ 

1 

! 

I 

• i 

I 

i 

i 

i 

MLO 1984 KULANI MAUKA 198 4 

'" ' 00 

,,' '" n '" ' , " '00 '

,~ 

" 

~ ,~ 

1 ,~ 

'" 

'" 

'" 

! '" '00 I " 

,~ 

'" 

' 00 ~ " ~ " " ~ 

" 

" 

" " ~ 

" , " " 

= " " " ., "" ~- = ., 

$0 __ 

22 MI LE SITE 1984 HALAI H ILL 19 8 4 

'00 ~ 

" 

" " 

J ~ 

" 

" 

~ ! 

I 

~ " " 

~ 

" ~ 

, ~ 

" 

" 

" " 

= .' "" = ., "" ~-

CAPE K UMUKAHI 1984 KAUAI 1984 

ir I~ , 

If I~ ~ ~ I~ l~ • , • . .0 11 

IZZI ... (!Ul SO«_ 

Figure l.--Monthly precipitation weighted means for six sites on the 

islands of Hawaii and Kauai during 1984. 

REGIONAL MEASUREMENTS 

Two new NOAA NADP/NTN regional precipitation sites were opened in 1984; all 

of the old sites remained in operation. A second site, Presque Isle, was 

established in northern Maine near an existing site in Caribou. A second Texas 

site, Beeville, was established near an existing site in Victoria. 

77 
,~ 

'" '" '" '" '" 1 '" '" '" ! '" ,~ 

, " , " ~ " " " 

~ " 

" " , 

HAWAIIAN MONTHLY SULFAfl DATA 

m 11 .. 

HAWAIIAN MONTHLY EXCESS SULFATE DATA 

::r-------------------------------------, 

'" '" '" '" '" '" '" , " 

,~ 

" " " " " " ~ 

" " ,~~~~~~~~~~~J 

10 " 11 

Figure 2.--Mon thly precipitation weighted (left) sulfate means and (right) 

excess sulfate means for five sites on the island of Hawaii. 

S M O H+ WEIGHTED MEAN S' 984 

~------------------------------------, 

" 

" 

" 

" " I?ZZl c .. cc fU) 

Figure 3.--Monthly precipitation 

weighted pH at SMO. Values vary as 

a function of time between sample 

collection and measurement. 

BARROW , 984 

,~ 

" 

" 

1 " 

" ! 

~ " 

i ., 

~ 

" 

" 

, 

IZ2l H.o- ~ 50 4_ 

, 

~ 

~ ~ 

~ ~ 

! 

1 

i 

HAWAIIAN MONTHLY PRECIPITAllON DATA 

" 

" 

~ 

" 

" 

! l~ h 1: i I ~ d. ';~ 

" " 

I?ZZl n .. , 

Figure 4.--Monthly precipitation 

at Hawaiian sites for 1984. 

SOUTH POLE 1984 

" 

" " 

" 

Figure 5.--Snow sample ion concentrations for BRW and SPO during 1984. 

78 
I NTRODUCTI ON 

7.2 Cooperative Programs 

PRECIPITATION AMOUNTS ON ALASKA'S NORTH SLOPE 

George P. Clagett 

Soil Conservation Service 

Anchorage, Alaska 99501 

Barrow and Barter Island have been National Weather Service first-order 

weather stations for 43 and 37 years, respectively. The mean annual precipitation derived from these records and published by the National Weather 

Service is 4.4 inches for Barrow and 6. 4 inches for Barter Island . As a 

result, the widely held belief is that the Arctic is a " frozen desert" . 

Articles, reports, scientific documents and educational institutions nearly 

all refer to this belief right up to the present . 

Precipitation gauges equipped with "Hyoming Windshields" are now into the 

tenth year on the North Slope. Of the seven locations , two are at Barrow and 

Barter Island. Data from these instruments indicate that the mean annual 

precipitation is nearly 10 inches at Barrow and 12 to 13 inches at Barter 

Island. 

PRECIPITATION AMOUNTS CONTROVERSY 

Precipitation data from sites equipped with Wyoming windshields is a 

controversy among some groups that have reviewed the data: 

1. Correct Catch. Rechard (et al ., 1973, 1975) who developed the design 

of the Wyoming windshield , reported a correlation coefficient, R, of 0 . 98 with 

a standard error, S, of 0.07 for 160 separate storms between a Wyoming shield 

gauge and the standard (forest protected site) . The storms covered a three 

winter period , November through March between the fall of 1972 through the 

spring of 1975. 

2. Undercatch . Sturges (1984) , reported that over a 7-year study 

period , the gauge caught only 48% of the standard (forest protected site) 

during the midwinter (November-March) months . Also, the amount of undercatch 

is correlative with windspeed . Their data indicate under catch begins at winds 

of about 3 mph and can exceed 80% of the storm total if winds exceed 20 mph . 

3 . Overcatch . The National Weather Service ' s comment concerning the 

wide discrepancy bet\1een their data and the Wyoming gauge data at Barrow and 

Barter Island is that the Hyoming windshield erroneously "loads up" the catch 

and, therefore, makes it much greater (E . Diemer , Chief Meteorologist, 

National Weather Service , Anchorage; personal communication , 1984). They do 

not officially recognize their data as differing from a true or 100% catch, 

even though their gauges are not equipped with even so much as an Alter 

Shield. 

79 
NORTH SLOPE PRECIPITATION INVESTIGATIONS 

A fair amount of research and analysis has been directed toward resolving 

this conflict. This includes analysis of the Weather Service's historical 

records at Barrow and Barter Island; measurements of the actual water-content 

of the tundra snowpack and the volume of water held in enormous drift 

catchments . The results of these investigations include: 

1. Tundra snow measurements. Snow pack water-content measclred on the 

tundra are a minimum estimate of winter precipitation because the remaining 

snow is, in itself , less than the amount precipitated. Some of the total 

amount of snow is always relocated by wind and either evaporated or deposited 

in drifts. Measurements near Barrow by Black (1954) and Benson (1982) 

indicate the NWS winter catch of precipitation is at least 40% less than the 

snow water-content on the tundra . Similarly, U.S. Geological Survey 

measurements of tundra snow in 1977 , 1978, 1982, and 1983 near Barrow made 

during mid to late April indicate the NWS data is 36% less than snowpack 

water-content (Sloan et al 1979, 1980, 1982 , 1983). The USGS snow 

measurements averaged 30% less than nearby Wyoming gauge precipitation data 

for the same periods of time . 

2. Drift catchments . Measurement of snow in huge drift catchments was 

conducted along the banks of the Meade River near Atkasook, approximately 60 

miles SSW of Barrow between 1961 and 1979 . The amount of snow caught in the 

drifts , if it could be redeposited back upwind onto the fetch area , leads to 

an estimate of the amount of snowfall it would have taken to produce the 

drift. Benson (1982) estimated that an average 7. 68 inches of moisture fell 

as snow, of which 4.~5 inches remained on the tundra , while 3.23 inches were 

relocated. A portion of the relocation moisture was sublimated , while the 

rest accounted for the drifts which averaged 72 tons of moisture per meter of 

river bank from east winds and 31 tons from west winds. The analysis also 

shows that during heavy snow years , the NHS gauge catches a much higher 

percent of the Wyoming gauge catch. 

3. Complications due to "traces". Another source of error in weather 

station records comes from the slow rates of snowfall in Arctic areas . This 

frequently results in a run of " traces" which are not entered quantitatively 

in the records (Jackson , 1960). At both Barrow and Barter Island there are a 

large number of "traces" in the precipitation records. During the calendar 

year 1978 at Barrow , there were 282 days with recorded prec i pitati on , but 192 

of these days (60%) showed only "T" (for trace). These 192 entries of T add 

up to zero in the annual preCipitation record , and the error introduced by 

this is lnknown (Benson, 1982). 

4. Precipitation records analysis. Comparison of precipitation records 

at Barrow and Barter Island between NHS and Hyoming gauge data ShOH Wyoming 

gauges catch an average three times as much snow from September 1 to May 31 

(Benson , 1982). Individual years vary considerably from the average , 

however. During very low snowfall Hinters, the NWS standard gauge catch may 

be as low as 10% of the Hyoming gauge catch . In 1983, for instance at Barter 

Island, the NHS catch was only 16% of the tundra snowpack water-content in the 

near vicinity measured by the USGS and only 11 % of the Vlyoming gauge catch . 

80 
5 . Summer precipitation . 

summer months (June , July , and 

frequency of "trace" entries . 

Overall correction is obtained 

1 • 1. 

CONCLUSION 

National Heather Service records during the 

August) are also deficient due to the high 

Brown et al . (1968) concl~ded an adequate 

by multiplying the summer record by a factor of 

Benson ' s estimates (1982) of 9. 8 inches of mean annual precipitation at 

Barrow and 12 . 5 inches at Barter Island were arrived at through analysis of 

drift catchments and Tundara snow measurements. These analyses make the 

Wyoming gauge data appear about right . Hyoming gauge data is , however , far 

from a precise measure of precipitation. These data should only be considered 

as today ' s best available estimate of rain and snowfall in wind blown , exposed 

locations . 

It is important to continue operation of the Hyoming gauges on the Arctic 

Slope . In particular , the gauges at Barrow and Barter Island need to be 

maintained in comparison with the unshielded gauges operated by the National 

Heather Service so that refinements can be made in our correction of existing 

precipitation records. The Barrow , Hyoming-shielded gauge is maintained by 

NOAA, GMCC , while the one at Barter Island is maintained by the U. S. Fish and 

Wildlife Service . 

REFERENCES 

Benson , C. S., 1982. Reassessment of winter precipitation on Alaska ' s Arctic 

slope and measurements on the flux of windblown snow . Geophysical 

Institute, University of Alaska Report UAG R-288, September 1982 . 

Black , R. F., 1954 . PreCipitati on at Barrow , Alaska, greater than recorded. 

American Geophysical Union Transactions , 35:203-206. 

Brown , J ., S. L. Dingman , and R. I. Lewellen, 1968. Hydrology of a drainage 

basin on the Alaskan Coastal Plain . CRREL Research Report 240 . 

Glude , W. , and C. Sloan , 1980. Reconnaissance snow survey of the National 

Petrol eum Reserve in Alaska , April-May 1979. U. S. Geological Survey , 

Water Resources Investigatio ns . 

Jackson , C. I ., 1960 . Snowf all measurements in Northern Canada, Quart . J . Roy 

Meteorol. Soc. , 6:(368)273-275. 

Rechard , P. A., R. E. Br ewer , and A. Sullivan , 1973 . Measuring snowfall, a 

critical f act or for snow resource management . Paper presented at 

Symposium on Advanced Concepts and Techniques in the Study of Snow and Ice 

Resources . Monterey, Calif ., December 1973 . 

Sloan, C., D. Trabant , and W. Glude , 1979 . Reconnaissance snow survey of the 

National Petroleum Reserve in Alaska , April 1977 and April- May 1978. U.S. 

Geological Survey , Hater Resources Investigations Open-file Report 79-

1342 . 

81 
Sloan, c. E., 1982. Reconnaissance snow survey and spring inventory, North 

Slope, Alaska, 1982. u.S. Geological Survey , ,later Resources 

Investigations trip report, May 1982 . 

Sloan, C. E., 1983. Reconnaissance snow survey and spring inventory, North 

Slope, Alaska, 1983. U.S. Geological SJrvey , \·Iater Resources 

Investigations trip report , May 1983 . 

Sturges, D. L., 1984 . Comparison of precipitation as measured in gages 

protected by an Alter Shield , Hyoming Shield, and stand of trees. 52nd 

Proceedings , Western Snow Conference , Sun Valley , Idaho, April 1984. 

Proc . \-ISC 1984, 57-67 . 

82 
INTRODUCTION 

6C'3 IN ATMOSPHERIC C02 

Irving Friedman , Jim Gleason , John Stacey 

U.S. Geological Survey 

Denver , CO 80225 

With the encouragement of Lester Machta and with financial support from 

GMCC, we have been monitoring the 6C' 3 of atmospheric CO,. Sampling began in 

1981 at South Pole, Samoa, Mauna Loa and Point Barrow. Initially, the 

frequency of collection varied from one sample a month at South Pole Station 

and Barrow, to once a week at Mauna Loa , and twice monthly at Samoa. Later, 

the frequency at Barrow was increased to twice monthly and Mauna Loa was 

decreased to twice monthly. 

EXPERIMENTAL 

Samples were collected in 10 1. stainless steel flasks that were pretreated to remove carbon from the steel surface by heating them in air for 24 

hours at 450 0 C. The flasks are sealed at both ends with stainless steel 

diaphram values. The samples were collected by drawing air through two flasks 

connected in series with copper tubing. The bottom side of the flasks were 

heated to - 60 0 c during sampling to aid in convective mixing of the inflowing 

gas. The sample air was obtained from the station sampling stack. Upon 

receipt in Denver, the air from each 10 1. flask was passed through a trap 

cooled with liquid nitrogen to condense CO, and water. The trap was then 

warmed to dry ice temperature and the C02 and H20 separated. The 6C'3 and 

60'8 of the C02 is measured on a specially constructed 12 " radius, triple 

collector mass spectrometer . Replicate air samples from a high pressure tank 

has been processed and analyzed for 6C'3 with a two sigma of .020 /00 . The 

6C'3 results are reported in per mill compared to P. D.B . We report a 6'3 of 

-28.00 for NBS-21 (spectrographic graphite) as well as -1 . 950 /00 for NBS-19. 

No corrections have been applied for N20 , inasmuch as the N,O content of the 

air has been reported to be relatively constant over the time interval that we 

have been sampling . 

RESULTS 

Fig . 1 are plots of the 6C'3 versus time for the four stations . A linear 

regression of all of the data shows a decrease in C'3 at all stations 

sampled . Point Barrow , Samoa and Mauna Loa show a decrease of . 1 ± . 020 /00 

per year. South Pole shows a much smaller decrease of .020 /00 per year. If 

we eliminate a number of samples collected in early and mid 1983 that show a 

large deviation from the average , then the yearly change at South Pole is 

reduced to . 01 0 /00 per year . 

Keeling , et. al (1984) published 6C'3 data on samples collected during 

1981 at South Pole and 1981 to early 1982 at Mauna Loa. Fig. 2 shows plots in 

which their data and our data are compared. In general, the agreement is 

good , although occasional sample dates show significant disagreement . 

83 
DISCUSSION 

The seasonal variation in 6C 11 in atmospheric CO. from samples collected 

at POint Barrow is higher than at the other three stations. There is also a 

decrease in 6C 11 from south to north (see Fig. 3). these changes parallel 

those found by Mook, et al. (1983). However, we find a smaller change in 6C1. 

with time at the South Pole than that reported by Mook, et al. 

Mook, II. G., Koopmans, M., Carter, A. F. , and Keeling, C. D., 1983. 

Seasonal, latitudinal, and secular variations in t he abundance and 

isotope ratios of atmospheric carbon dioxide. Journal of Geophysical Research 88: 10915-10933. 

... 

.... 

..., 

..., 

... , 

... 

. " 

ae" ... . " 

-7.7 

.,. 

.,. 

.,. 

." 

." 

-1.1 

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... 

.... 

..., SAMOA 

..., 

... , 

... 

. " 

ae" "'" . ,. 

. " 

.,. 

.,. 

.,. 

. " 

." 

-7.1 

.,. ,., '''' 

... 

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..., 

..., 

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... 

., . ac" ... ., . 

.,. 

.,. POINT BARROW ." 

." 

-7.1 

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... 

.... 

..., SOUTH POU 

..., 

... , 

.... 0.11yl . 

ae" .... . ,. 

-7.7 

.,. 

.,. 

., . 

." 

." 

·7.1 

,.., , .. "" .,. YEARS ,., '''' 

Figure l.--Plots of 6C13 versus time. 

,.., 

VIARS 

,.., 

YEARS 

MAt..tv.lOA 

, .. 

, .. 

,,,,, . 

'''' 

,_ . 

O.ol~ . 

'''' 
te· ... 

_ ... ----. .. -,~ . ..... 

-'·~~=-~""~~OM~~N<~~_~,~7~~~"~'~~MG~ ~==~=on~ CH~~OK=-~»O=-~"~-~~ 

- -

- --........ _11. 

Figure 2.--Comparison of the data of Mook, et al. 

and this paper. 

-~'r----'r----'-----'-----'-----' 

-ll 

-LO 

actS '1M -7.1 

-,.I 

-7A 

_'2L-____ ~ ____ -L ______ ~ ____ ~ ____ ~ 

- ,., 

...... - - Figure 3.--Variation of 6C13 

with time. These lines are 

linear regression plots of the 

data plotted in Figure 1. 

85 
MEASUREMENT OF ULTRAVIOLET IRRADIANCE BETWEEN 290 nm AND 325 nm 

Bernard Goldberg 

Smithsonian Institution 

12441 Parklawn Drive, Rockville, MD 20852-1773 

Since August 1984 there has been a high precision scanning ultraviolet 

radiometer taking data in e i ght 5 nm wide bands. These bands are nominally 

centered at 290 nm, 295 nm, 300 nm, 305 nm, 310 nm, 315 nm, 320 nm and 325 

nm. The instrument was developed at the Smithsonian and a good description of 

it has been published by Goldberg (1985). 

The data are global, i . e., they contain both the beam and sky component. 

This makes it very difficult to do exact computations for ozone, however, a 

simple relationship between the various bands a llm.s us to compute with a high 

degree of accuracy, the changes in ozone. The relationship assumes equal 

effects on all bands by aerosols and other pollutants. Figure 1 shm.s a 

comparison between our calculated values and the Dobson values for ozone. 

Both data sets are raw values. 

'1Au~IA LOA 

0.' 

.., - 5 -,' 

. -: .-' 

N 

0 

"-

0 0.' 

UJ 

cr 

'" ~ • OOEISOO VALUES 

'" I: 

~ 0.' + CALCULATED FROM THE 300nm an6 305M! BANDS z 

'" U 

0" '0' DEC 

1984 

Figure 1. Comparison of Dobson 

values and computed values from 

the scanning radiometer. Although 

the computed values are lower, they 

track with the Dobson readings. 

Although the purpose of the data are not to study ozone changes, the fact 

that the simple computat i on allm.s us to do so is important f or checking the 

consistancy of the data and also helps to determine drifts in calibra tions. A 

sample set of data are shmm in Figures 2 and 3 for a fixed solar zenith 

distance in the morning. The data have a positive slope because the ozone has 

a negative slope. From all three Figures we see that two " solar events" took 

place in December of 1984 . 

86 
- " 

E 

'" cr w , >-

w 

l: 

OJO 

w 

-' 

:J 

o 

~ 

MAUNA LO A AIR SS 2.5 AM 

325nm ........ 

.-'. 

310nm 

..... ~ .. . "''' .. 

00' '" 

1984 

Figure 2. Variability at fixed solar 

angle in the longer wavelengths of the 

UVB. 

-, 

z 

l: 

, 

E 

c 

OJ 

, 

cr 

:..oJ 

>-

w 

l: 

'" w 

-' 

:J 

0 

.., 

0'1 

ost , 

! 

"t 

I ."' 

~~~A LOA AIR ~ASS 2.5 A~ 

-

305nm 

,.' "-.,." : . :~ +-- '. 

300nm 

1984 

: 

. , 

+ --. 

Figure 3. Va riability at the 

shorter UVB waveleng ths . Notic e 

the low level of 295 nm, a nd the 

absence of 290 nm i r rad ianc e. 

Although there is no 290 nm energy at this particular solar angle or at 

air mass 1.5, there is energy at noon when the sec z is less then 1.3. A more 

sensitive unit will be used to replace the one now in operation to be tter 

detect changes in the lm,est two wavelength bands. 

REFERENCE 

B. Goldberg, et al. 1985. Instrumentation for performing spectral 

measurements in a marine environment. Marine Tech. Soc. J. 18: 44 

87 
RECENI' aJNI'RIBlJI'IONS OF THE GLOBAL PRECIPITATION CHEI~IS1'RY PROJECT 

Im'ROOOCTION 

W. C. Keene and J. N. Galloway 

Department of Environmental Sciences 

University of Virginia, Charlottesville, VA 22903 

G. E. Likens 

Institute of Ecosystems Studies 

cary Arboretum, Millbrook, NY 12545 

J. M. Miller 

Air Resources Laboratory 

NOAA, Silver Spring, MD 20910 

Anthropogenic emissions of S02 and NOx has resulted in widespread acidification of precipitation and subsequent environmental damage in Eastern North 

America and Northern Europe. Of numerous research questions posed by this 

phenomenon, two are of special interest: (1) What was the composition of 

precipitation prior to the advent of fossil-fuel combustion; and (2) To what 

degree dces the long-distance transport of sulfur and nitrogen speci es influence the composition of precipitation in remote regions of the world? The 

Global Precipitation Chemistry Project (GPCP) was initiated in 1979 to address 

these questions. Principal objectives are to measure the chemical composition 

of precipitation in remote areas of the world and to determine major processes 

controlling measured composition. Earlier reports of the GPCP include a 

preliminary assessment of the composition of precipitation in remote areas of 

the world (Galloway, 1982), an analysis of organic acidity in precipitation 

from remote regions (Keene et al., 1983) and an evaluation of the long 

distance transport of anthropogenic pollutants from North American to Bermuda 

(Jickells et a1., 1982; Church et al., 1982). In this report, we will summarize current research and review more recent contributions of the project. 

MATERIALS AND ME:I'HODS 

Samples of precipitation are coll ected by event in scrupulously washed 

polyethylene containers. Immediately after collection, pH is measured, samples are treated with CHCl3 to prevent biological activity and aliquots are 

susequently sent to the University of Virginia for analyses for major organic 

and inorganic chemical constituents. To-date we have analyzed 1,247 samples 

of precipitation collected at 12 land-based sites and during 4 oceanic cruises. 

RESULTS AND DISCUSSION 

Composition of Precipitation and Influence of Air Mass Source Region 

Amsterdam Island, Southern Indian Ocean. Precipitation on Amsterdam 

Island h~s two components, seawater and acid (Galloway and Gaudry, 1984). 

Using Mg + as the ;teawater t:f.acer, the£e were ~o si:p.ificant differences 

between the K+ /Mg +, Cl-/Mg +, N + /Mg + and ca + /Mg + ratios of the rain and 

those of seawater. The S~-/Mg + ratio was significantly larger than the 

88 
seawater ratio although the non-seasalt component was substantially smaller 

than the seasalt component. The volume weighted pH of the precipitation 

samples was 5.06 with primary donors being H2SOA, organic acids (HCOOH and 

CH3COOH) and HN03• The maximum contributions of these acids to precipitation 

aCldity were 30, 25 and 15%, respectively. The alkaline seawater component 

reacted with the acid component neutralizing 10% of the original volume 

weighted free acidity. Specific samples ranged from 10 to 50% neutralization, 

~2~nding on the relative magnitude of the acid and seawater components. 

Rn was used as a tracer to estimate the influence of the long range 

transport of continental material on the composition of Amsterdam Island 

precipitation. Only N03- was found to have a possible continental source. 

Alaska. The chemical composition of precipitation collected at Poker 

Flat, Alaska and at Point Barrow, Alaska was analyzed in conjunction with 

backward air trajectories to evaluate temporal variations in, and the influence of source regions on precipitation chemistry in Alaska (Dayan et aL, 

1985). The free acidity of precipitation generally decreased from spring 

through autumn at both sites. Three major sources of air were associated with 

precipitation events at Poker flat. Southwesterly flow from the Pacific Ocean 

generated 42% of the storms (volume weighted H+ = 9.8 ueq/l); localized flow 

generated 25% (volume weighted H+ = 12.7 ueq/l); and northerly flow from the 

arctic generated 19% (volume weighted H+ = 7.8 ueq/l). H~4 was the most 

important source of a acidity contributing between 46 ana 80% of free H+. 

Organic acids contributed a maximum of 33%, and HN03 contributed a maximum of 

20% of free H+ in samples. Pacific and local storms were similar in composi- ti~n, suggesting a similar mix of sources. Arctic storms exhibited higher 

S04- but lower H+ concentrations, suggesting long-distance transport and 

neutralization of anthropogenic acids from the Polar region. 

Organic Acidity in Precipitation 

Extending previous work, Keene and Galloway (1984) measured organic 

anions in 16 precipitation events sampled in central Virginia between 25 April 

and 1 October 1983. HCOOH and 0l3COOH contributed 16% of volume weighted free 

acidity. The decrease in free aCldity in stored aliquots was directly 

proportional to the disappearance of dissociated HOOO- and 0l3000-. The loss 

of free acidity between pH measured at field sites and at central laboratories 

was used to estimate dissociated organic acidity in samples collected by the 

National Atmospheric Deposition Program (NADP) and the MAP3S Precipitation 

Chemistry Project. Based on the arithmetic means of the volume weighted 

averages for each site, it was estimated that organic acids contributed 18-35% 

of free acidity in NADP samples and 16% of free acidity in MAP3S samples. The 

loss of free acidity in MAP3S samples was three times greater during the 

growing season than it was during the rest of the year. Because they are 

rapidly assimilated by microbes, organic acids are unimportant in the longterm acidification of the environment. The nature of organic acidity in 

precipitation is, however, an important consideration for analytical 

techniques such as Gran's titrations which are commonly used to differentiate 

strong and weak acidity in precipitation (Keene and Galloway, 1985). 

Natural Versus Anthropogenic Components in Precipitation 

The concentrations of H+, soa-, and NO) in the precipitation of eastern 

North America are greater now than they were historically as a result of 

89 
fossil-fuel combustion. Because of a lack of data prior to 1950, the absolute 

increases in the concentrations of these three ions are unknown. This problem 

can be addressed by comparing the composition of precipitation from impacted 

areas with that of precipitation from remote areas. An analysis of precipita- tion data indicates that many areas of eastern ~rth America receive 

precipitation with substantial~ greater H+, S04-' and N03 concentrations than 

remote areas. For example, S04-' the most ecologically slgnificant indicator 

of change, is enriched 2 to 16 times in eastern North American precipitation 

relative to its concentration in remote areas (Galloway et aL, 1985). 

Otn)I~ RESEARCH 

Research efforts which are currently underway within the GPCP include: 

o A rigorous evaluation of assumptions involved in correcting 

precipitation chemistry for the influence of seasalt. 

o A reanalysis of process controlling precipitation chemistry on Bermuda. 

o Analysis of processes controlling precipitation chemistry at 

Katherine, Australia. 

o Development of a sampler for organic acids in the gaseous and 

particulate phases. 

REFERENCES 

Church, T. M., J. N. Galloway, T. D. Jickells, and A. H. Knap, 1982. The 

chemistry of western Atlantic precipitation at the mid-Atlantic coast and on 

Bermuda. Journal of Gecphysical Research 87: 11013-11018. 

Dayan, U., J. M. Miller, w. C. Keene, and J. N. Galloway, 1985. A meteorological analysis of precipitation chemistry from Alaska. Atmospheric Environment 19: 651-657. 

Galloway, J. N. and A. Gaudry, 1984. The chemistry of precipitation on 

Amsterdam Island, Indian Ocean. Atmospheric Environment 18: 2649-2656. 

Galloway, J. N., G. E. Likens, W. C. Keene, and J. M. Miller, 1982. The 

composition of precipitation in remote areas of the world. Journal of 

Gecphysical Research 87: 8771-8786. 

Galloway, J. N., G. E. Likens, and M. E. Hawley, 1985. Acid precipitation: 

Natural versus anthropogenic components. Science 226: 829-830. 

Jickells, T. C., A. H. Knap, T. M. Church, J. N. Galloway, and J. M. Miller, 

1982. Acid precipitation on Bermuda. Nature 297: 55-56. 

Keene, W. C., J. N. Galloway and D. H. Holden, Jr., 1983. Measurement of weak 

organic acidity in precipitation from remote areas of the world. Journal of 

Gecphysical Research 88: 5122-5130. 

Keene, W. C. and J. N. Galloway, 1984. Organic acidity in precipitation of 

North America. Atmospheric Environment 18: 2491-2497. 

Keene, W. C., and J. N. Galloway, 1985. Gran's titrations: Inherent errors 

in measuring the acidity of precipitation. Atmospheric Environment 19: 199-

202. 

90 
TRICHLOROTRIFLUOROETHANE (F-l13): 

TRENDS AT PT. BARRQl, , ALASKA 

H. A. K. Khalil and R. A. Rasmussen 

Department of Chemical, Biological, and Environmental Sciences 

Oregon Graduate Center, Beaverton, OR 97006 

The production and uses of trichloro trifluoroethane (C2C13F3i F-113) have 

been increasing ra pidly. Since the atmospheric lifetime of F-113 is quite 

long, its atmospheric concentration is also inc r easing rapidly. Although at 

present the atmosphe ric levels are only around 30 pptv, it constitutes some 

90 pptv of anthropogenic gaseous chlorine. In the future increased levels of 

F-113 may deplete the stratospheric ozone layer. He r e we will report on the 

rate of increase of F-113 observed at Barrow and the precision of measurement 

of F-113 in flask sampl es. 

Starting in January 1983 we have taken measurements of F-113 at Pt. 

Barrow, Alaska. Tr iplicate air samples were collected in 0.8 L s tainless 

steel flasks and sent to the Oregon Graduate Center where the concentrations 

of trace gases were measured (Rasmussen & Khalil, 1980). In all, some 115 

weeks of data have been obtained thus far, constituting a total of nearly 350 

sampl es of air. The concentration of F-113 was measured with a gas chromatograph equipped 'vith an electron capture detector (EC/GC). 

The concentrations of F-113 were found to be almost the same in ' the three 

flasks that constituted a weekly sample . The standard error (est a/Jn ; n = 3) 

of the concentrations in the three cans of the triplicate sample may be 

interpreted as the c.ombined prec.ision due to shor t-term atmospheric 

variability, and the sampling and analytical methods. Figu re l a shm,s the 

frequency distribution of the standard deviations of the concentrat i ons 

observed each week in the triplicate samples. In Figure lb these data are 

expressed as the percent of time the standard deviation exceeded the value on 

the horizontal axis. For instance, according to Figure la the standard 

deviation \Vas most often (mode) between 0 . 07 pptv and 0.33 pptv (37% of the 

time in 113 \Veekly samp l es) . According to Figure lb, 50% of the time the 

st andard error of the triplicate samples was l ess than 1% of the mean value , 

90% of the time it was less than 2.5%, and it never exceeded 5%. These 

r esults demonstrate that in our method of flask sampl ing and EC/GC analysis 

the variability of F-113 is extreme l y small and that flask samples can be 

used to accurately determine the lon g-term trend of F-113 at Barro\V, Alaska. 

From the observations of F-113 at Barrow it is apparent that the 

concentrations are increasing at a relatively rapid rate caused by the 

increasing emissions and the long atmospheric lifetime. In Figure 2 the 

monthly averaged concentrations of F-113 are plotted. The rate of increase 

Has determined by using the equation C = a e Bt . According to the results 

shown in Table 1, F-l13 increased at a rate of 13% per year betlVeen January 

1983 and early 1985 (27 mon ths). Over the past 21 mont hs the rate of 

increase is about 14% per y ear. It is probable that the rate of increase of 

F-113 is als o increasing. In Table 1 the results obtained at Barrow, Alaska , 

are compared with previously published results of the increase of F-113 

observed at the Sou th Pole (Rasmussen & Khalil, 1982). The time series of 

meas urements of F-ll 3 at Barrow and the South Pole are for different times . 

91 
100 

90 

60 

0 ~ 70 

<f) 60 z 

0 

I- 50 

<l 

> 

0: 40 w 

<f) 

CD 30 

0 

20 

10 

0 

0.0 

F-113 Precision 

Borrow, Alaska 

, r- FIt. 1 .. 

- 0 

'r rror- h-n-.-, 

,,, '" 001 060 "0 STAtlOARO OEVIATtONS (",tv) 

0.5 1.0 1.5 2.0 2.5 3.0 3.5 4.0 

STANDARD ERROR (%) 

-

,,, 

4 .5 5.0 

Figure la.--Precision of measured concentrations of F-113 shown as the 

distribution of standard deviations of the concentrations of F-113 at 

Barrow, Alaska, in each week's triplicate samples. 

Figure lb.--Cumulative frequency distribution of the Standard Error of 

the concentrations of F-ll3 in triplicate flask samples collected at the 

same time. The variability of the short-term atmospheric concentrations, 

sampling and analytical methods is ~ 2.5% 95% of the time (baseu on 113 

sets of triplicate samples). 

33 

32 

-; 31 "-

"- 30 

Z 

0 29 

I-

<l 

0: 26 

Iz 

w 27 

U 

Z 

0 26 u 

25 

24 

F-113 0 

PI. Borrow, Alaska 0 

0 0 

0 

0 

0 

0 

0 0 

0 

0 

o 0 

0 

00 0 

0 

0 5 10 15 20 25 

JAN 1983 T11AE (monlhs) 

Figure 2 .--The increase of trichlorotrifluoroethane 

(C ZC13F3 ; F-ll3) at Barrow, Alaska. The first datum 

is for January 1983. 

92 
At the South Pole the measurements were reported from 1979-1982, while the 

Barrow data are for 1983-1985. The rates of increase are comparable, and the 

difference may be due to the acceleration of the accumulation of F-113 in the 

atmosphere. The calculations of the increase based on the linear equation 

C = A + bt are also given in Table 1. 

We conclude that (1) the trends of F-113 can be accurately measured by 

using weekly flask sampling procedures; (2) the concentration of F-113 is 

increasing relatively rapidly at a rate of about 14% per year in response to 

the long atmospheric lifetime and the increasing uses of F-l13; and (3) the 

F-113 may be increasing at a faster rate now than a few years ago. 

Table l . --The rate of increase of F-113 observed at Pt. Barrow, Alaska 

S (%/yr) 

b (pptv/yr) 

a (pptv) 

A 

r 

N (months) 

Exp. (Barrow) 

All data 21 months 

13.0 

±O.l 

23.9 

0.98 

27 

14.3 

±l.l 

23.4 

0.98 

27 

Lin. (Barrow) 

3.7 

±0.3 

23.7 

0.98 

21 

Exp. (South Pole) 

10 

12 

0.99 

4 

a and S refer to the (exponential) model C - ae SE , and A and b refer to 

(linear) C = A + bt. The ± values are the 90% confidence limits. r is the 

correlation coefficient . N is the number of months data during which measurements were taken. At the South Pole measurements are taken only during the 

austral summer of each year. Exp. r efers to the exponential case and Lin. to 

the linear case. The data for the South Pole are for 1/1979-1/1982 and those 

for Barrow are from 1/1983-3/1985. 

REFERENCES 

Rasmussen, R. A., and M. A. K. Khalil, 1983. Atmospheric fluorocarbons and 

methyl chloroform at the South Pole. Antarctic Journal of the United 

States, Volume XVII, No. 5 : 203-205. 

Rasmussen, R. A., and M. A. K. Khalil, 1980. Atmospheric halocarbons: 

measurements and analyses of selected trace gases. Proceedings, NATO 

Advanced Study Institute on Atmospheric Ozone: Its Variation and Human 

Influences, Algarve, Po rtugal, October 1-13, 1979. A. C. Aikin (Ed.), 

U.S. DOT, Hashington, D.C., 209-231. 

93 
DETECTION OF ATMOSPHERIC TRACERS IN ANTARCTICA 

E. J. Mroz, M. Alei, J. H. Cappis, P. R. Guthals, 

A. S. Mason, T. L. Norris, J. Poths, and D. J. Rokop 

Los Alamos National Laboratory 

Los ALamos, New Mexico 87545 

The Antarctic Tracer Experiment is designed to aid scientific 

understanding of meridional atmospheric transport processes in Antarctica. 

Meridional transport is responsible for bringing pollutants, both natural 

and man-made, to Antarctica from the lower latitudes. These materials then 

become part of the record of climate history that is frozen in the polar 

ice cap . The experiment consists of releasing unique gases into the 

atmosphere at a time and place of our choosing and subsequently sampling 

the antarctic atmosphere in search of the tracer gases. Figure 1 shows the 

experimental concept and the location of the stations where sampling for 

the tracer is being conducted. 

The tracers used are 13CD4 and 12CD4. These gases are isotopic 

analogs of methane and are called IIheavy methanes" because they are 

composed of the heavy isotopes of carbon and hydrogen, namely, 13C and 

deuterium. These gases can be detected in the atmosphere at a level of a 

few parts in 10 17 in air . This extremely low level of detection means that 

the gases can be detected over four thousand kilometers from the point of 

release. 

1984 Field Activities 

During the austral spring of the 83/84 season samplers were deployed 

to eight stations on the antarctic continent. The stations included the US 

stations at McMurdo, Palmer, and Amundsen-Scott. Samplers were also 

"'W ZEALAND 

HEAVY METHANE 

TRACER GAS 

PACIFIC OCEAN 

ROSS SEA 

--~~-~ ~~ 

~~ (USAI AMUNDSEN-SCOTT 

DUMONT SOUTH POLE (USA) 

DURVILLE 

(FRANCE) . .. ;. 

CASEY 

(AUSTRALIA) 

. PALMER 

(USA) 

WEDDELL SEA 

ATLANTIC OCEAN 

INDIAN OCEAN 

Figure 1. Conceptual view of the Antarctic Tracer Experiment. 

94 
installed at Halley Bay (UK), Dumont D'Urville (FR), Syowa (Japan), and 

Casey and Mawson (AUS). Sampling at these locations is being conducted 

with the cooperation of personnel stationed there. 

After the sampling network was established w~ conducted t~e first 

release of the tracer gas. This took place at 55 OO'S and 167 47'E at 

18,000 ft MSL on 9 January 84 (0015Z). One kilogram of 13CD4 was released 

from a NSF LC-130 aircraft flying from Christchurch, NZ, toward McMurdo 

Station. Upon release of the tracer, all sampling stations were notified 

to begin sampling. The sampling protocol consists of collecting one sample 

continuously over a three day period. This is followed for 60 days after 

the release. Thus, twenty samples are collected by each station following 

each release. 

Following the January release, additional samples were collected by a 

cryogenic sampler developed for use on board LC-130 aircraft. Samples were 

collected on a nearly daily basis from 9 January to 15 February by taking 

advantage of the normal flight operations of VXE-6. Samples were collected 

on flights between McMurdo and Siple, Byrd, Amundsen-Scott stations as well 

as between McMurdo and Christchurch . Other flights on which samples were 

collected included flights to the Siple coast, Martin Hills, Mt. Smart, and 

the Ohio Range areas. About one hundered samples were collected by this 

means . 

A second release of 1 kg of 13CD 4 was made on 8 June 1984. This 

release was conducted with the ass~stance of th~ US ~ir Force using a 

WC-135 aircraft and was made at 59 40'S and 160 4S'W at 18,000 ft HSL. 

Sampling was conducted at the Antarctic stations in the manner described 

above. Of course no airborne sampling CQuid be conducted during the 

austral winter. 

The third and final release took place on 18 October 1984. ThiS . 

rel~ase was comprised of two releases of different tracer gases at 62 15'S, 

172 10'E but at different altitudes. The release of 1 kg of 13CD 4 was made 

at 5,000 ft while 20 kg of 12CD4 was released at 18,000 ft. The releases 

were made from a USAF C-141 aircraft enroute from McMurdo to Christchurch, 

NZ. Following this release we again collected samples during LC-130 

aircraft flights in the same manner as after the January release. 

Trajectory Analysis 

Understanding the path by which the tracer travels is an important 

aspect of this research. A trajectory forecast of the first tracer release 

in January 1984 has been performed by meteorologists of the US Air Force, 

British Antarctic Survey, and National Oceanic and Atmospheric Administration (NOAA). 

The results are shown in Figure 2. Trajectories A through D were 

forecast by Mr. David Limbert of the British Antarctic Survey while 

Trajectory E was forecast by the US Air Force . The forecast by Dr. Elmer 

Robinson of NOAA is essentially the same as trajectory C. The dearth of 

meteorological observations in the high southern latitudes exacerbates the 

uncertainties aSSOCiated with trajectory forecasting. The plotted 

trajectories of the tracer show a wide divergence of possible paths after 

95 
just a few days. However, all of the trajectories agree that the initial 

path was toward the east and south. Similar trajectory analyses have been 

performed for the other releases. 

Figure 2. Forecast Tracer Trajectories 

Following the Release on 9 January 1984. 

We are currently analyzing the samples that were obtained following 

the January release for the presence of heavy methane. We have detected 

heavy methane in samples collected at 24,000 ft over the Ross Ice Shelf 26 

hours after the release. The tracer was found to have persisted in this 

region for several days following the release. This finding indicates that 

southward transport from the release point was much faster and further than 

had been predicted from trajectory analysis. Small amounts of tracer have 

been detected in samples collected at the South Pole and at Halley Bay 

within about a week to 10 days after the release. However, during this 

same time interval no tracer was detected at McMurdo. This suggests that 

the heavy methane did not mix down to the surface until after passing over 

McMurdo. 

This work was supported in part by National Science Foundation grant 

OPP 81-18562. Los Alamos National Laboratory is operated by the University 

of California for the United States Department of Energy under contract 

W-7405-ENG-36. 

96 
FURTHER STUDIES OF DATA COLLECTED DURING THE ARCTIC GAS AND 

AEROSOL SA}lPLING PROGRAM (AGASP)--SPRING 1983 

R. C. Schnell 

Cooperative Institute for Research in Environmental Sciences 

University of Colorado, Boulder, CO 80309 

INTRODUCTION 

The NOAA Arctic Gas and Aerosol Sampling Program (AGASP) is a study of a 

type of anthropogenic air pollution commonly known as Arctic haze. In spring 

1983, a NOAA WP-3D research aircraft, flown for 144 hours across the Arctic, 

measured Arctic haze in relation to similar measurements at surface baseline 

stations such as those at Barrow, Alaska; Alert, Northwest Territories; and Ny 

Alesund, Svalbard. The initial results from these flights and the companion 

cooperative programs conducted by scientists from Canada, Norway, Sweden, 

United Kingdom, and the Federal Republic of Germany have been published in a 

special issue of Geophysical Research Letters, Vol. Q, Hay 1984 (28 papers). 

Some subsequent analyses and future research plans are presented below. 

PARTICULATE SULFUR IN ARCTIC HAZE 

Sulfur in various forms is a large component of the haze aerosols. On 

the AGASP flights, particulate sulfur was captured on a variety of filter 

media for various exposure volumes both in and out of visible haze layers. 

Some samples were integrated over a total flight. 

In fig. 1 are presented the concentrations of particulate S as measur ed 

by five separate groups using different sampling systems on the AGASP flights. 

For the FSU impactors, like the CNL filters, integrations are over periods 

from 4.5 to 9.5 h and usually include up to 3 h of high-altitude ferry time in 

air with little or no haze. The measurements by the LBL group are from 

filters exposed for periods ranging from O.S to 2 h in either haze or clearair target zones. The NCAR fi l ters were exposed mainly in haze layers for 

periods of from 1 to 2 h. The NOAA sample for flight 6 was obtained from 

impactor grids and in situ aerosol probes; this is discussed by Shapiro et al. 

(1984) • 

The highest S values plotted in fig. 1 were from the haze layer measurements and the lowest values for "c l ean air" zones. The S values obtained from 

the flight-integrated filters (FSU and CNL) fall within the lower portion of 

the two extremes, as would be expected. With respect to the highest S values 

measured during the AGASP program, Hansen and Rosen (1984) have shown that 

they occurred in haze layers restricted to the lower 2 km of the Arctic atmosphere and that the S concentrations measured aloft were greater than those 

measured at the surface near sea level at the Barrow GMCC Baseline Station. 

With respect to the flight-integrated samples, it is worthy of note that 

on flights 7 and 9 the CNL filter and FSU impactor began and ended sampling 

relatively close in time of each other; they also pr£1uced comparable S concentration values. The CNL system ran at 10.S L min and the FSU system at 

97 
SULFUR, AGASP 1983 

2000 - Alaska - -Norway6 2 

• 

1000 • • 2 

l Ii 

• • M 

I 500 

E 

Figure 1.--Particulate sulfur concentrations measured during the 

AGASP program. Flight numbers and 

dates are 1, 11 March; 2, 13 March; 

3, 15 Harch; 4, 17 March; 5, 21 

March; 6, 23 March; 7, 28 March; 8, 

31 March, 9, 4 April; 10, 5 April; 

and 11, 10 April, 1983. The sulfur 

measurements were conducted by LBL 

(Hansen and Rosen, 1984), NCAR 

(Lazrus and Ferek, 1984), CNL 

(Cahill and Eldred, 1984), FSU, and 

NOAA. All concentrations are in STP 

units. 

OJ 

C 

• o 

200 

100 

KEY: 

• FSU 

• 

o NOAA .. 

.. LBL 

6NCAR 

oCNL 

50L-~-L2~3~~4~5~~6--7~~8~79~10~~'1~ 

AGASP Flight No . 

. -1 1.6 L m1n On flight 4, the CNL filter was run for a 30% longer period on 

the ferry leg (clean air) than the FSU impactor, which is reflected in higher 

per unit volume S concentrations observed on the FSU impactor. On flight 5, 

the exposure times were reversed (40% longer clean-air exposure on the FSU 

impactor), with the result that higher average S concentrations were observed 

on the CNL filter. 

Both the comments in the flight observers' logs and the gas and aerosol 

profiles collected during AGASP leave an overall impression that the haze in 

the Alaskan Arctic was much more stratified and layered than in the Norwegian 

Arctic. For instance, on flights 1 and 2 in the Alaskan Arctic, up to six ha ze 

layers interspersed with extremel y clean air were observed (Schnell and Raatz, 

1984). On flights 7 and 8 in the Norwegian Arctic, when the aircraft was in 

haze, the haze appeared to be more well mixed throughout the troposphere, and 

fewer clean zones were observed between haze bands (Raatz and Schnell, 1984). 

These observations could explain the greater variation in measured S concentrations in the Alaskan Arctic than in the Norwegian Arctic. 

Sulfur measured in stratospheric air within a tropopause fold (flight 6) 

is also plotted in fig. 1. From these data it may be observed that S was 

measured in concentrations similar to those measured in Arctic haze layers. 

This S is thought to be in the form of pure H

2

S04 produced by the El Chichon 

eruption. Shapiro et al. (1984) have published electron micrographs of these 

sul fur-containing droplets. 

Finally, it is of interest to note that within the haze, S values a!3 

va r ious altitudes on both sides of the Arctic cluster at about 1000 ng m STP 

in concentration. This suggests that S is dispersed fairly evenly througho ut 

the polluted Arctic troposphere and that there were no major sinks for S over 

the Arctic ice cap during the period of these measurements (March-April 1983). 

98 
TRANSPORT OF POLLUTION OVER THE NORWEGIAN ARCTIC 

On two research flights in the Norwegian Arctic, the horizontal and verti cal variability of the Arctic haze was probed using the NOAA WP-3D research 

aircraft and dropwindsondes. The results from a flight on 4 April 1983 are 

presented here. 

As shown in fig. 2, the aircraft flew north at 426 mb and descended to 

o 0 1000 mb at 69.75 N, 10.7 E through the southern frontal boundary of a polluted 

continental polar air mass. The dry, haze-laden zone of haze transport was 

traversed between 680 and 820 mb (Raatz and Schnell , 1984). 

APRIL 4, 1983 

400 

,.... 

.a 

E 

,.; 500 

W 

a: 

::::> 300 

en 600 en 

w 

a: 

a. 700 

290 

800 

900 280 

1000 

67 68 69 70 

BOD 

71 72 73 74 75 

DROP+ 3 DROP+ 2 

LATITUDE (ON) 

..----I-_~, , 

\ 

\ 

, 

300 

1..----1' 

_~--+C"- 290 

~-,- )I\L:::c.;.:.~ ... ::-:: .. t:. -':: ~~-r-\-280 

~.-,.-\-

" 

76 717 7,8 

DROP

~ 

#1 BRG 

Ice edge 

1-

79 

Figure 2:--Latitude-altitude cross section of potential temperature (K, solid -2 -1 ) lines) and water vapor mixing ratio (x 10 g kg ,thin broken lines for 4 

April 1983. The aircraft flight track is indicated by the thick broken line; 

wind speeds are in knots. The approxi mate core of the haze transport zone is 

indicated by shading. The top of the marine boundary layer is indicated by 

the dark dotted line. 

99 
After completing the profile, the aircraft probed the horizontal variability of the main haze transport zone characteristics. Between 1011 GMT 

(69.9S

o

N, 11.420E) and 1127 GMT (73.020 N, 23.73oE) the aircraft flew at a constant pressure of 770 mb northbound. Within the haze transport zone of heavy 

aerosol loading (-1030 GMT), the aircraft passed into a patch of relatively 

cleaner and drier air at the northern edge of the transport zone. At 1118 G~lT 

the core of the haze transport zone was reentered east of the earlier exit 

point. 

Fo r a portion of the flight, the aircraft flew in the haze transport zone 

and made two descents through the marine boundary layer to just above the 

ocean. Toward the end of the flight, the aircraft flew through the ice edge 

baroclinic zone to a point 175 km north over the pack ice. On the climb out, a a at 79 -78 N for the return leg, the bottom of the haze was observed at 790 mb 

and the top of the main haze zone at 610 mb. On that day the northern boundary of the haze zone was not determined, but it was north of 790

N. 

The boundaries of the core of the haze transport zone on 4 April were 

well defined at the top and bottom, determined in general terms on the southern edge, and extended beyond 780

-790 N, the limit of the aircraft flight path. 

These boundaries are shown in fig. 2 by the shaded area. 

These and other measurements document the transport of heavy concentrations of anthropogenic aerosols (within well-defined dry continental air 

masses) out of Eurasia into the Norwegian Arctic. Such haze transport zones 

had be en suggested as being in existence by Raatz and Schnell (1984). 

AGASP-II, MAltCH-APRIL 1986 

In spring 1986, Arctic haze will be studied both at the surface and aloft 

in a comprehensive international program. Surface measurements of gases, 

aerosols, solar radiation, and meteorology will be conducted from baseline 

stations located at Barrow, Alert, and Ny Alesund. Upward-pointing lidar 

measurements of the haze layers will be obtained at Alert, and ozonesondes 

will be released from both Alert and Barrow. The NOAA WP-3D, University of 

\,ashington C-131A, and Max-Planck-Institute Hawker Siddeley 125 aircraft will 

operate together out of Thule, Greenland, flying research patterns above and 

upwind of the Alert baseline station. Similar patterns will be flown by the 

NILU Piper Navajo in relation to the Ny Alesund baseline station, both above 

and in conjunction with the NOAA WP-3D and ~[ax-Planck Hawker Siddeley. The 

NOAA WP-3D will fly solo research flights in conjunction with ground measurements at the Poker Flat Optical and Atmospheric Chemistry Facility and the 

Barrow baseline station. The planned flight paths and surface locations are 

shown in fig. 3. 

In addition to the above program, heavy methane tracers and constantlevel balloons will be released from Europe to trace the pollution across the 

polar region. 

100 
AGASP-II USSR 

March-April, 1986 /; 

"-PI. 

Anchorage 

\ 

REFERENCES 

700 -. 

AC' • Pen Taymyr Insula_ ~ oJ) 0 

0(') d ~.../ 

C>~ 800 ~ Novaya 

i East ;/ :.. Zemlya S SIberian 0.. cand~avia 

e Sea Svalbard \ B~dO Intensive ~ Study__ I 

Area 

D 

Kellavik Figure 3.--0perational area, flight 

tracks , and s urf ace sampling and 

base operations fo r the 1986 Arc tic 

ha ze r esearch project. 

Cahill, T. A., and Ellred, R. A .• 1984 . El emental composition of Arctic particulate matter. Geophysical Research Letters 11: 413-4 16. 

Hansen, A. D. A., and H. Rosen, 1984. Vertical distributions of particulate 

carbon, sulfur, and bromine in the Arctic haze and comparison with groundlevel measurements at Barrow, Alaska. Geophysical Research Le tters 

11:381-384. 

Lazrus , A. L., and R. J. Fe r ck , 1984. Acidic s ulfa te particles in the winter 

Arctic Atmosphere . Geophysical Research Letters 11:417-419. 

Raatz, W. E., and R. C. Schnell, 1984. Aerosol distributions and an Arctic 

aerosol front during AGASP : Norwegian Arctic. Geophysical Research Letters 

11: 373-376 . 

Schnell, R. C., and W. E. Raatz, 1984. Vertical and 

tics of Arctic haze during AGASP: Alaskan Arctic. 

Letters 11:369-372. 

hor i zontal characterisGeophysical Research 

Shapiro, M. A., R. C. Schnell, F. P. Parungo , S. J. Oltmans, and B. A. 

Bodhaine, 1984. EI Chichon volcanic debris in an Arc tic tropospheric fold. 

Geophysical Research Letters 11:421-424. 

101 
INTRODUCTION 

ATHOSPHERIC SUBHICRON PARTICLE 

COLLECTION AT THE SOUTH POLE OBSERVATORY 

R. E. Ihtkowski and Iv. A. Cassidy 

University of Pittsburgh 

Pittsburgh, PA 15260 

G. IV. Penney 

Carnegie-Hellon University 

Pittsburgh, PA 15213 

In a continuing effort as part of the University of Pittsburgh Antarctic 

Search for Meteorites Project, an atmospher ic particle collector has been in 

operation at the South Pole Observatory's Clean Air Facility (IVitkowski, et al., 

1984). To date, more than 12,000 hours of collection time has been logged; a 

total of 27 specimen plates have been exposed and returned to the labora tory 

for study using scanning transmission electron microscopy coupled with energy 

dispersive spectrometry and selected area diffraction for particle morphology, 

elemental composition and crystallographic structure determinations. Particles 

nO\, have been collected throughout the entire year (December 1933 to the end 

of November 1984) with detailed laboratory studies being carried out on specific 

specimen plates exposed for time intervals as low as 24 hours and as high as 

4000 hours. These studies have s ho\;n that collection periods of 1000 hours 

during the austral summer a nd 4000 hours during the austral winter "ill produce 

collections that are ideal for individual particle anrtlysis, i. e., high particle 

density per unit area , without such high densities that agglomerates form . 

RESULTS AND DISCUSSION 

Submicroscopic particles from contamjnating sources are very abundant in 

the atmosphere at the South Pole. Even though this site is a loca tion "here 

airborne particles of artificial, natural and terrestrial contamination are 

expected to have low abundance, particularly during the austral winter, particles 

resulting from fossil fuel burning (fly ash alumino-silicate spheres) and volcanic and marine origin (sulfuric acid and a fragment of a siliceous radiolarian 

shell) have been found. 

In addition to these particles, "hich can be identified as terrestrial 

contaminants, a number of particles whose terrestrial origin cannot be confirmed 

have been isolated and studied. These include rod-shaped grains, typically 0.1 

micrometer long that give Ca and S elemental signatures and, although rather 

rare in number, another group of submicron size grains that apparently consists 

of single metallic elements (or, for example, their oxides, hydroxides, carbides 

or carbonates) that give single-element signatures of Hg, Ti, Cr, Fe, and Co. 

In some special cases, selected area electron diffraction measurements could be 

obtained, with the resulting diffraction patterns giving some c lue to the chemical and crystallographic make-up of a particle. For example, the fluffy aggregate of needle-like crystals (Figure 1) that gives an appearance of extreme 

fragility, and the plate-like crystals (Figure 2), yielded a pattern that suggests the mineral species magnetite or goethite . Ivhile these particles have the 

102 
I 0 . 2 .m I 

Figure l.--Needle-like c rystals. 

(Plate #14 , 1032 hours.) 

Figure 2.--Plate-like crystals . 

(Plate #14, 1032 hours.) 

simple compositions and small physical sizes that "ould be expected of extraterrestrial dust grains, they cannot be positively identified as such; the 

possibility of terrestrial contamination sources or condensation smokes of 

stratospheric origin (see, for example, Hunten, et al., 1980) still must be 

considered. 

FUTURE PROGRAI'I 

The particle collector "ill remain in operation throughout the 1984-85 

austral season. An additional set of nine collector specimen plates "ill be 

exposed. Laboratory studies "ill continue in the identification and characterization of material already returned from the previous year. 

ACKNOHLEDGMENTS 

He acknm.ledge LTJG Frank Migaiolo, NOAA-GMCC Station Chi ef, "ho maintained 

this experiment throughout the "inter season . This "ork is made possible by NSF 

grant DPP 83 14496; the electron microscope facil ities "ere made available by 

the Hestinghouse R&D Center. 

REFERENCES 

Hunten, D. M., R. P. Turco, and O. B. Toon, 1980. Smoke and dust particles of 

meteoric origin in the mesosphere and stratosphere. Journal of the Atmospheric Sciences, 32:1342-57 . 

Hitkowski, R. E., H. A. Cassidy and G. H. Penney, 1984. The search for part i c les 

of cosmic origin at SPO . Geophysical Monitoring for Climatic Change Summary 

Report No. 12, December 1984, J. M. Harris and E. V. Nickerson (Ed . ), NOAA 

Environmental Research Laboratories, Boulder, Colorado, 149-150. 

103 
8. INTERNATIONAL ACTIVITIES 

From June 1984 to January 1985, the CO 2 group had use of a Siemens 

Ultramat III infrared gas analyzer on loan from N. Trivett of Atmospheric 

Environment Service, Canada. This analyzer was tested as a possible 

replacement for the aging URAS analyzers currently in use at the GMCC 

observatories. 

Collection of flask samples for CO 2 and CH 4 analyses was begun in April 

1984 at Cape Grim Observatory, Tasmania in cooperation with the Australian CO 2 

group at CSIRO. Flask sampling was also begun at Christmas Island , Republick 

of Kiribati in cooperation with J . Bryden of Christmas Island and SIO. 

In April 1984, L. Waterman of the CO 2 group visited the CO 2 group at 

CSIRO , Australia, and made a trip to the Cape Grim Observatory. 

B. Bodhaine participated in the Third Symposium on Arctic Air Chemistry, 

7-9 May, at Downsview, Ontario, Canada. He presented the GMCC aerosol record 

obtained at BRW, and an analysis of some aerosol measurements from the AGASP 

flight program in March-April 1983. 

B. Bodhaine participated in the Scientific Application of Baseline 

Observations of Atmospheric CompOSition meeting, 7-9 November, at Aspendale , 

Australia. He presented an analysis of the GMCC aerosol record obtained at 

SMO. Many of the attendees at this meeting had the opportunity to visit the 

Australian baseline station located at Cape Grim, Tasmania. 

On 9-13 April, J. DeLuisi partiCipated in a HMO-sponsored Meeting of 

Turbidity Experts at Tenerife, Canary Islands, to commemorate the opening of a 

Spanish baseline observatory. The meeting was attended by nine experts 

representing the United States, W. Germany, Switzerland, Italy, Canada and 

Spain . The deliberations of the meeting were concerned with applications of 

sunphotometery, including measurement of °

3 , N02 , and H20, besides aerosol 

optical depth. The partiCipants recommended nine standard wavelengths for 

sunphotometery. DeLuisi described GMCC's baseline station sunphotometer 

measurements and plans for upgrading of the U. S. turbidity network . He also 

offered the MLO GMCC solar radiation facility as an ideal site for calibration 

of primary standard sunphotometers used by various countries maki ng BAPMoN 

turbidity measurements. WMO subsequently issued a memorandum designating the 

site as a World Sun photometer Calibration site. 

R. Grass and R. Evans visited Perth , Australia during July and August 

1984 to install automated Dobson ozone spectrophotometer No . 81 for operation 

at the Australian Bureau of Meteorology Weather Office . The Perth station is 

one of seven global si tes where Umkehr observations will be made on a longterm basis to monitor possible future stratospheric ozone depletion by manmade pollutants such as the chlorofluorocarbons. 

R. Grass spent 3 weeks at Melbourne, Australia, in August 1984, training 

Australian technicians in Dobson spectrophotometer operating procedures . 

Instructions were provided also, in optically aligning and calibrating the 

Dobson instruments. 

104 
W. Komhyr and R. Grass convened an International Comparison of Dobson 

spectrophotometers at Melbourne, Australia, 19 November to 10 December 1984, 

under auspices of the HMO. Participating countries were Australia, India, 

Japan, New Zealand, and the U.S.A. 

J. Peterson headed a U.S. delegation of five scientists to Vilnius, 

Lithuania, U.S.S.R., d~ring A~gust 1984 . The delegation participated in the 

Symposium on atmospheric trace gases affecting climate hosted by the U.S.S.R. 

under Horking Group VIII of the U.S.-U.S. S.R . bilateral agreement on 

protection of the environment. He gave talks on "The NOAA halocarbon and 

nitrous oxide measurement program," and "Results from AGASP." 

J . Peterson, (B. Mendonca, E. Dutton, G. Herbert, R. Gammon, P. Steele, 

and B. Bodhaine) participated in the conference "The Scientific Application of 

Baseline Observations of Atmospheric Composition" at Aspendale, Australia, in 

November 1984 . He presented a paper on "Measurements of atmospheric CO 2 at 

Barrow, Alaska, from the U.S. NOAA/GMCC program." 

P. Steele, visiting scientist from Australia, continued his appOintment 

at GMCC as an NRC-NOAA Research Associate up to 14 September 1984. He took 

over full management of the cooperative program between CSIRO, NOAA/GMCC, and 

OGC to measure CH4 and CO 2 concentrations by gas chromatography in flask air 

samples from the GMCC cooperative flask sampling network. He traveled to the 

SABOAC Conference held at the CSIRO Division of Atmospheric Research during 7-

9 November 1984 where he presented a paper on results from this cooperative 

program. While en route to this conference, visits were made to the New 

Zealand Meteorological Service (Atmospheric Physics and Chemistry Section) in 

Wellington, and to the cooperative flask sampling site located at Kaitorete 

Spit near Christchurch. Seminars were presented at the following 

institutions: Centre for Resource and Environmental Studies, Australian 

National University , Canberra ; Meteorological Department, Bangkok, Thailand; 

Department of Environmental Sciences, University of Lancaster, Lancaster, 

England . 

R. Schnell attended the 3rd Arctic Haze Symposium 

1983 where he presented a paper on the AGASP results. 

for the 2nd AGASP program were developed with Canadian 

in Toronto, Canada , May 

At the same time , plans 

counterparts. 

June 6-9, R. Schnell co-hosted the 2nd International Conference on Ice 

Nucleation Bacteria held in Flagstaff , AZ. Two papers presented at this 

conference bear his authorship . 

105 
9 . PUBLICATIONS AND PRESENTATIONS BY GMCC STAFF , 198~ 

Baker-Blocker , A., J . J. DeLuisi , and E. Dutton. Received ultra violet 

radiation at the South Pole . Solar Energy 32(5) : 659-662. 

Bodhaine , B. A. The GMCC aerosol program. Paper presented at The Scientific 

Application of Baseline Observations of Atmospheric Composition , 7-9 

November 198~, Aspendale , Australia . 

Bodhaine , B. A., E. G. Dutton , and J . J. DeLuisi. Surface aerosol 

measurements at Barrow during AGASP. Geophys . Res. Lett . 11(5)377-380. 

Bodhaine , B. A., E. G. Dutton, and J . J . DeLuisi . Surface aerosol 

measurements at Barrow. Paper presented at Third Symposium on Arctic Air 

Chemistry , 7- 9 May , Downsview , Ontario, Canada. 

Cowherd, C., G. E. Muleski , P. Englehart , and D. Gillette . Rapid assessment 

of exposure to particulate emissions from surface contamination sites. 

MRI Dr aft Report, Midwest Research Institute, Kansas City , MO . 

Dayan , U., J . M. Miller , D. W. Nelson. 

and evaluation of the first decade. 

The acidity of Samoan rain - trends 

NOAA Tech . Memo . ERL ARL-132 , NOAA 

Environmental Research Laboratories , Boulder , Colo ., 22 pp . 

DeLuisi , J . J ., T. DeFoor , K. Coulson , F. Fernald , and K. Thorn . Lidar 

observations of stratospher ic ap.rosol over Mauna Loa Observatory : 197~-

1981 . NOAA Data Report, ERL ARL-4, NOAA Environmental Research 

Laboratories , Boulder , CO , 107 pp. 

DeLuisi , J. J ., C. L. Mateer , and P. K. Bhartia . On the correspondence 

between standard Umkehr, short Umkehr and SBUV vertical ozone profiles. 

Proc . Quad . Ozone Symp., Halkidiki , Greece , 3-7 September 198~. 

DeLuisi , J . J., C. L. Mateer , and W. D. Komhyr. Effects of El Chichon 

stratospheric aerosol cloud on Umkehr measurements at Mauna Loa , Hawaii. 

Proc. Quad . Ozone Symp ., Halkidiki, Greece, 3-7 September 198~ . 

Dutton , E. G., J. J. DeLuisi , and B. A. Bodha ine . 

depth observed at Barrow , March 10- 20 , 1983. 

11(5):385-388. 

Features of aerosol optical 

Geophys . Res . Lett. 

Dutton , E. G., and J. J. DeLuisi . Interpretation of Apparent Atmospheric 

transmission usin g solar photometer precipitable water measurement . 

Extended abstracts of CSIRO conference on The Scientific Application of 

Baseline Observations of Atmospheric Composition , 7-9 November 198~, 

Aspendale, Australia . 

Fall, R. R., and R. C. Schnell. Association of an ice-nucleating Pseudomonad 

with cultures of the marine dinoflagellate , Heterocapsa niei. J. Marine 

Res . ~3:257-265 Fall, R. R., and R. C. Schnell. Bacterial i celnuclei of 

marine ori gin : some recent observations. Preprints , 11 Int. Conf . on 

Atmos . Aerosols, Condensation , and Ice Nuclei , Budapest, Hungary, 3-8 

September 19 8~ . 

106 
Fall, R. R. , and R. C. Schnell . Isolation of ice-nucleation active bacteria 

from marine sources. Preprints, 2nd American Conference on Ice Nucleating 

Bacteria, Flagstaff, AZ, 6-9 June 1984. 

Fraser, P. J ., M. A. K. Khalil, R. A. Rasmussen, and L. P. Steele. 

Tropospheric methane in the mid-latitudes of the Southern Hemisphere. J . 

Atmos. Chem .. 1 :125-1 35 . 

Gammon, R.H. The response of the global carbon cycle to climatic change. 

Presentation at EPA Symposium Rising CO 2 and Changing Climate : Forest 

Risks and Opportunities, Boulder , Colo, June 1984. 

Gammon, R. H. Atmospheric methane and climatic change . Presentation at Ocean 

Industry Sumposium, Woods Hole Oceanographic Institution, Woods Hole, 

Mass. , September 1984. 

Gammon , R. H. Carbon cycle trace gas distributions: results from the jOint 

U. S. /U . S.S.R. Pacific expedition SAGA of the RV KOROLEV, Fall 1983 . 

Presentation at the U.S./Soviet Symposium on Trace Gases and Climatic 

Change, Vilnius, Lithuania, September 1984. 

Gammon, R. H. , W. D. Komhyr , L. S. Waterman, T. J. Conway , and K. W. 

Thoning. Estimating the natural variation in atmospheric CO 2 since 1860 

from interannual changes in tropospheric temperature and the history of 

major El Nino events. Paper presented at the Chapman Conference on 

Natural Variations in Carbon Dioxide and the Carbon Cycle, Tarpon Springs , 

FL , 9-13 January 1984 . 

Gammon, R. H., W. D. Komhyr , L. S. Haterman, T. J . Conway, K. W. Thoning, and 

D. Gillette. The 1982/83 ENSO event: The response of the global 

atmospheric CO 2 distribution. Paper presented at the Conference on the 

Scientific Application of Baseline Observations of Atmospheric 

Composition, Aspendale , Australia, 7-9 November 1984. 

Grass, R. D. , and W. D. Komhyr. Traveling standard 

Dobson ozone spectrophotometers during 1981-83 . 

Halkadiki , Greece , September 3-7, 1984. 

lamp calibration checks on 

Proc. Quad. Ozone Symp ., 

Harris, J . M. Trajectories during AGASP. Geophys . Res. ~ett . 11(5):453-456. 

Harris, J. M. and E. C. Nickerson (eds). 

Change , No . 12: Summary Report 1983. 

Laboratories , Boulder , CO , 184 pp. 

Geophysical Monitoring for Climatic 

NOAA Environmental Research 

Hilsenrath , E., J. Ainsworth, A. Holland , J. Mentall, A. Torres, W. 

Attmanspacher, A. Boss , W. Evans , W. Komhyr, A. J. Miller , M. Proffitt, D. 

Robbins, S. Taylor, and E. Weinstock. Results from the balloon ozone 

intercomparison campaign (BOIC) . Proc. Quad. Ozone Symp., Halkadiki , 

Greece, September 3-7 , 1984. 

Komhyr, W. D., R. D. Grass , R. D. Evans , R. K. Leonard , and G. M. Semeniuk . 

Umkehr observations wi th automated Dobson s pectrophotometers. Proc. Quad . 

Ozone Symp. , Halkadiki, Greece , September 3-7, 1984. 

107 
Komhyr, W. D., S. J . Oltmans , A. N. Chopra, R. K. Leonard , T. E. Garcia , and 

C. McFee . Results of Umkehr , ozonesonde , total ozone , and sulfur dioxide 

observations in Hawaii following the eruption of El Chichon volcano in 

1982. Proc. Quad. Ozone Symp ., Halkadiki, Greece, September 3-7, 198~ . 

Komhyr, W. D, S. J . Oltmans, A. N. Chopra, and P. R. Franchois. Performance 

characteristics of high-altitude ECC ozonesondes. Proc. Quad. Ozone 

Symp. , Halkadiki, Greece, September 3-7, 198~. 

Mateer, C. L., and J. J. DeLuisi . A comparison of ozone profiles derived from 

standard Umkehr and short Umkehr measurements from 15 stations . Proc . 

Quad. Ozone Symp., Halkidiki, Greece, 3-7 September 198~ . 

Mendonca , B. G., J . J. DeLuisi, and E. G. Dutton. Atmospheric transmission 

decreases and stratospheric warming at Mauna Loa during the 2 years after 

the El Chichon volcanic eruption. Extended abstracts of CSIRO conference 

on The Scientific Application of Baseline Observations of Atmospheric 

Composition , 7-9 November 198~, Aspendale, Australia. 

Nickerson, E. C. On the role of mesoscale meteorological models in assessing 

the climatological impacts of urbanization in tropical areas. Paper 

presented at the WMO Technical Conference on Urban Climatology and its 

Applications with Special Regard to Tropical Areas. Mexico City, 26-30 

November 198~. 

Nickerson, E. C., D. Medal, E. Richard, and R. Rosset. Mesoscale numerical 

modeling of heavy precipitation events over mountainous terrain. Paper 

presented at the Fall AGU Meeting, San Francisco , CA, 5 December 1984. 

Parungo, F. , C. Nagamoto, J. Harris, B. Rosenuasser , and L. Ruhnke. Analyses 

of aerosol and precipitation samples collected during a transatlantic 

research cruise, NOAA Tech . Memo, ERL ESG-5, NOAA Environmental Sciences 

Group, BOulder, CO, 63 pp. 

Patterson, E., J. J . DeLuisi, B. Mendonca, R. Pueschel, R. Castillo, and T. 

Ackerman. Measurements of the absorption of cold water and unactivated 

within-cloud aerosols at Whiteface Mt., New York. Proc . International 

Radiation Symposium, 21-29 August 198~, Perugia, Italy. 

Peterson, J. T. Measurements of atmospheric CO 2 at Barrow, Alaska , from the 

U.S . NOAA/GMCC program. Paper presented at conference on The Scientific 

Applications of Baseline Observations of Atmsopheric Composition , 

Aspendale , Australia , November 198~. 

Peterson , J. T. Results from AGASP. 

Atmospheric Trace Gas Components 

U.S.S . R., August 198~. 

Paper presented at US-USSR Symposium on 

Affecting Climate , Vilnius , Lithuania , 

Peterson, J . T. The NOAA halocarbon and nitrous oxide measurement program. 

Paper presented at US-USSR Symposium on Atmospheric Trace Gas Components 

Affecting Climate, Vilnius, Lithuania, U.S.S.R., August 198~. 

Raatz , W. E. , and R. C. Schnell . Aerosol distributions and an Arctic aerosol 

front during AGASP: Norwegian Arctic, Geophys. Res. Lett. 11 :369-372. 

108 
Reinsel , G. C., G. C. Tiao , J. J . DeLuisi , C. L. Mateer , A. J. Miller , and J . 

E. Fredrick. Analysis of upper stratospheric Umkehr ozone profile data 

for trends and effects of stratospheric aerosols . J . Geophys . Res . 

89:4833- 4840 . --

Schnell , R. C. Aerosol measurements during the 

sampling program (AGASP) : March-April 1983. 

Symposium, Toronto, Canada, May 1984 . 

Arctic gas and aerosol 

Preprints , 3rd Arctic Haze 

Schnell , R. C. Arctic Haze : Editorial, Geophys. Res. Lett . 11 :359. 

Schnell , R. C. Bacterial ice nuclei and their role in the atmosphere. 

Preprints , 2nd American Conference on Ice Nucleating Bacteria , Flagstaff, 

AZ, 6- 9 June 1984 . 

Schnell , R. C. Condensation nuclei and aerosol size distribution measurements 

in Arctic haze. Preprints, 11 Int . ConC . on Atmos . Aerosols , 

Condensation , and Ice Nuclei , Budapest , Hungary, 3-8 September 1984 . 

Schnell , R. C. and W. E. Raatz . Vertical and horizontal characteristics of 

Arctic haze during AGASP: Alaskan Arctic , Geophys . Res. Lett. 11 :373-376 . 

Schnell , R. C .. Ar ctic Haze and the Arctic gas and aerosol sampling program 

( AGASP) , Geo ph ys. Res . Let t. 11: 361 - 3 64. 

Shapiro, M. A., R. C. Schnell , F. P. Parungo, S. J . Oltmans , and B. A. 

Bodhaine . El Chichon volcanic debris in an Arctic tropopa use fold. 

Geophys. Res . Lett. 11 : 421-424. 

Steele , L. P. , P. J . Fraser, R. A. Rasmussen , M. A. K. Kha lil , T. J . Conway , 

A. J. Crawf or d , R. H. Gammon, K. A. Masari e , and K. W. Thoning. The 

global distributi on of methane in t he troposphe r e . Paper presented at the 

Scientific Application of Baseline Observations of Atmospheric Composition 

(SABOAC) Conference held at CSIRO Division of Atmospheric Research, 

Aspendale, Victoria, Australia , 7- 9 November 1984. 

Winchester , J . W. , S. Li , S. Fan , R. C. Schnell , B. A. Bodhaine , and P. S. 

Nae gele . Coarse par ticle soil dust i n Arctic aerosols , spring 1984. 

Geophys . Res. Lett . 11 :995-998 . 

109 
AES 

AGASP 

AL 

ALE 

ARL 

ASCS 

ASR 

ATV 

BOIC 

BRIV 

CAF 

CAMS 

CDIC 

CIRES 

CN 

CNC 

CNL 

C02 

CSIRO 

DAS 

DC 

DEIV 

DOE 

DOY 

EC 

ECC 

EML 

ENSO 

EP A 

ERL 

FTS 

FSU 

GC 

G. E. 

GEOSECS 

GMCC 

GPCP 

GMT 

GSA 

GSFC 

HASL 

HP 

ICDAS 

IR 

ISIVS 

ITCZ 

JSC 

LBL 

LST 

10. ACRONYMS AND ABBREVIATIONS 

Atmospheric Environment Service, Canada 

Arctic Gas and Aerosol Sampling Program 

Aeronomy Laboratory , Boulder, CO (ERL) 

Atmospheric Lifetime Experiment 

Air Resources Laboratory , Silver Spring , MD (ERL) 

Alaska Soil Conservation Service 

Aerosols and Solar Radiation 

all terrain vehicle 

Balloon ozone intercomparison campaign 

Barrow Observatory , Barrow , Alaska (GMCC) 

Clean Air Facility 

Control and Monitoring System 

Carbon Dioxide Information Center , Oak Ridge , TN (DOE) 

Cooperative Institute for Research in Environmental Sciences, 

University of Colorado , Boulder 

condensation nuclei 

condensati on nucleus counter 

Crocker Nuclear Laboratory 

Carbon Dioxide , referring to CAMS 

Commonwealth Scientific and Industrial Research Organization, 

Austral ia 

data acquisition system 

direct current 

Distant Early Warning 

Department of Energy 

day of year, Julian 

elemental carbon 

Electrochemical concentration cell 

Environmental Measurements Laboratory (DOE) 

101 Nino-Southern Oscillation 

Environmental Protection Agency 

Environmental Research Laboratories , Boulder , CO (NOAA) 

Feder al Telecommunication System 

Flor i da State University 

gas chromatograph 

General Electric 

Geochemical Ocean Sections Study 

Geophysical Monitoring for Climatic Change , Boulder , CO (ARL) 

Global PreCipitation Chemistry Project 

Greenwich mean time 

Government Service Administration 

Goddard Space Flight Center (NASA) 

Health and Safety Laboratory (EPA) 

Hewlett-Packard 

Instrumentation Control and Data Acquisition System 

infrared 

Illinois State Water Survey 

Intertropical Convergence Zone 

Johnson Space Center (NASA) 

Lawrence Berkeley Laboratory (DOE) 

local standard time 

110 
MAP/GLOBUS 

MAP35 

MLO 

M03 

MSL 

NADP 

NARL 

NASA 

NCAR 

NCDC 

NESDIS 

NDIR 

NH 

NIP 

NILU 

NMC 

NOAA 

NRL 

NWR 

NWS 

NWT 

OGC 

PMEL 

PMOD 

PRC 

PV 

QBO 

SABOAC 

SAGA 

SBUV 

SEASPAN 

SEAREX 

SH 

SID 

SMO 

SUN YA 

SPO 

SRL 

SRBL 

SST 

TTO 

UIC 

URI 

USGS 

UV 

WMO 

WPL 

Middle Atmosphere Program/Global Budget of Stratospheric Trace 

Constituents 

MAP Precipitation Chemistry Project 

Mauna Loa Observatory , Hawaii (GMCC) 

Meteorology and Ozone 

mean sea level 

National Atmospheric Deposition Program 

Naval Arctic Research Laboratory , Barrow, AK 

National Aeronautic & Space Administration 

National Center for Atmospheric Research , Boulder , CO 

Nati onal Climatic Data Center, Asheville, NC 

National Environmental Satellite , Data , and Information Service 

nondispersive infrared 

Northern Hemisphere 

normal incidence pyrheliometer 

Nor wegi an Institute for Air Research 

National Meteorological Center , SUitland, MD 

National Oceanic and Atmospheric Administration 

Nava l Research Laboratory , Washington , D.C. 

Niwot Ridge , CO 

National Weather Service 

Northwest Territories (Canada) 

Oregon Graduate Center, Beaverton, OR 

Pacific Marine Environmental Laboratory, Seattle, HA 

Physikalisch-Meteorologisches Observatorium Davos 

Peopl es Republic of China 

photovoltaic 

Quasi- biennial oscillation 

Scientific Applicat i on of Baseli ne Observations of Atmospher i c 

Composition , CSIRO Conference , Australia 

Soviet-American Aerosol and Gas Experiment 

Solar backscattered ultraviolet 

SEAREX South Pacific Aerosol Network 

Sea-Air Exchange Program 

Southern Hemisphere 

Scri pps Institution of Oceanography, La Jolla , CA 

Samoa Observatory , American Samoa (GMCC) 

State Universi ty of New York at Al bany 

South Pole Observatory , Antarctica (GMCC) 

Smithsonian Radiation Laboratory 

Smithsonian Rad i ation and Biologi cal Laboratory 

sea surface temperature 

Transient Tracers in the Ocean 

Ukpiagvik Inupiat Corporation 

University of Rhode Island , Kingston , RI 

United States Geological Survey 

ultraviolet 

World Meteorological Organization , Geneva , Switzerland 

Wave Propagation Laboratory , Boulder , CO 

-u .s. GOVER NM ENT P R I NTING OFFI CE: 1 987-0-773-002/605 1 4