CO) 

rn 

o 

"'tI 

::3: 

< en 

~ 

,... 

~ 

~ -

o 

::ICI 

Z 

CO) 

"TI 

o 

::ICI 

n 

,... 

:z 

!=' 

...... 

A 

U.S. DEPART ME liT 

OF COMMERCE 

UTiDIIAl 

OCEAIIIC AIID 

ATMOSPHERIC 

ADMIIIISTRATIOII 

EIIVIROIIMEIITAl 

RESEARCH 

lABORATORIES 

Geophysical Monitoring 

for Climatic Change 

,-",,. 0, ('0 

4-.... ..,. 'sf ~+ 4'" , ~ ~ ~ 

~ ~ : \ . ~ f'o - ~. 

"""'TU Of p.+ 

No. 14 

arl Reporll B 8 5 

0(1 (e 

• 

· l 

• 
Geophysical Monitoring 

for Climatic Change 

No. 14 

Summary Report 1985 

Russell C Schnell , Editor 

Rita M. Rosson, Assistant Editor 

Air Resources Laboratory 

Geophysical Monitoring for Climatic Change 

Boulder. Colorado 

December 1986 

U.S. DEPARTMENT OF COMMERCE 

Malcolm Baldrige, Secretary 

National Oceanic and Atmospheric Administration 

Anthony J. Calio , Administrator 

Environmental Research Laboratories 

Vernon E. Derr, Director 
NOTICE 

Mention of a commercial company or product does not constitute an endorsement 

by NOAA Environmental Research Laboratories. Use for publicity or advertising 

purposes of information from this publication concerning proprietary products 

or the tests of such products is not authorized . 

,~ ak- i'~ the '-alllln:ll Technl.::)1 Inforlllallon Ser\lce. ~~85- PO ri Ro\'al Road 

~rnll!!iield . \.\ ::21ti1 

ii 
CONTENTS 

Page 

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

GMCC STATION INFORMATION •...•••.••••..•...••• .. •.••.... ..........•.•..... x 

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

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

2. 1 Matma Loa .......•.••••.••.•..•••••.••.••••• • .••.•.••.•••••• ••• • 3 

2. 2 Barr ow •••• . •••..•••• .•.•..• ••• •. • .•...• • •. .• •.. .••• . .•. ... •.• . 1 0 

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

2. 4 South Pole .•.........•.• •. •....••.• • .• • •.••...••..••....••• • . • 16 

3. AEROSOLS AND RADIATION MONITORIING GROUP ..•..•••.•. • ......•...•.... 21 

3. 1 Cont i nui ng Programs •.........•..•...•••..••........•.•..••...• 21 

3.2 Speci al Projects ••• • ••.••• • ••• ..••••. • •• ••• ••.••••••••.•..• • .. 35 

3.3 References .••••.••••.•••••.••••..•••...•..•••.•.••...••.••.••. 36 

4. CARBON DIOXIDE GROUP •• •• •• ••• ••• • ••••••••••••••••••••• • • •. ••••• • ••• 37 

4.1 Continuing Programs ..•. • .... •.•• •.. • . •• .•...•....... • •..••.•• • 37 

4.2 Special Projects •••••• •• • • ••• • •.•••••••••.•• • ••••••••• ••••• ••. 44 

4.3 References ..•........•....•...........•.•.•..........•..•..... 46 

5. TRACE GASES GROUP ••••.•••••.•..•.•.....•...•...•........•.••...•.•. 47 

5.1 Continuing Programs •. • • .. ••• • •• . .••..••••.••••••.•••.•••••••.• 47 

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

6. ACQUISITION AND DATA MANAGEMENT GROUP ••• • • • ••.• • •. . •••• ••• .•••.••• . 61 

6.1 Continuing Programs .• •• ...•.••.••.•••...•••..•••......•.... .. • 61 

6. 2 Special Projects ...•.•..•....•.•.•......•......•......•....... 68 

6.3 Refer ences •••••• • •. •• ••• •••• • •.• .• ••• ••.••• ••• ••. ••• • •..••• •• • 72 

7. AIR QUALITY GROUP •••••••.•••.•••••••••••••.••••••••••..••••.•••...• 73 

7.1 Continuing Programs ..••.•.•..•••..•••...••......•........•.... 73 

7.2 Speci al Projects •• •••• •.• .•••••••••• • .••• •• •.•• • ..••... • . . .•.. 85 

7. 3 References •...••.•....•......•.........•.••....•• •••• ...••.•.. 90 

iii 
8 . DIRECTORS OFFICE ...... .... .... . . •...... .•.. ........ . . .. . . .. . .. ..• . • 92 

8 . 1 Continuing Programs ..... . . . ........•......................... . 92 

Impact of Alkal i ne Aerosols on 

Precipitation Chemistry ...... . ................................ 92 

Precipitation Chemistry .........••......•......•.•.........•.. 95 

(R . S. Artz) 

8.2 Arctic Gas and Aerosol Sampling Program .. .• ...•..•.••........• 98 

Arctic Haze Above the Barrow Baseline Stati on ............. . ... 98 

( R. C. Schnell) 

8.3 Cooperati ve Programs .. .. .... •.. . ..... . . .. . •. .....•. •. . . .• ... . 1 03 

Monitoring for Sulfur Dioxide and Total 

Suspended Particulate at Mauna Loa Observatory ... . . .. . . ...•. . l03 

(Henry Yee, Wilfred Ching , and Richard Sasaki) 

The Global Precipi tation Chemistry Project .. .. ............... l05 

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

3 J. M. Milled 

ecl In Atmospheric Carbon Dioxide .... . .. . .. . ................ 108 

(Irving Friedman , Jim Gleason, and Augusta Warden) 

Following the Trail of AntarctiC Winds ..... •........ .. ..... .. 111 

(Eugene J . Mr'oz, Mohammed Alei , John H. Cappis, 

Paul R. Guthals , Allen S. Mason , and Donald J. Rokop) 

Some Results from UVB MeasUr'ements at Mauna Loa 

and Rockville , MD ........ ... ........... . .... ... ...... ..... . .. 114 

(Bernard Goldberg) 

LogistiC and Other Models for the Trends 

of Nitrous Oxide ..... .. ...... •. ... .....•.•................... 117 

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

Atmospheric Submicron Particle Collection at the SPO ......... 121 

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

Washout Ratios of Nitrate , Non-Sea-Salt Sulfate , and Seasalt on Virginia Key , Florida and American Samoa ...... 124 

(Dennis L. Savoie , ~9~eph M. erospero , and Ruby T. Nees) 

Seasonal Variations of Pb and '(Be 

at Mauna Loa and Barrow .•.................................... 127 

(Richard Larsen and Herbert Feely) 

Radioactivity at Barrow and Mauna Loa 

Following the Chemobyl Accident .......................... . .. 130 

(Richard Larsen and Z. Russell Juzdan) 

Experimental Sampling of Atmospheric Methane .•............... 133 

(Lester Machta, Kirby Hanson, and Monte Poindexter) 

9. INTERNATIONAL ACTIVITIES ................... . ...................... 134 

10 . PUBLICATIONS AND PRESENTATIONS BY GMCC STAFF ..... •. . . .... ...... . . . 137 

11 . ACRONYMS ......................................................... 144 

iv 
Mauna Loa Obse~vato~y afte~ the const~uction of the lava 

dive~sion embankments in 1985 . (U.S.C.S . photo by J. P. Lockwood.) 

v 

GMCC Staff , 1985 

Director's Office 

James Peterson, Director 

Bernard Mendonca, Deputy Directory 

Jeanne Kelsey, Secretary 

Roland Christofferson, CIRES 

Edwin Flowers, CIRES 

Dale Gillette, Physical Scientist 

Paul David Herrera, CO-OP 

Lori Neff, Scientific Data Clerk 

Everett C. Nickerson, Meteorologist 

Rita Rosson, Clerk-Typist 

Russell Schnell, CIRES 

L. Paul Steele, CIRES 

Paul Stockton, Physical Science Aid 

Delois Roberson, CO-OP 

Thomas Watson , Physical Science Aid 

David Wuertz, CO-OP 

Acquisition and Data Management Group 

Gary Herbert, Chief 

Karen Ciocchetti , Secretary 

Sandra Furney, Secretary 

Richard Clark, Computer Programmer 

Richard Cook , Physical Science Aid 

Teresa Davenport , Physical Science Aid 

Joyce Harris, Computer Specialist 

Troy Higgins, Jr. Fellow 

Steve Roughton, Computer Assistant 

Kenneth Thaut, Electronic Technician 

Aerosols and Radiation Monitoring Group 

John DeLuisi, Chief 

Karen Ciocchetti, Secretary 

James Baumhover, Electronic Technician 

Barry Bodhaine, Meteorologist 

Fernando Congeduti,-Guest SCientist 

Ellsworth Dutton, Meteorologist 

Jeffrey Guerrieri, Engineering Technician 

Rudy Haas, Mathematician 

Gerard Jennings, NRC 

David Longenecker, CIRES 

David Massey, Physical Science Aid 

Hong Minh, Engineering Technician 

Linda Mitchell, CIRES 

Kevin Moore, Physical Science Aid 

Donald Nelson, Meteorologist 

Tony Puig, Physical Science Aid 

Timothy Quakenbush , Physical Science Aid 

Patrick Reddy, CIRES 

Traci Simms, Physical Science Aid 

Lois Stearns, Meteorologist 

vii 
Ai~ Quality G~oup 

Joseph Boatman, Chief Sand~a F~ney, Sec~eta~y 

Ma~k Cichy , CO-OP 

La~een Gunte~, Meteo~ologist 

Helmut Ho~vath, CIRES 

Menachem Lu~ia, NRC, Post Docto~ate 

He~man Sieve~ing , Guest Wo~ke~ 

Ka~en Stamminge~ , Physical Science Aid 

Slavko Cvencek, Physical Science Aid 

Cha~les VanValin , Resea~ch Chemist 

Dennis Wellman, Enginee~ 

Stan Wilkinson, Meteo~ologist 

Ca~bon Dioxide G~oup 

Piete~ Tans, CIRES 

Lee P~ende~gast, Sec~eta~y 

Rita B~own, Sec~e ta~y 

Dana Fleming, Sec~eta~y 

B~ian Ande~son, Physical Science Aid 

C~aig Ave~an, CO-OP Te~esa Bals, CO-OP 

David Bont~age~ , Physical Science Aid 

Thomas Conway , Resea~ch Chemist 

Ellen DeMoney , CIRES 

Duane Kitzis, CIRES B~adley Halte~, Meteo~ologist 

Kenneth Masa~ie, CIRES 

John Pa~ke~, CO-OP Ki~k Thoning, CIRES 

Lee Wate~man, Chemist 

Monito~ing T~ace Gases G~oup 

Walte~ Komhy~, Chief 

Lee P~ende~gast, Sec~eta~y 

Rita B~own, Sec~eta~y 

Dana Fleming, Sec~eta~y 

Sean Coleman , Physical Science Aid 

Egan, Keith , CIRES Robe~t Evans, CIRES 

Ma~k Fish, Physical Science Aid 

Paul F~anchois, CIRES 

Robe~t G~ass, Physicist Glo~ia Koenig, Compute~ P~o~amme~ 

Kent Leona~d, CIRES 

Samuel Oltmans , Physicist F~ank Polacek, III, Meteo~ological Technician 

G~ego~y M. Siedelbe~g , CIRES 

Thayne Thompson, Phsicist 

Ronald Tho~ne, Enginee~ing Technician 

Thomas Stewa~t , Physical Science Aid 

Glenn Weile~, Physical Science Aid 

viii 
Barrow Observatory 

Daniel Endres , Station Chief 

Steve Ryan , Station Chief 

James Wendell, Electronic Technician 

Mauna Loa Observatory 

Elmer Robinson, Director 

Judith Pereira, Secretary 

Arne Austring , Physical Scientist 

John Chin , Physicist 

Thomas DeFoor , Electronic Engineer 

Thomas Garcia , Meteorological Technician 

Dorothy Johnson , Physical Science Aid 

Barbara Kerecman, Data Clerk 

Darryl Kuniyuki , NOAA Jr. Fellow 

Stephen Lent , Physical Science Aid 

Mamoru Shibata, Electronic Technician 

Alan Yoshinaga , Chemist 

Samoa Observatory 

Steve Ryan , Station Chief 

Donald Nelson, Station Chief 

Roger Williams, Electronic Technician 

Meridith E. Wilson, Electronic Technician 

Efaraima Peau , W. G. Laborer 

South Pole Observatory 

James Waddell, NOAA Corps, Station Chief 

Mark Mihalic , Electronic Technician 

Clifford Wilson, NOAA Corps, Station Chief 

Bradley Halter , Electronic Technician 

ix 
Name: 

Latitude : 

Longitude: 

Elevation : 

Time Zone: 

Office Hours: 

Telephone -

Barrow (BRW) 

71 . 3233 

156.6067 

o km 

GMT -9 

8:00am- 5:00pm 

Office hours: (907) 852-6500 

x After hours: (907) 852-6500 

Postal Address: Officer in Charge 

NOAA/ERL/ARL/GMCC 

Pouch 8888 

Barrow, AL 99723 

Freight Address: 

GMCC Station Information 

Mauna Loa (MLO) 

19 . 533 

155.578 

3.4 km 

GMT -10 

8:00am-5:00pm 

(808) 961-3788 

(808) 961-3788 

US Dept . of Commerce 

NOAA - Mauna Loa 

Observatory 

P.O. Box 275 

Hilo, HI 96720 

US Dept. of Commerce 

NOAA - Mauna Loa 

Observatory 

154 Waianuenue Ave . Hilo, HI 96720 

Samoa (SMO) 

-14.2522 

170.5628 

Okm 

GMT -11 

8:00am-5:00pm 

011-(684) 622-7455 

011-(684) 699-9953 

US Dept. of Commerce 

NOAA - GMCC Samoa 

Observatory 

P.O. Box 2568 

Pago Pago, American 

Samoa 96799 

South Pole (SPO) 

-90 . 000 

0.000 

2.8 km 

GMT +12 

8:00am-5:00pm 

Relayed through 

GMCC Boulder 

Officer in Charge, 

GMCC Program 

Box 400 USARP 

C/O NAVSUPPFORANTARCTICA 

FPO San Francisco, 

CA 96692 

ATTN : South Pole #S-257 

S. Kuester 
GEOPHYSICAL MONITORING FOR CLIMATIC CHANGE 

NO. 14 

SUMMARY REPORT 1985 

1. SUMMARY 

At MLO, the major facilities change was construction of lava diversion 

embankments. The diversion system, which hopefully will never be tested, was 

designed to divert a flowing lava stream around the observatory. Upgrade of 

the lidar system continued. It detected an enhanced stratospheric aerosol 

layer late in the year, presumably the result of the November eruption of 

Nevada del Ruiz in Columbia. A new solar radiation program was begun cooperatively with the University of Arizona. The program goal is to study 22-year 

variability in solar constant as measurable at ground level. 

At BRW, the long-term problem of availability of reliable electrical 

power was solved with an agreement with the USAF DEW line facility to supply 

power to the observatory. A major cost savings was achieved by arranging for 

annual shipment of gas tanks by barge rather than regular shipments by air. 

LBL discontinued their long-running cooperative aerosol measurements when the 

project leader took a position in a private company. 

At SMO, our long-term Station Chief and Electronic Technician took new 

NOAA jobs in Boulder, resulting in a completely new station staff. The photovoltaic system performed well , providing uninterrupted power to several 

projects. The ALE/OGe cooperative halocarbon monitoring project was improved 

with the installation of upgraded gas chromatographs. 

At SPO, the new crew mod ified the CAF floor plans. The remodeling was 

done to improve efficiency of operations , sampling intake lines, and reliability of power. Drifting snow around CAF continued; plans have been drafted 

to raise CAF next year. There were few changes in NOAA and cooperative 

scientific programs during the year. 

The ongoing GMCC core measurement programs continued. These programs 

include measurements of CO2 from the flask network and observatories , total 

column ozone, ozone vertical distribution by ECC sonde and Umkehr technique, 

surface ozone, stratospheric water vapor by balloon soundings at Boulder, 

CFC-11 and -12 and N20 from flask samples, stratospheric aerosols at MLO using 

lidar, aerosol light scattering and CN concentration, direct and diffuse solar 

radiation, meteorological variables, and chemistry of precipitation. 

In the Aerosols and Radiation Group, the observatory CN records, all at 

least 10 years long, show no significant long-term trends. A first assessment 

was completed of upward- and downward-directed solar and longwave radiation 

measurements at Barrow. The MLO concurrent Umkehr ozone and lidar aerosol 

profiles following the El Chichon eruption were used to confirm theoretical 

aerosol corrections to long-term Umkehr measurements. Administratively, the 

ARL Solar Radiation Facility was transferred to the ARM Group. The facility 

maintains U.S. radiometric standards and calibrates instruments for the NOAA 

solar network. 
The Ca~bon Dioxide G~oup continued in situ CO2 meas~ements at the obse~vato~ies and flask analyses of CO2 and CH4 at 2b sites. The mean global 

CO2 1985 inc~ease was about 1.2 ppm . A ~epo~t by Komhy~ et al. (1985) gives a 

complete histo~y and comp~ehensive analysis of the CO2 flask sampling net o~k 

t~ough 1982 . The 1985 methane global ~owth ~ate ave~aged about 0.9%. 

Sampling of CO2 in the ai~ and ocean su~face wate~ du~ing a May-July oceano- g~aphic c~uise showed equato~ial pC02 values as high as 500 ppm . 

The T~ace Gases G~oup continued the Dobson total ozone meas~ement ~eco~d 

at 14 sites and its inte~national calib~ation wo~k . The South Pole ~eco~d 

shows la~ge Octobe~-Novembe~ dec~eases , pa~ticula~ly du~ing the 1980 's, now ~efe~~ed to as the Anta~ctic Ozone Hole . The NESDIS SBUV/2 p~og~am continued 

with ozone p~ofiles by Umke~ at five sites and by ECC sonde at t~ee sites. 

The 12-yea~ s~face ozone meas~ements at BRW and MLO show long-term , significant inc~eases. Regula~ balloon soundings of st~atosphe~ic wate~ vapo~ 

continued. We continued to take flask samples at the obse~vato~ies fo~ CFC11, CFC-12, and N20. As pa~t of RITS, a gas c~omatog~aphic system was 

designed and pu~chased fo~ in situ, continuous meas~ements at the obse~vato~ies of these species. 

The Acquisition and Data Management G~oup ~epo~ted the meteo~ological 

data f~om the obse~vato~ies. The annual dist~ibution of wind di~ection was nea~ normal, but wind speeds we~e significantly g~eate~ (than no~mal) at SMO 

and sightly ~eate~ at SPO. The new data acquisition systems installed du~ing 

1984 a~e mo~e ~eliable than thei~ p~edecesso~s. The ai~ mass t~ajecto~y 

p~og~am was imp~oved with the capability fo~ computations ove~ Southe~n Hemi- sphe~c pola~ ~egions, which was tested via compa~ison to South Pole meas~ements of sea salt ambient ae~osol . Nume~ous t~ajecto~ies we~e computed fo~ 

NOAA ~esea~che~s and affiliates at unive~sities and othe~ agencies. 

An administ~ative change t~ansfe~~ed the ARL Ai~ Quality Division to GMCC 

as the Ai~ Quality G~oup. P~ojects unde~taken by the G~oup included: cont~ibution of nat~al sulfu~ emissions f~om the Gulf of Mexico to the No~th 

Ame~ican total sulfu~ budget; compute~ simulation of the nat~al sulfu~ cycle 

in the ma~ine bounda~y laye~; mechanism by which ae~osols a~e ~eleased to the atmosphe~e by evapo~ating clouds; the ~ole of thunde~storm convective 

p~ocesses in the ve~tical t~anspo~t of ai~ pollutants; pa~ticipation in WATOX 

to determine the flux of anth~opogenic emissions f~om the easte~n edge of the 

No~th Ame~ican continent; installation and imp~ovement of scientific inst~uments on the NOAA King Ai~ ai~c~aft; deposition of sulfu~ pa~ticles 

du~ing high wind-speed conditions; and G~and Canyon wind flow patte ns when 

visibility is ~educed du~ing cont~olled fo~est bu~ning pe~iods . 

Within the Di~ecto~'s Office, ~esea~ch is continuing on the effects of 

nat~al sou~ces of alkaline mate~ials (wind-blown soil ae~osol , and ~oad dust) 

on p~ecipitation chemist~y p~ecipitation and on chemical analyses of p~ecipitation samples collected at the obse~vato~ies and a six-site netwo~k in 

Hawaii. Many data analyses f~om AGASP flights du~ing 1983 we~e published . Planning fo~ AGASP-II du~ing Ma~ch-Ap~il 1986 was well unde~way. Many 

scientists f~om unive~sities and othe~ institutions used the obse~vato~ies fo~ 

coope~ative ~esea~ch. This ~epo~t includes summ~ies f~om seve~al p~ojects . 

2 
2. OBSERVATORY REPORTS 

2.1 Mauna Loa 

FACILITIES 

The MLO ~esea~ch and monito~ing p~og~am was ca~~ied out th~ough the yea~ 

without majo~ dis~uptions in the co~e obse~vations. The CAMS units pe~fo~ed 

well , and essentially complete data ~ecove~y was achieved. 

A majo~ const~uction p~og~am was ca~~ied out at the end of the yea~ when 

the long-planned lava dive~sion embankments we~e const~ucted. The design of 

the dive~sion system was developed by USGS Hawaiian Volcanoes Obse~vato~y. 

The embankments, upslope f~om MLO, we~e bulldozed f~om the on-site lava and 

designed so that a flowing lava st~eam would be dive~ted a~ound the MLO 

site. Lava embankments we~e used successfully du~ing a 1983 e~uption of Mt. 

Etna in Sicily to dive~t a lava flow and p~otect seve~a l facilities (Lockwood 

and Romano, 1 985) . 

The ozonesonde p~og~am, begun in Decembe~ 1984 with NOAA NESDIS suppo~t, 

was continued on app~oximately a weekly schedule t~ough the yea~ using the 

NWS ~adiosonde facility at Hilo ai~po~t. 

Lida~ obse~vations continued on a weekly schedule , sky conditions 

pe~mitting. In Novembe~ and Decembe~ a cha~acte~istic st~atosphe~ic volcanic 

cloud signal was detected , which appa~encly was due to the 13 Novembe~ 1985 e~uption of Nevada del Ruiz in Columbia. The upg~ade of the MLO lida~ with 

EPA g~ant suppo~t continued t~oughout the yea~. 

The Pu'u 0 ' 0 vent of Kilauea volcano e~upted pe~iodically, on an almost ~egula~ 27 - day schedule, t~oughout the yea~. The~e was no impact, gene~ally, 

on MLO ope~ations o~ data, although occasionally an outgassing Kilauea plume d~ifted past the Obse~vato~y . 

In August IAMAP held a 2-week-Iong meeting in Honolulu . MLO staff 

attended and pa~ticipated in the meeting. Visito~s in August totaled mo~e 

than 90 , mainly lAMAP attendees , including many fo~eign scientists , and an lAMAP-o~ganized tou~. 

An eme~gency, b~eak-glass-to-use telephone has been installed at MLO fo~ 

public use in case of eme~gencies on the mountain . 

PROGRAMS 

The p~incipal p~og~ams conducted at MLO du~ing the yea~ a~e listed in 

table 1. Those inst~uments ~eco~ded continuously by the CAMS a~e indicated by 

• B~ief comments on some of the individual p~og~ams follow. 

3 
Table 1.--Summary of sampling programs at MLO i n 1985 

Cases 

CO2 

Program 

CO2 and CH4 

Sur-face ozone 

Total ozone Ozone prof 11 e 

CfC-l1 , CFC-12 , and N20 

Aerosols 

Condensation Nuclei 

Optical properties 

Stratospheric aerosols 

Solar Radiation 

Global irradiance 

Direct !rradiance 

Dlffuse lrradia~ce 

TW"bidity 

Meteorology 

Air Temperature 

Dewpolnt temper-ature 

Relative humIdity 

Pre.ssur'e 

Wind (speed and direction) 

Precl pi tation 

Total precipitable water 

Precipitation Chemistry 

pH 

Conducti vity 

Chemical components 

Cooperatl ve Programs 

CO2 (~30) CO2, C, N20 (S ID ) 

Surface SD? (r3A)'2 CO2, CO . cR4, CI C 

(CS I RO) 

C02 ' CHq and other trace 

gases (NCAR) 

HNO~ and Hel vapor 

(Colorado College) 

Instr'tment 

Sal'l'Ipl ing 

Fr'equency 

Remarks 

------------- ----------------------

URAS~2T infrared analyze/,Ii 

3-L glass nask.~ 

O.5-L glass flasks , p3 

D.5-L glass flasks, tht"ough analyzer 

5-L evacuated glass flasks 

Gas chrc:xnatogt"aph 

Dasi bi ozone meteril 

Dobson spectrophotometer no. 76 

Dobson spectrophotcmeter no. 76 

Balloontx)I'ne ECC sonde 

300-mL stainless steel flasks 

Pollak CNC 

G. E. CNCiI 

rour-wavelength nephelc:xneterLidar 

Continuous 1 pai!' w.-:- I 

1 pair wl<-1 

lpai:, wk- I 

1 pairW\(-l 

Conti nuous 

Conti~vollS 

3 day 2 day-l 

1 , .. 1.:- 1 

I pai t"Wk- 1 

Discrete 

Continuous 

Continuous 

Discrete 

Eppley pyranometers (3) wi th Q , Continuous 

OGl , and ReB rilters· 

Eppley pyrhelic:xneters (2) with Q Continoous 

f 11 terEppley pyrheliO'lleter wi th Q , OG1 , 3 day -1 

RG2 , and ReB filters 

Eppley/Kendall active cavity Discrete 

radiometer 

Eppley pyranometer with shading disk Continuous 

and Q filter· 

J-series 1982 sunphotc:xneters 3-day-l 

Pt-'()D three-wavelength sunphotanete!,iI Continuous 

Thermistor (aspirated)! 

Max .-min . thermaneters 

Hygrothermograph 

Dewpoint hygrO'lleter! 

Hygrothermograph 

CapaCitance transducer! 

Mlcrobarograph 

Mercurial barometer 

Bendix Aerovane· 

Rain gauge , 8-in 

Rain gauge , 8-1n 

Rain gauge , weighing bucket 

Rain gauge , tipping bucket-t 

Foskett infrared hygrometerHAD Infrared hygrometeril 

pH meter - Hilo lab . 

Conducti vi ty bridge H Uo lab . 

Ion chromatograph - Hilo lab , 

Infrared analyzer (Applied Physics) 

5-L evacuated glass flasks 

Chemical bubbler system 

Pressurized glass flask sample 

Evacuated stainless steel flasks 

Special sampling system 

4 

Conti::tyous 

1 day 

Continuous 

Co ntinoous 

Contimnus 

Continuous 

conti::ty:'US 

1 day 

Conli~1fus 

1 day 

1 wk- 1 

Continuous 

Continuous 

Continoou.s 

Continuous 

Weekly 

Weekly 

''':eekly 

Conti nuaus 1 pait" wk- I 

Evet'Y 12 days 

I mo- 1 

1 pair '.lk- 1 

4 periods y(,-1 

"LO 

MLO and K1JJ\ukahl 

(seacoast) 

/oW and Kunukahi 

t·1LO 

m.o and K1JJ\ukah i 

rolLO 

MLO 

Weekdays 

Umkehr 

From lIilo Air~rt 

MLO 

Weekdays 

450 , 550 , 700 , 850 nm 

694 . 3 nm; aV~1age 1 

p!'oflle wk 

'eekdays 

Weekdays 

''':eekdays 

Weekdays 

380, 500 , 778 , 862 run ; 

nat'rowband 

380 , 500 , 778 run ; narrowband 

2-m height 

Standard shelter 

rolLa and Kulani Ha uka 

2-m height 

f-!LO and Kulani Mauka 

(8300 ft) 

6-m height 

Kulani Mauka 

Weekly chart record 

Program began Oct . 

Rainwate!' collectiOns , 

5 sites 

Rainwater collections, 

5 sites 

Rainwater collections , 

5 sites 

M..O and Kunukahi 

24-h (0000-2400) sample 

MLO 

/OlLO and K unukah i 
Table 1.-- Summa~y of sampling p~og~ams at MLO in 1985--Continued 

Programs Instrument 

Cooperative Prosrams--Cont . 

Total suspended particles High-volume sampler 

(OOE) 

Total suspended partIcles High-volume sampler 

( EPA ) 

Ultraviolet radiation 

(Temple Unlv.) 

Ultr'avloiet radiation 

(Smithsonian) 

Solar varlabilityt 

(Unlv. of Arizona) 

Solar Aureole Intensltyt 

(Colo . State Unlv .) 

Precipitation collection 

(OOE) 

PrecipItatIon collection 

(ISWS) 

Precipitation collection 

(Univ . of VIrginia) 

Wet-dry deposition 

(ISWS) 

Aerosol chemistry 

3

(Untv. of Washington) 

1 C (USGS . Denver) 

Carbon monoxi de 

(Max Planck Inst.) 

Various trace gases 

(0<X) 

Ultraviolet radi ometer (e rythema) 

1-wavelength UV radiometer 

Solar photometer 

Mul ti-aperture tracking photomet er 

Exposed collection pails 

Aerochemetric automati c collector 

Aerochemetric automati c collector 

Aerochemetric automatic collector 

Nuc lepore fi I ters 

lO-L stainless steel flasks 

Chemical reaction with HgO 

Stainless steel flasks 

'Indicates progra~ recorded by CAMS. 

tIndicates new program initiated during 1985. 

Ca~bon Dioxi de 

Sampling 

frequency 

Continuous 

1 filter wk- l 

Re'Ilarks 

Every 12 da ys 24-h (0000-2400) sample 

Continuous Radiation responsible for 

sunburning of skin 

Continuous 295- 325 nm , narrowband 

Discrete Program began Sept . 

Continuous Program began Jan. 

Continuous 

Continuous Analysis for 7Be and lOBe 

Continuous Organic acid analysis 

Continuous NADP 

Continuous Upslope-downslope discrimi nati on Biweekly 

Continuous 

1 set wk- 1 MLO and Kumukahi 

<3 flasks) 

Atmosphe~ic CO2 was monito~ed continuously using both the GMCC URAS-2T inf~a~ed analyze~ and an automatic gas chromatog~aph with a flame ionization detecto~. The SIO Applied Physics infra~ed analyze~ was also ope~ated in 

pa~allel with the GMCC systems. Prelimina~y ~esults f~om the GMCC URAS system 

indica~~ that the ~ate of CO2 increase fo~ 1985 was app~oximately 1.33 

pj:m y~ . 

The weekly CO2 flask sampling p~og~ams at MLO and Cape Kumukahi, the easte~nmost point on the island, were continued du~ing the yea~. It is 

usually expected that CO2 concent~ations at Kumukahi will be slightly highe~ 

than those at MLO. In the past 9 yea~s , 1976 through 198~ , Kumukahi values 

have averaged 0.3 ppm highe~ while the diffe~ences ~anged f~om a to 0.8 ppm. 

As in past yea~s, outgassing f~om the volcanic calde~a at the summit of 

Mauna Loa and f~om vents along the no~theast ~ift caused dis~uptions of some 

of the CO2 ~eco ds in each month of the year . These events occu~~ed mainly 

between 0000 and 0800 LST during the downslope wind regime . Since these 

disruptions a~e ~eadily detectable in the inst~ument ~eco~ds, they can be 

excluded f~om the concentration data and do not influence the MLO CO2 ~eco~d . The f~equency of the 1985 monthly occur~ences is listed in table 2. 

5 
Table 2. Monthly occu~~ences of outgassing f~om the 

volcanic calde~a on Mauna Loa du~ing 1985 

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

No. of days 10 20 13 11 19 20 15 21 9 17 12 9 176 

Pe~cent of 32 71 42 37 61 67 48 68 30 55 40 29 48 

days 

The 1985 f~equency of outgassing events, 48%, is a significant decr'ease 

fr'om the 61% f~equency that occur'~ed in 1984 in the 8 months following the 

1984 Mauna Loa er'uption. Both values a~e significantly g~eate~ than the p~ee~uption 5-y~ aver'age f~equency of 27%. It should be noted that these f~equencies r'elate to the number' of occu~~ence days and not to the numbe~ of 

hour-s of data that a~e affected; most events last only about an hou~ o~ so. 

Ozone 

Ozone measu~ements we~e made using th~ee sepa~ate p~ocedu~es: total 

sUr'face ozcne using the Dasibi UV photometer'; total ozone in the atmosphe~ic 

column, and the t~opospher'ic and str'atospher'ic ozcne p~ofile using the Umkeh~ 

technique and automated Dobson instr'ument no. 76; and ozcne pr'ofiles to about 

40 km on a weekly baois using ECC ozonesonde systems. The automated Dobson inst~ument is set to take daily mo~ning and afte~noon Umkeh~ measu~ement 

sequences, although the after'noon obse~vation is f~equently affected by 

upslope st~atus cloud fOr'mations. Total ozcne Dobson measur-ements ar'e 

initiated manually thr'ee times a day when sky conditions pe~mit . The ECC 

ozonesonde flights ar'e made on a weekly schedule f~om the NWS ~adiosonde 

facility at the Hilo ai~po~t and a~e suppo~ted by NOAA NESDIS. In 1985 52 

flights we~e launched, of which 46 Or' 88% we~e successful in ~eaching the 

ozone laye~ . The maximum altitude attained by an ozonesonde was 42 km, and 

70% of the successful flights ~eached 39 km o~ higher'. When possible the 

ozcnesonde flights wer'e scheduled to coincide with over'passes of the NOAA-7 

satellite , which car'~ies ozone pr'ofiling instr'umentation . 

SUr' face ozcne concent~ations we~e obtained near'ly continuously using the 

Dasibi UV photomet~ic inst~ument. Calibr'ations wer'e car'~ied out on a r'egula~ 

weekly schedule. 

Su~face Ae~osol Measur-ements 

Thr'ee inst~uments we~e in use to cha~acte~ize the sur-face ae~osol 

pa~ticles: the G.E. CNC, the Pollak CNC, and the nephelometer'. 

The G.E. CNC oper'ated continuously with only occasional maintenance o~ 

mechanical p~oblems. The Pollak counter' was ope~ated in the nOr'mal manner' du~ing the yea~ and ser'ved as a convenient calib~ation check on the pe~for'mance of the continuous G. E. CNC system. The nephelometer' was placed 

back into ser'vice in May afte~ an extended per'iod in GMCC Boulde~ labo~ator'ies 

fo~ r'ebuilding and calib~ation . 

6 
Stratospheric Aerosols-Lidar 

Lidar observations were carried out , sky conditions permitting, on 

approximately a weekly schedule. When possible lidar observations were 

correlated with SAGE II satellite overpasses so that the lidar profiles could 

be coordinated with the SAGE aerosol experiments. A total of 52 observations 

were made during the year. The stratospheric aerosol loading from the spring 

1982 El Chichon eruption continued the decreasing trend established in 

previous years and apparently approached a pre-El Chichon background in 

November 1985 . 

During 1985 work supported by an EPA grant to upgrade the MLO lidar 

system was continued . This upgrade wi ll include new optical components , a 

redesigned mounting configuration , and improved data acquisition systems. 

Completion is expected in early 1987. 

Meteorology 

Meteorological measurements were continued without major problems during 

1985. The tipping-bucket rain collection system was installed in October to 

provide input signals to the CAMS and the daily weather report. 

Solar Radiation 

No major changes were made in t he MLO solar radiation program. There are 

several components in this system: continuous solar and total-sky measurements 

using both stationary and tracking instruments ; discrete broadband and 

narrowband observations on a routine, weather- permitting basis; discrete 

manual, hi gh-precision observations ; and calibrations and intercomparisons of 

instruments using MLO facilities and instruments as working standards. All of 

these activities continued in 1985 . 

A normal incidence pyrheliometer with Q filter , three global pyranometers 

with Q, OG1, and ReB cutoff filters, and a diffuse Q pyranometer with shading 

disk were operated throughout the year to obtain continuous radiation 

measurements. A filter-wheel pyrheliometer wit h Q, OG1, RG2 , and RG8 cutoff 

filters was operated to obtain discrete broadband radiation measurements . 

Transmission generally increased slightly as the year progressed . Turbidity 

measurements were obtained with hand-held sunphotometers J202 (380 and 500 nm) 

and J314 (778 and 862 nm ) throughout t he year . 

The active solar tracker and the 32-channel CAMS 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. Instruments mounted in the solar 

dome included a normal incidence pyrheliometer , an infrared water vapor meter, 

a three-wavelength PMOD sunphotometer, and an active cavity radiometer . 

The MLO solar radiation program was augmented by a number of cooperative 

programs . 

7 
P~ecipitation Chemist~y 

The GMCC p~ecipitation chemist~y p~og~am continued without difficulties at 

about the same level of activity as in p~io~ yea~s. The usual MLO pro~am 

consists of the collection and analysis of precipitation collected at five 

local sites, although the coastal site at Cape Kumukahi was out of service for 

many months because of repeated vandalism. MLO also carries out the analysis 

of precipitation samples collected on the Island of Kauai and at the GMCC 

observatories at Barrow, Samoa, and South Pole. Weekly snow or rain samples 

are collected at these GMCC sites. Samples are analyzed in the MLO Hilo 

laboratory for pH and conductivity. Both anions and cations are determined in 

these samples using ion c~omatography. Seve~al cooperative pro~ams in 

precipitation and deposition chemistry augment the GMCC prog~am. 

COOPERATIVE PROGRAMS 

The large number of cooperative pro~ams at 

operation and with little change t~ough 1985. 

and a brief summary of some of these activities 

MLO continued in normal 

These are listed in table 1, 

follows. 

The program of high-p~ecision BUV radiation measurements at seven 

wavelengths (295-325 nm) was continued at MLO by the Smithsonian Institution 

Radiation Biology Laboratory as was the erythema (sunb~n) radiation data 

gathered at MLO for a number of years by Temple University. These two sets of 

data are important in assessing the potential impact of changes in the ozone 

layer. 

Precipitation collection for chemical analysis continued, and there were 

several cooperative investigator pro~ams in this research area. Collections 

of precipitation for organic acid analysis for the University of Virginia and 

for beryllium 7 and 10 analyses for the ISWS continued, as did sample 

collections for DOE and NADP. 

Aerosol particle samples were collected for the University of Washington 

on a weekly schedule using Nuclepore filters. This program used a sample~­

controller discriminating on the basis of time of day, wind speed, wind 

direction, and Aitken nuclei count. The p~pose of this controller is to 

separate sample collections according to upslope and downslope air 

trajectories and to exclude calm conditions. Downslope air should be 

representative of mid-tropospheric conditions whereas upslope air masses may 

contain various amounts of material with a recent origin at the earth's 

surface. Total particle filters were also collected for DOE. High-volume 

filter samples were collected for EPA using standard EPA methods with one 24-h 

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

began in 1971, although there have been some significant breaks in the 

record. Annual geometric ~3an values for total suspended particles appea~ to 

range between 2 and 4 ~g m with no evidence of a long-te~ trend for the 

period 1973 to 1984. 

Total ozone and S02 in the atmosphe~e were meas~ed for AES, Canada, 

during the year with a Brewer spectrophotometer. The CO analyzer of the Max 

Planck Institut, Mainz, Germany. was operated d~ing the year; however, there 

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

8 
The SIO Applied Physics inf~a~ed CO2 analyze~ ope~ated without majo~ 

p~oblems du~ing 1985 in pa~allel with the GMCC CO2 analyze~ . Flask samples of ai~ f~om MLO and Cape Kumukahi continued to be supplied to SIO on a weekly 

basis. 

Flask sample collections we~e made both at MLO and at the seacoast at Cape 

Kumukahi fo~ seve~al investigato~s . Flask collections we~e madr2at MLO fo~ 

the Aust~alian CSIRO who a~e analyzing the s amples fo~ the 1jC/ C ~atio as 

well as fo~ CO , CO2 , and CH4. Othe~ flask sample p~og~ams i nclude those of 

the OOC , NCAR, and SIO. Colo~ado College continued thei~ pe~iodic sampling at 

MLO fo~ nit~ic acid and hyd~ochlo~ic acid vapo~s ove~ 2-wk pe~iods eve~y 3 

months. 

Two new coope~ative sola~ ~adiation p~og~ams e~e begun , one by Colo~ado 

State Unive~sity and one by t he Unive~sity of A~izona . The CSU p~ogram 

installed a five-element, multi-field-of-view tracking sola~ photomete~ system 

designed to mo nit o~ the sola~ a~eole. The Unive~sity of A~izon a p~ogram , 

suppo~ted by a NOAA ARL grant , includes the installation of a multi-wavelength so la~ spect~o~adiomete~ and its long-term ope~ation at MLO. The overall goal 

of the p~ogram is to dete~mi ne the long-te~m va~iability of sola~ spect~al 

i~~adiance , i .e ., the sola~ constant. II Meas~ements ove~ a sola~ cycle a~e 

contemplated. 

REFERENCES 

Lockwood, J. P. , and R. Romano, 1985. In Sicily: Lava dive~sion p~oved in 1983 

tests at Etna . Geotimes 30(5) :10-12 . 

9 
2.2 BarTow 

FACILITIES 

Ukpiagvik Inupiat Corporation completed the takeover of NARL . Power and 

third-party support that had been previously supplied by NARL is now being 

supplied by the DEW line site. 

BRW can now orde r supplies through the GSA Alaska Customer Supply 

Center. 

The station staff at BRW began an extensive program to utilize the IBM PC 

to the fullest extent. The PC is now being used for most of the word 

processing duties. 

A water still was added t o the station inventory, giving the station a 

good supply of distilled water for the G.E . CNC and the MLO precipitation 

program. Water was formerly supplied by NARL. 

Because the cost of shipping tanks of gas by air increased this year, the 

barge was used to transport the tanks to BRW. This method worked without any 

major problems, so it will probably be continued in the future. 

During the winter the largest herd of Caribou ever, 250,000 and growing 

by 10% per year, moved into the North Slope . A small number were as close as 

50 ft to the station. 

Acoustic tile was installed at the Observatory bringing the sound level 

down from 85db . 

The interior of GMCC housing unit B-5 was painted and carpeted. 

Vehicles 

The 1982 Dodge truck, which has had a history of problems, threw a rod 

and had to have the engine replaced. The 1979 GMC had very few problems and 

is still the best vehicle. New tires were put on late in the year . The 

Sidewinder was excessed and is no more. Paperwork was also begun to excess 

the 1977 Chevy Suburban . 

Procedures have been initiated to purchase a new snow machine early in 

1986. 

PROGRAMS 

Programs carried out in BRW are listed in table 3. Comments on some of 

the programs follow. 

10 
Table 3. --Summary of sampling programs at BRW in 1985 

Program 

Surface ozone 

Methane 

CFC-l1 , CFC-12. and IbO 

Total ozone 

Aerosols 

Condensation Nuclei 

Optical properties 

Solar Radiation 

Albedo 

Global irradiance 

Direct irradiance 

Direct irradiance 

Terrestrial (IR) radial ion 

Turbidity 

Meteorology 

Air temperature 

Dewpoint temperature 

Pressure 

Wind (speed and direction) 

Precipitation Chemistry 

pH 

Conduct! vily 

Cooperative Programs 

Total surface particulates (DOE) 

Aecosol chemistry (URI) 

Ultraviolet radiation (Temple Vnlv.) 

Precipitation gauge (ASCS) 

Various trace gases (OGe) 

MagnetiC fields (USGS) ! lC (USGS) 

Various trace gases (NCAR) 

I l e/ 11C (eSIRO) 

CO~ I llC , NzO (SIO) 

Llr;; llc (Vniv . 'rJashington) 

Halocarbon monitoring (Vnlv. of 

Calif ., Irvine) 

Aerosol chemistry 

(Uni v . of Alaska) 

ULf waves (Univ . of Tokyo) 

Earthquake detection 

(Univ. of Alaska) 

Instrument 

URAS-2T infrared analyzer 

O.5-L glass flasks , pI 

O.5-L glass flasks, through .'1nalyzer 

3-L glass flasks 

Dasibi ozone meter 

0.5-L glass flasks 

Carle GC with fiP acquisition 

300-rnL stainless steel flasks 

Ozone balloons 

Dobson ozone spectrophotometer 

Pollak CNC 

C. E. CNC 

rour-wavelength nephelometer 

Eppley pyranomter 

Eppley pyranometers with Q and RCS 

filters 

Tracking NIP 

Eppley pyrheliorneter with Q , DCl , 

RC2, and Rca filters 

Eppley pyrgeometer 

Sun photometers with 380- , 500- , 118-, 

and 862- nm narrowband filters 

Thermistor 

t-lax .-min . thpnnometers 

Dewpoint hygcometer 

CapaCitance transducer 

t·1i crobarograph 

~lercuri al barcmeter 

Bendi x Aerovane 

pH meter (samples analyzed at t-1LO) 

Conducti vi ty bridge (samples analyzed 

at MLO) 

High-volume sampler 

Hi gh- vol ume sampler 

Ultraviolet radiometer 

"'yomi ng sl1i elded preci pi taU on gauge 

Stainless steel flasks 

Magnetometer 

lO-L stainless steel flasks 

3-L stainless steel flnsks 

5-L glass flasks 

5-L evacuated glass flasks 

35-L stainless steel flasks 

Various stainless steel flasks 

Hi - Vol filters 

Cassette recorder 

Seismograpll 

11 

Sampl ing 

frequency 

Continuous 1 pairwk- J 

1 pair wk - ! 

1 pair wk- J 

Continuous 

1 pair wk- L 

Continuous 

1 pair wk- J 

1 wk- J 

Discrete 

Discrete 

Continuous 

Continuous 

Continuous 

Continuous 

Continuous 

Discrete 

Continuous 

Discrete 

Continuous 

1 rlay- J 

Cont i nuous 

Continuous 

Continuous 

Discrete 

Continuous 

Discrete 

2mo- J 

Continuous 

( I filter wk- J) 

Continuous 

(2 filters wk- ~) 

Continuous 

2 mo- J 

1 set '..Jk- I (3 flasks 

set - I) 

station check wk- I) 

pair mo- J 

pairwk- I 

pair (2 '..Jk)-I 

pail' wk- I 

(2 wk )-! 

set (3 mo)-I 

Continuous 

3 filters '..Jk- 1 

Continuous 

1 tape wk- 1 

Continuous 

Check site wk-! 

Change tape mo-! 
Carbon Dioxide 

The only problem with the URAS/NDIR analyzer this year was a thermal cutout switch that burned open and had to be replaced. CO2 monitoring, including 

the flask samples , went smoothly all year. 

Surface Owne 

The Dasibi meter was sent to Boulder for repair early in the year. On 

the return trip it was apparently dropped during shipping and damaged; 

therefore, it was again returned to Boulder. It was back in operation in 

May. 

Total Ozone 

A Dobson instrument is being considered for reinstallation in the near 

future . 

Aerosols 

Aside from the usual maintenance, the G.E. CNC ran well all year. The 

Pollak counter (no. 16 ) malfunctioned late in the year and was replaced by no. 

21. This did not solve the problem. A series of small leaks and new zero 

filters that were defective from the factory were found to be the problems and 

corrected . 

Solar Radiation 

An albedo rack was installed to study the heat budget. The two hand-held 

sunphotometers were sent to MLO to be calibrated. A new solar tracker, with a 

built-in ephemeris, was installed and was found to be an excellent tracker . 

Meteorology 

The dewpoint hygrometer had problems most of the year even after being 

sent to the factory for repair work. The BRW staff repaired the unit and 

returned it to operation late in the year . 

Cooperative Programs 

In 1985 LBL shut down its filter sampling equipment. This consisted of a 

daily sampler , a weekly Hi-Vol sampler, and a weekly dichotomous sampler. All 

of the solar equipment including an albedo rack, from the University of Alaska 

was also returned this year. The University of Tokyo installed a set of three 

sensors to look at ULF waves. The data were logged on a Walkman-like cassette 

recorder. 

1 2 
2.3 Samoa 

FACILITIES 

A complete changeove~ of pe~sonnel occu~~ed in June and July at SMO with 

the appointment of a new technician and station chief. The depa~ting staff, 

Don Nelson and Roge~ Williams, had se~ved in Samoa fo~ 10 and 8 yea~s 

~es pecti vely . 

The obse~vato~y building was upg~aded and ~eo~ganized in August. The 

~oof-top g~ating table was painted in August , and the ~oof was ~esu~faced with 

an epoxy paint in Octobe~ . That same month the shingles we~e stained and the 

wate~ catchment was d~ained and cleaned. GMCC inst~uments in the building we~e put on a UPS in 1985. 

In Ap~il, th~ee sections we~e added to the Matatula Point towe~, b~inging 

its total height to 15 m. The GMCC CO2 sampling line and the SEASPAN ae~osol 

sample~ we~e ~elocated to this new height. 

The photovoltaic system ope~ated well all yea~. A ~eplacement CAMS box 

configu~ed to cont~ol the system was tested f~om Ap~il to June but p~oved 

unsatisfacto~y. Fo~ the ~emainde~ of the yea~ the system was ope~ated unde~ 

cont~ol of the o~iginal ~acto~y-installe d ci~cuits. The Samoa photovoltaic 

system p~ovides uninte~~upted, "clean" powe~ to all t&ee CAMS boxes , the CO2 analyze~ system , all meteo~ology inst~uments, and all sola~ ~adiation 

i ns t~uments. 

On 31 M~ch, a fi~e dest~oyed NOAA housing unit #T-6 in Tafuna, the 

station chief's qua~te~s . Appliances, f~nit~e, pe~sonal belongings , and 

most of the wooden st~uct~e of the house we~e substantially lost. The cause 

of the blaze is believed to be an elect~ical sho~t that occ~~ed somewhe~e in 

the vicinity of the maste~ bed~oom ceiling . 

The station chief's qua~te~s we~e ~elocated to unit #T-7, a vacant NOAA 

house next doo~ . The new unit ~equi~ed a conside~able amount of ~enovation 

including the installation of new sc~eening, floo~ing, appliances, and sinks, 

along with a complete inte~io~ and exte~io~ paint job and mino~ ~epai~ wo~k. 

The ot he~ NOAA/GMCC housing unit also unde~went imp~ovements with the addition 

of new appliances, a new counte~ top and faucets, and the ~emodeling of the 

bat&oom. 

In Ma~ch, the badly ~usting Datsun pickup was ~eplaced by a new Toyota fou~-wheel-d~ive pickup. 

PROGRAMS 

P~o~ams ca~~ied out in SMO a~e listed in table 4. Comments on some of 

the p~og~ams follow. 

Ca~bon Dioxide 

A URAS-2 inf~a~ed analyze~ continuously monito~ed the concent~ation of 

CO2 du~ing 1985 with no app~eciable downtime. T&oughout the yea~, 5-L and 

3-10 flask pai~s we~e exposed weekly. 

1 3 
Table 4.--Summar y of sampling programs at SMO in 1985 

Program 

Gases 

----c52 

Surface ozone Total ozone Methane 

CFe-tl , CFC-12 , and N20 

Aerosols 

Condensation nuclei 

Optlcal, properties 

Solar Radiation 

Global lrradiance 

Direct irradiance 

Direct irradiance 

Turbidity 

Meteorology 

Air Temperature 

Oewpoint temperature 

Relative humidity 

Pressure 

Wind (speed and direction) 

Precipitation 

Preclpitatl on Chemistry 

pH 

Conducti vi ty 

Cooperative Progra~ 

CO2, lle . N20 (SIO) 

ALE project : CFC-l1, CFC-12 , 

"20' CH,CCl, . CC14 (OGe) 

ALE project, CH4' CO . CO2 (OGe) 

Various trace gases (OOC) 

13c. 18o. CO2 (CSIRO) 

13C (USCS) 

Wet-dry deposi ticn OIADP) 

Bulk deposition (EML) 

Hi-Vol sampler (EHL) 

Hi-Vol sampler (SEASPAN Project) 

Instrument 

URAS-2T infrared ana3yzer O.5-L glass flasks P 

O. 5-L glass flasks . through analyzer 

5-L evacuated glass fl asks 

Dasibi ozone meter 

Dobson spectrophotometer no . ~2 

0. 5-L glass flasks 

300-mL stainless steel flasks 

Pollak CNC 

G. E. CNC 

F'our-wave length nephe lcmetel' 

Eppley pyranometers with Q and ReB 

fi lters 

Eppley pyranometers with Q 

fllters on tilted mounts 

Eppley pyrhel10meter with Q filter 

Eppley pyrheliometer with Q , OG1 , RG2 , and ReB filters 

SlUlphotcmeters wi th 380- , 500- , 178- , and 862-nm narrowband filters 

Thermi stor 

Max.-min . thermometers 

Hygrothermograph 

Thermistor 

Dewpoint hygrometer 

Hygrothermograph 

Sli ng psychrornetec 

capacitance transducer 

Mi crobarograph 

Mercurial barometer 

Bendi x Ael'ovane Polyeth ylene funnel, bottle 

Corning model 125 meter with semlmicro combi nation electrode 

Beckman mode I RC-16C meter 

5-L evacuated glass flasks 

HP58ljOA gas chrcmatograph 

Carle gas chromatograph 

Stainless steel flasks 

5-L glass flasks 

10-L stainless steel flasks 

HASL wet-dry collector (ne·,., 

Chemetrics , Dec 81) 

Plastic bucket 

Hi-Vol pump and filter 

Hi-Vol pLlllp and filter with clean 

14 

Sampling 

F'cequency 

Conti nuous 1 pall' wk- 1 

1 pair wk- 1 

1 pair wk- 1 

Continuous 

3 day-I 

1 pair wk -1 

1 pair wk- 1 

Discrete 

Continuous 

Continuous 

Continuous 

Continuous 

Conti nuous Discrete 

Discrete 

Contl~vous 

1 day 

Contl~~ous 

, day 

Conti nuous Cont!nuous 

Discrete 

Continuous 

Continuous 

Discrete 

Conti~vous 

1 day 

day-I «('MCC) ; 

1 wk- 1 (NADP) 

day-I (G>'CC) ; 

1 wk- 1 (UADP) 

1 p~V wk- 1 

I h 

3 h- I 

1 set wk- 1 

(3 flasks set -1) 

1 set mo- 1 

2 pa!, mo- 1 

1 wk , wet; 2 ~fl. dry 

mo 

wk -' 

wk- 1 
Surface Ozone 

Surface ozone was measured continuously by a Dasibi UV ozone monitor and 

recorded on a strip chart. Beginning in June , long periods of digital data 

loss occurred when the CAMS box failed to read the digital data stream from 

the Dasibi. In an attempt to "unsti ck" the system , boards were replaced, 

connectors remade, and various keyboard inputs tried . The problem was 

eventually resolved by tying together the ground from the main observatory 

building with the ground from the aerosol-sampling building . 

Total Ozone 

Dobson ozone spectrophotometer no. ~2 provided discrete total atmospheric 

column ozone measurements throughout the year. 

Surface Aerosols 

Condensation nuclei were measured by a G.E. CNC continuously in 1985 

except for a period from June through August when the instrument was in 

Boulder for repairs . The four-wavelength nephelometer ran without 

interruption. An attempt to operate a Knollenberg Counter was thwarted 

because of tape drive problems. 

Solar Radiation 

The complement of solar radiation instruments of SMO remained 

unchanged. In March, a preamp was added to the CAMS input to boost the 

millivolt signal levels and improve the signal-to-noise ratio. 

Meteorology 

Meteorological instrumentation remained the same as in 1984. In 

September a dewpoint hygrometer was calibrated and put on line. 

Precipitation Chemistry 

Both GMCC and NADP precipitation chemistry programs continued at SMO, 

providing on-site measurements of pH and conductivity in rainwater. NADP 

samples were collected weekly and GMCC samples were collected daily when 

preCipitation was present. The observatory receives an annual average of 100 

inches of precipitation. 

Cooperative Programs 

OGe continued to monitor trace gases in 1985. At the start of the year a 

Carle and an HP58~0 gas chromatograph were in operation. In July, OGe 

installed an HP5880 chromatograph and a UPS. After some months of side-byside comparison, the Carle was removed during a subsequent visit by OGe staff 

in November. 

15 
2 . lJ South Pole 

FACILITIES 

The National Science Foundation ' s CAF experienced few problems functionally or structurally during the 1984-1985 season . There were some modifications made to the floor plans of the CAF ; fig. 1 illustrates the latest 

layout. Improvements or changes made inside the CAF areas follow : (1) GMCC 's 

CAMS units were installed . (2) The ICDAS clock was wired to print each hour 

on the aerosol and the solar radiation chart recorders. (3) Antistatic 

matting was installed in the NOAA room. (lJ) A new flask sampling table was 

built and all flask pumps were mounted to it for air sampling through the new 

sampling pipe discussed below. (5) A new storage shelf was built above the 

CO2 tanks in the NOAA room . (6) A new work table with a plexiglass top was 

built for the Pollak area . (7) An ink drawing of the CAF 's floor and roof 

plan was produced on Mylar . (8 ) A new work table for the 02N2 pump and flasks 

was built . (9) All excess wires in the overhead racks were cleaned out . (10) 

New stainless steel shelves were installed in the Co-op room . (1 1) A new 

plexiglass Dobson hatch was built and installed. (12) The instrument racks ' 

front panels were painted. (13) All pump controls in the Co-op room were 

rewired. (1lJ) All sampling stacks were heat traced and insulated. (15) The 

solar radiation heater/aspirator box was rebuilt and replumbed , and thermostatically controlled heat was added. (16 ) Fluorescent lighting was installed 

near the mercurial barometer . (17) The CAF's thermostats were relocat ed. 

(18) The pump cabinet in the Co-op room was reorganized and rewired--it is now 

used for only sampling pumps and not miscellaneous storage as before. 

---Grid North 

Cosmic 

NOAA CSIRo~Samphng Stacks Shelves Dust 

G~ I Gas L Aerosol 1 uS~~~~~OE 

H,'.m'" J:'b b- .;, ~ pr;l I 0 6l; 6 6 6""'"'"-7"'== 

Pollak ~.J High Volume 

lIephe lometer Sutl~ce Sampling Pumps 

r;. 

dt=J' ~ GECNC Ozon e 

CO 2 TankS ""! ~ O,H, 0 

g Mercur al ........-c:;r;=:!::!;=E:~;=:!::;r=!::=::J g Baromete r Cryoc!lol_ 

Hood 

Clean 

~ Microbarograph 

lj-CO 2 Hum d~ Folding 

Mel. door 

Common 

Storage 

& 

NOAA/GMtC Olliee AnaL 

File Ouk 

Storage 

Sionge 

Deck ......... -. 

StQrage 

Keeling Fluk 

C14 Spller! 

Storage 

TECH 

Shop 

Repair 

Bentl! 

Table 

& 

Parts 

Drawers 

NSF 

Desk 

Figure 1. --Clean Air Facility SPO, 1985 

16 

D 

Dobson Parts 

- CSIRO 

C14 

C!!:3 

Dobson Ronm 

NOAA / GMCC ---------

0 

0 

O_~ CO2 Solar 0 Stonge Radiation 0 

Room 0 

FW NIP 

= Table 
The following synopsis describes those events affecting data acquisition . On 12 March 1985 , the trace gas sampling stack was pressurized with CO2 from the aerosol unit after both ends were sealed . Three pinpoint leaks, each 

located at the base of a sampling stem , were immediately apparent. An attempt 

was made to weld , solder , and braze these leaks closed , but the efforts were 

fru i tless. The CO2 intake line was moved to the aerosol stack , surface 

ozone 's line was moved to its own sampling line outside , and halocarbon 's and 

NCAR 's intake remained on the trace gas sampling stack until the sampling 

pipe , mentioned below , was installed . 

On 21 March 1985 , a new sampling pipe was installed in the northeast 

corner of the CAF . Within the pipe ar e t wo 1/4-in copper tubes , one 1/4-in 

stainless steel tube , one 1/4-in Teflon tube , and one 3/8-in Teflon tube . The 

pipe stands approximately 15 ft above the CAF 's roof and is heat traced with 

4-W heat tape . Surface ozone , halocarbons , NCAR , 02N2 , and a separate flask 

sampling line now utilize this pipe. 

On 2 April 1985 , the CAF had a power loss due to a break in one of three 

power phases somewhere between the CAF and the power plant. The location of 

this break was unknown until 29 August 1985 . It is believed that th is break 

resulted from ice sh ifting . Power was restored by means of an open- delta 

connection between the CAF and the power plant transformers on 4 April 1985 . 

On 24 May 1985 , a D- 6 Caterpillar cut through a powercable to the CAF 

while removing snow from the station 's front entrance. The cable was spliced 

back together and power was restored 1 1/2 hours later. On 29 August 1985 , two power phases to the CJ\F were cut by a D-6 Caterpillar while it was 

removing snow from the station ' s front entrance. By coincidence, the lost 

power phase of 2 April 1985 was found within 20 ft of the newly broken 

cables. All three were spliced to their appropriate halves giving the CAF 

three-phase power 5 1/2 hours later . 

GMCC 's CAMS units were installed to replace ICDAS , to control and monitor 

aerosols , car bon dioxide , meteorology , solar radiation , and surface ozone . 

Three CAMS units were installed during the 1984-1985 season . The ASR (aerosol 

and solar rad i ation) CAMS was initiated on 27 November 1984 at 0539 GMT , the 

CO2 (carbon dioxide) CAMS on 14 November 1984 at 0022 GMT , and the M03 

(meteor ology and surface ozone) CAMS on 19 November 1984 at 2310 GMT. All 

CAMS data are stored via cassette tape drives onto Digital DECTAPE II 

cassettes. 

Heavy demands on the station ' s power plant resulted in 13 blackouts , 11 

brownouts, and 3 power surges. Although no instrument damage resulted , all 

blackouts resulted in an "AUTORESTART" on each CAMS unit. Four "BRAM LOST" 

messages were recorded for the year , all of which resulted from power blackouts. 

PROGRAMS 

Table 5 lists the sampling programs carried out during the 1984-1985 

seasons. 

17 
Table 5.--Summary of sampling programs at SPO in 1985 

Program 

Surface ozone Total ozone CFC-l', CFC-12 , and N20 

02N2 (NOAA/ARL) 

Ae('osols 

Condensation nuclei 

OpU cal properti es 

Solar Radiation 

Global spectral irradiance 

TUr'bidi ty 

Albedo 

Tercestcial (IR) radiation 

Meteorology 

Air Temperature 

Snow temperature 

Pressure 

Wind speedldirection 

Cooperati ve Pcogcams 

CO2 • 13C • N20 (SlO) 

Total surface particulates 

( DOE) 

Aerosol physical properites 

(SUllYA) 

Carbon aerosol (LBL) 

Various trace gases (aOC) 

1 3C(1 2c , CH~ (USGS) 

14C (NOAA/ARL) 

Snow acidity (NOAA/ARL) 

CH~ . CO OleAR) 

1 lIC/ 12C NaOH samples 

(USGS) 

Atmospher'i c Tracer Exp . 

(Los Ala~os Nat . Lab.) 

Cosmic Dust Collection 

(Univ . of Pittsb"rghl 

Interhemispheric 1jCl1 C 

(CSIRO) 

InstrLment 

URAS-2T infrared analyze!' 

O.5-L glass flasks p3 

O.5-L glass flasks, through analyzer 

Dasib1 ozone meter 

Dobson spectrophotometer no . 80 

300-mL stainless steel flasks 

Gas chranatograph 

Flasks 

Pollak Clle 

G. E. eNC 

Four-wavelength nephelaneter 

Eppley pyranometers with Q and 

RGB filters 

Eppley pyrhel iometer wi th Q , OC1 , RG2 , 

and RG8 filters 

Sunphotometers with 380- , 500- , 178- , and 862-nm narrowband filters 

Eppley pyranometers wi th Q and ReB 

filters , downward-facing 

Eppley pyrgeometer~ I up ..... acd- and 

da~nward-facing 

Platinum resistor 

Platinum resistor 0.5 cm 

Capacitance transducer 

t-lercur"i al baraneter 

Bend i x Aerovane recorder 

5-L evacuated glass flasks 

High-volu~e sampler 

Pollak CNC with diffusion battery 

Nuclepore filters 

High-volume sampler 

Stainless steel flasks 

lO-L stainless steel cylinder 

3,000 psi spheres 

125-mL Nalgene flasks 

Baseline gas chromatograph 

Aluminum flasks 

Gas bubbler 

CHII detector 

Cosmic dust collector 

flasks 

------------------_._-_ ..... 

18 

Sampling 

fr'equency 

Continuous 

1 pair (2_~k)-1 

1 pall' wk 

Conti~vous 

3 day 

1 pair wk- 1 

1 pair wk- 1 summer· 1 pair 

rna-I, wintlr 

1 pair week2 analySeS_~k-l 

flask rna 

present 

Discrete 

Continuous 

Continuous 

Continuous 

Discrete 

Discr'ete, stmner 

Continuous 

Continuous 

Cont inuous 

Continuous 

Conti nuous -1 

2 times day 

Continuous 

2 mo- 1 (3 flasks 

sample- 1 

Continuous 

(I filter wk- 1) 

01 screte 

Discrete 

Continuo~~ 

Twice rna 

(3 fla~ks 

set- ) 

1 mo- 1 

(2 cyli?derS 

sample- ) 

500 psi day-1 

Weekly 

Daily 

Weekly 

20 days mo- 1 

3-60 day 

periods 

Continuous 

2 flasks mo- 1 
Su~face Ae~osols 

The Pollak CNC ope~ated well all yea~. Both G.E. CNCs , nos. 7007 and 

3264296 , functioned well all yea~ with ve~y few complications. No. 7007 

expe~ienced two bad chips on the elect~onics boa~d, t~ee malfunctioned 

the~misto~s, and one system boil out. The the~isto~ p~oblem was ~esolved by 

a new elect~onic wate~ level sensing ci~cuit. No. 3264296 ~equi~ed nume~ous 

high-voltage adjustments f~om 5-8 Octobe~ 1985. This CNC was totally ~ebuilt. 

No majo~ p~oblems we~e expe~ienced with the nephelomete~. CO2 and ~elative calib~atio ns, powe~ blackouts, and powe~ b~ownouts caused data on all 

fou~ channels to be lost occasionally. These data we~e quickly ~esto~ed by e~asing the memo~y and then simultaneously using "hold ambient" and "mode A" fo~ each filte~ . This p~ocedu~e ~esulted in minimal data loss . 

Carbon Dioxide 

On 15 Decembe~ 1984, befo~e ~ealigning the URAS-2T, the optical qua~tz 

glass tube c~acked while using Dust Off to ~emove pa~ticles f~om its 

s~face . GMCC in Boulde~ was notified. A ~eplacement tube was sent, and it 

was in place by 12 Janua~y 1985. The t~ee pinpoint leaks found in the t~ace 

gas sampling stack on 12 Ma~ch 1985 ~esulted in the CO2 intake line being 

moved to the ae~osol stack fo~ the ~emainde~ of the yea~. Othe~ p~oblems 

included one ~aulty ~egulato~, c~acked Dyna pump diaph~ams, and two bu~ned-out 

fuses . The P sample~ functioned well t~oU~hout the yea~ . Afte~ the 21 Ma~ch 1985 sampling pipe inst~llation, all P flasks we~e exposed via the 

pipe's 3/8-in Teflon tUbe. P flasks p~io~ to this date we~e exposed on the ~oof. 

The 02N2 high-p~ess~e flask sample~ expe~ienced a leak in the 

comp~esso~'s stage no. 1. New comp~esso~ ~ings we~e sent on the midwinte~ 

ai~d~op, though once installed the pump could only attain 30 psi and 60 ~pm. 

This p~oblem was alleviated by using a 10-in pulley and a 2-hp moto~ to 

achieve 750 ~pm. This allowed us to take the ~equi~ed 1750-psi flask 

samples. 

aloca~bo s 

Hal oca~bon sampling p~oceeded with no p~oblems. 

Meteo~ology 

The~e we~e no p~oblems with this p~og~am except that the Bendix F~iez's 

wind di~ection accu~a cy was constantly off by seve~al degrees and the 

switching mechanism would not function p~ope~ly when the wind di~ection pen ~eac ed the 0° o~ 180° ma~k. These p~oblems we~e co~~ected on 25 June 1985 afte~ the anticipated ~eplacement ~eco~de~ did not a~~ive on the midwinte~ 

ai~d~op. New points we~e fab~icated from relay contacts and the pen adjusted 

to t r ack acc~ately with CAMS. The Bendix Friez t~acked with 1° from then on. 

19 
Ozone 

Surface ozone and Dobson measurements continued with no difficulties . 

Solar Radiation 

There were no major problems with this program . Solar irradiance was 

measured from 21 September 1984 to 22 March 1985. After the austral winter , these instruments were reinitiated on 25 September 1985 and have worked 

well. A new solar radiation preamp for CAMS was installed on 2 February 

1985 . Aside from general maintenance, it has functioned well throughout the 

year. 

COOPERATIVE PROGRAMS 

All programs operated without incident with the following exceptions: 

The U.S. DCE's high-volume sampler's main motor and backup shorted out during 

November 1984. DOE was notified, but replacement motors did not arrive until 

the midwinter airdrop. This project ran well once reinitiated. After the 

power outage of 2 April 1985, the three-phase carbon-14 motor could no longer 

be used because of CAF's new two-phase power. On 21 April 1985, the first 

sample using a new two-phase pump built by the GMCC electronic technician, was 

taken . All samples before and after this down period went smoothly. 

Many el ectroniC and mechanical problems were experienced with NCAR 's GC 

this year. An average of 6 to 8 of the required 12 runs per month were made 

between GC repairs. Early in the year the GC 's hydrogen generator developed a 

hole in its ECC assembly . NCAR was informed of this, though no replacement 

came on the midwinter airdrop. This project was retrograded to NCAR in 

November 1985 at their request. 

20 
3. AEROSOLS AND RADIATI ON MONITORING GROUP 

3.1 Continuing Programs 

SURFACE AEROSOLS 

The GMCC baseline aerosol monitoring program continued operations during 

1985 as in previous years. Condensation nucleus (CN) concentration and 

aerosol scattering extinction coefficient (Osg) were measured continuously at 

BRW, MLO, SMO , and SPO. A G.E. automatic CN ounter (CNC) operates 

continuously and a Pollak CNC provides daily calibration points at each 

station . A four-wavelength nephelometer at each station continuously measures 

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

A renovated four-wavelength nephelometer was installed at MLO during the 

last week of May. The renovation involved use of the original optics with 

upgraded electronics so that the MLO instrument is now identical t o the 

instruments at BRW , SMO , and SPO. The design of the original MLO nephelometer 

was described by Miller (1975), and the new design was described by Hanson 

(1977) and Bodhaine (1979) . Although the optics are identical in beth 

designs, the electronics in the old design performed an internal geometric 

mean , whereas the new design performs an arithmetic mean. This implies that 

during hours of significant signal variation , the new instrument may give 

slightly higher data values than those given by the old design . It is not 

possible to deduce one from the other without knowing the statistical 

distribution of the data during the hour . 

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

GMCC stations for 1985. Angstrom exponents calculated from the fourwavelength light scatteri ng data are shown in the upper portions of each 

graph. Monthly geometric means for each station are shown in fig . 2 for the 

entire data record and are listed in table 1 for 1985. 

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

the springtime, typical of the well-known Argtic haze. The regular annual 

cycle is appare~5 i~1the BRW long-term record shown in ~5g '- f in which monthly 

means exceed 10 m in the spring and can be below 10 m in the summer. 

The BRW CN long-term record shows a more variable semiannual cycle in which 

maxima usually occur in March and August, and minima usually occur in June and 

November. 

The MLO CN data shown in fig. 1 are typical for the downslope conditions 

at Mauna Loa and are most likely representative of the background troposphere 

for this region of the atmosphere. The as record for MLO shown in fig. 1 was 

produced by the new MLO nephelometer and sRows an annual trend similar to that 

of previous years. The long-term record of asp in fig. 2 shows a repeatable 

annual cycle with a maximum in April-May that 1s caused by 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 . The SMO aerosol is representative of a 

background marine air mass. Bodhaine and DeLuisi (1985) presented a detailed 

analysis of the entire SMO data record. 

21 
JAN fEB w.R APR MAY JUN rut AUG SEP OCT NOY DEI: 

1965 

AERCSOL DATA fOR SAld"OA 

JAN FEB YAH APR W.AY .ruN JUt AUG SEP ocr NOY DOC 

i~ I CtmllJ~ I I:d tir! ;~< ,J, 

, ~ 

7 .:--

, S1 

,I I 1 E 

~ ~.r.. ,A~ 1"1 II t- ' .1.. ... , M, iJ, J ::'y 'f I i 'vi • r y~ 

oS oS 

Y Y . . ". 

, .-, 

1" rJ ~ ~ J\\., ~J' ~" ~ t!'A Jvi "1 

~. Ji I .s - - JAN FEB WAR APR )dAY JtJN JUL AUG SEP ocr NOY DEI: 

1005 

JAN FEB:wAR APR llAY ruN JUL AUG SEP OCT NOY DEC 

1965 

AEROSOL DATA FOR 00fJI\{ POLE 

i~ I'AN IWff i

Y

If;lli:fi4¥M1 ~ i 

+ + 

I, .:-- -; . • , 

S' J>A 

, ~, ~ I1'JII ,v. Y E 

~ I;~" ~ ,~ I~~ · ~:;I '~\; .\ ,::} J ". ~ •.... ~ ..... ... ~ 'i.3' ~, \J '1- '~i\ . \ : \ , , oS ~-

Y . , 

" " 

". ru I\... :A , .-, 

].N ~ ' I "oj fJf \'-" .. "V "1 

o_ f'-" 0 - ~ 

~ l' oS oS 

0 0 

JAN FEB YAR APR WAY JUN JUL AUG SEP ocr NOY DEl:' 

1965 

Figu~e 1.--Daily geomet~ic means of asp and CN data at BRW, MLO, SMO, and SPO 

fo~ 1985. Fo~ each station, CN concent~ation (lowe~) is shown as a solid 

line. as data (middle ) a~e shown fo~ 450 (dotted), 550 (solid) , 700 

(dashed),Pand 850 nm (long-dashed) . Angst~om exponents we~e calculated f~om 

450- and 550-nm (dotted) , 550- and 700-nm (solid) , and 700- and 850-nm 

(dashed) asp data. 

22 
Table 1 .--Monthly geometric means of CN concentration (cm- 3) and asP. (m-l ) at 

450, 550, 700, and 850 nm, for BRW , MLO , SMO , and SPO during 1985 

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

BRW 

eN 144 668 491 309 231 165 314 322 238 141 184 113 

·sp(450) 1.44-5 1.35-5 1.65-5 1.98-5 5.44-6 1.59-6 1.68-6 2.10-6 3.11 - 6 5.41-61.11-6 1. 21-5 

·sp(550) 1.35-5 1. 25-5 1.53-5 1.12-5 4.39-6 1.24-6 1.33-6 2.44-6 2.88-6 4.10-66 . 21-6 1. 11-5 

·spOOO) 9.66-68 .80-6 1.09-5 1.09-5 2.65-6 1.26 -1 8.80-1 1.19-6 2.20-6 3.29-6 4. 28 -6 1 . 83-6 

·sp(850) 1 . 34-6 6 . 68-6 8.26-6 1.61-6 1.16-6 4.93 -1 6.90-1 1.35-6 1. 16 - 6 2.46-6 3.11-6 5.80-6 

MLO 

eN 238 216 221 229 215 304 346 252 333 281 343 262 

·sp(450) - 3. 20-6 2. 14 - 6 2.05-6 1.36-6 1.08-6 1.25-6 9 .59-1 1.04-1 1.05-6 

·sp(550) - 2 . 58-6 1. 13-6 1.61-6 9. 90-1 1.85-1 9.29-1 6 . 86-1 5. 24-1 1.39-1 

·sp (100) 1. 94 -6 1.50- 6 1.39-61.31-15.58-16.68-15.14-1 3.49-1 5.61 - 1 

·sp(850) 1.45-6 1. 14-6 1.10-65 . 08-1 3.98-1 4.80-1 5.03-1 3. 35-1 5.88-1 

SMO 

eN 266 291 269 229 190 225 262 421 221 213 259 383 

·sp(450) 1.14-5 1. 51-5 1. 25-5 1. 12-5 9. 15-6 1.20-5 1.48-5 2. 20-5 2.15-5 1. 99-5 1.62-5 1.18-5 

·sp(550) 1. 65-5 1. 41 - 5 1. 16-5 1.08-5 9. 38-6 1.19-5 1. 46-5 2 . 23-5 2 .14-5 1.91-5 1.51-5 1.59-5 

·spOOO) 1. 11 - 5 1. 46 - 5 1.15-5 1.12-5 9.55-6 1.25-5 1. 55-5 2.40-5 2.28-5 1. 98-5 1.61 - 5 1.51-5 

·sp(850 ) 1.16-5 1.54-5 1.18-5 1.20-5 9.95-6 1.33-5 1.68-5 2.62-5 2.46- 5 2.09-5 1. 14-5 1.49-5 

SPO 

eN 56 86 104 23 19 13 11 16 28 60 106 65 

·sp(450) 3.90-1 3 68-1 3.81-1 2.9 1-1 3.40-1 3.88-1 5. 91-1 5.25-1 5.94-1 6.43-1 5.41-1 5.16 - 1 

·sp(550) 2.33- 1 2.45-1 2.53-1 2.01-1 2.50-1 3.13-1 4.46-1 4.26-1 4. 85-1 5.02-1 4.4 1- 1 3.49-1 

·sp(700) 1.31-7 1.31-7 1.43-71.11-7 1.53-7 1.80-7 2. 85-7 2.65- 7 3. 19-7 3.33-7 2.96- 7 1. 8 1-7 

.sp (850) 6. 06- 8 7 . 11-8 9.20-8 7. 12-8 9.12-8 1 . 13-1 1. 14-1 1.74-1 2.1 0-7 2.34 - 7 2 . 06-7 1.16-7 

A compact exponential for mat 1s used for asp such that 1.44-5 - 1.44 x 10-5 • 

_ The SPO CN data show a strong annual cycle : a maxi~~m greater than 100 

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

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

ar~ 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, case studies of the winter seasalt events, and a study of 

aerosol chemistry were presented by Bodhaine et al. (1986 , 1987) . 

The least-squares trend lines shown in fig. 2 are not statistically 

significant, and the results are given in table 2. Trend lines have been 

calculated for these data in previous years and presented in previous GMCC 

Summary Reports. In general, as the data records have increased in length, 

the trend lines have been getting flatter, confirming previous suggestions 

that there is no significant l ong-term trend in the background aerosol 

measured at these four stations. 

Nephelometer and CN data are available in NOAA data reports . Requests 

for specific data sets on electronic recording media should be made to GMCC 

personnel. 

23 
Mauna loa 

5 

~ A If, /' 

~ '\ (\\ .LV 1 

f1 , -'\ ~ 

~ II 

'\ 

:\ 

"\ 

'E 

-6 bS! 

75 76 77 78 79 80 81 82 83 84 85 

Yur 

3 

2 

• M-

" 75 

~ ,f., 

[YJ V' 

7. n 78 

-;; 

II\, /'-,. .f'l. 0- ""\ "'" -

79 80 8' 82 83 84 85 

Year 

South Pole -6 'i 

E 

- b' 

Samoa .J ~~~--~-4--~-4--~~--+--+--+--1 ~ ~ 

BRW 

MLO 

SMO 

SPO 

75 76 77 78 79 80 81 

Year 

Figu~e 2.--Monthly geomet~ic means of a p and CN data fo~ the enti~e data ~eco~d. Details of the t~end~ines a~e given in table 2. 

Table 2.--Least-squa~es t~end analysis of the common loga~i thms 

of the data shown in fig . 2 

85 

Pa~amete~ Slope Inte~cept S.E. T~end (% y~ -1 ) 

CN 0.0162 -29 . 8 0.284 3.8 

asp 0.00345 - 12 . 1 0.395 0.80 

CN 0.00713 -11 . 7 0.120 1.7 

asp 0. 0159 -35 . 7 0. 348 3.5 

CN -0.00357 9. 5 0.102 -0.82 

asp -0.0288 52.3 0.106 -6 . 4 

CN -0.00462 10.8 0. 414 -1.1 

asp 0.0242 -54 .6 0. 180 5. 7 

SOLAR AND THERMAL RADIATION 

This section cove~s the sola~ and the~mal ~adiation meas~ements at the fou~ GMCC baseline obse~vato~ies. Included a~e a summa~y of activities at the 

sites, a discussion of calib~ation inte~compa~isons between field and ~efe~ence inst~uments ove~ the past 10 yea~s, and pa~tial ~esults f~om va~ious 

monito~ing p~ojects. 

24 
Barrow 

A new automated solar tracker was installed in the fall of 1985. The 

tracker is the commercially available 20/20 Licor that continuously adjusts 

for solar declination as well as hour angle . The new tracker improves the 

tracking accuracy, especially during extended periods of cloudiness when the 

sun is only occasionally visible. 

The blowers, which were installed to prevent condensation buildup on the 

pyranometer domes, were removed from service when it was determined that their 

useful life had been exceeded. A new blower system was developed and placed 

into operation in early 1986 . The new blowers operate only on the quartz and 

RGB upward-facing pyranometers and not on the downward-facing pyranometers. 

The instruments not served by the blowers rarely experience frost deposition . 

An HP-71 calculator-based backup data acquisition system was tested 

throughout 1985. A few minor problems were encountered , the worst of which 

was the quality of the printing on the system ' s strip chart. 

Complete radiation balance measurements were begun in June with the 

installation of a downward-facing pyranometer and pyrgeometer. The inverted 

instruments are suspended 2 m above the tundra at a distance of 300 m due east 

of the main building. These instruments measure upwelling solar shortwave and 

terrestrial longwave radiation . The downwelling flux is measured by two 

identical instruments mounted on the roof of the building. The instruments ' 

signals are routed to the ASR CAMS in the main building. 

Mauna Loa 

The Leeds and Northrup radiation strip chart recorder was replaced by an 

HP-71-based backup data system in May 1985. 

The dependence upon the Mauna Loa facility and staff as a primary 

sunphotometer calibration facility increased during 1985. This is due t o both 

the realization of the extent of problems wi th Boulder-based calibrations and 

the expanded awareness of the availability of the site to other government and 

nongovernment laboratories. The impact on the MLO staff' s workload has been 

minimized by requiring the outsi de users to supply their own personnel to 

perform the required operations. 

The automated solar observatory dome continues to operate , providing a 

sheltered platform for instruments requiring highly accurate solar tracking 

during early morning hours . The automated observatory's current principal 

function is to faCilitate operation of the PMOD three-wavelength precision 

sunphotometer that serves as the primary calibration standard for the U.S. and GMCC sunphotometer networks. 

Samoa 

Radiometer degradation is extreme at SMa. The RGB domes show visible 

changes in color after less than a year in the field at SMO . Fortunately, 

these color changes do not significantly change the filter t ransmission 

characteristics. A more serious instrument deteriQration is seen in the loss 

25 
of sensitivity in the qua~tz py~anomete~s. Sensitivity losses as g~eat as 3% pe~ yea~ have been documented. Howeve~ , the calib~ation d~ifts we~e well 

enough documented so that the data could be co~~ected to the ±1.0% level ove~ 

the long te~. 

South Pole 

In Decembe~ 1985, an HP-71-based data system was installed at SPO. The 

majo~ p~oblem encounte~ed was the quality of the p~inte~ ope~ation. This p~oblem was solved in pa~t by inc~easing the humidity in the building. 

The p~esent mounting ~ack fo~ the inve~ted ~adiomete~s is slowly being 

bu~ied by snow. As of the end of 1985, the downwa~d-facing inst~uments , 

qua~tz and ReB py~anomete~s and a py~geomete~ , we~e suspended about 2.5 ft ove~ the snow s~face . 

Inte~compa~ison With T~aveling Refe~ence Inst~uments 

Each yea~ a ~efe~ence standa~d py~anomete~ and py~heliomete~ with a filte~ wheel a~e sent to each of the obse~vato~ies fo~ a pe~iod of compa~ison 

with the station inst~uments. The compa~isons a~e accomplished du~ing seve~al 

days of side-by-side meas~ements. Although the compa~isons can be examined fo~ hou~ly and daily pe~fo~mance, the final ~esult is the ove~all ave~age of 

the ~atio between the calib~ated output of each inst~ument. The calib~ations 

assigned to all the inst~uments fo~ the pu~pose of the inte~compa~ison have 

been held constant ove~ the last 10 yea~s so that the ~esults of the compa~ison will show any ~elative change in sensitivity between the ~efe~ence 

and station inst~ument . The ~efe~ence inst~uments a~e calib~ated in Boulde~ 

at the Sola~ Radiation Facility . 

In gene~al the py~heliomete~s stayed ~elatively steady whe~eas the 

py~anomete~s sta~ted out stable but have inc~easingly d~ifted in ~ecent 

yea~s . The d~ifts in the station py~anomete~s a~e less at the colde~, d~ie~ 

locations. 

The filte~ facto~s fo~ the station filte~ wheels used with the hand-held 

py~heliomete~s a~e also dete~mined each yea~. The p~oced~e involves measu~ing the t~ansmission of a ~efe~ence filte~ in the labo~ato~y and then 

using that filte~ in the field to ve~ify the t~ansmission of the station 

filte~ . 

Clea~-Sky No~mal Incident I~~adiance 

Measu~ements of the di~ect no~mal sola~ i~~adiance in fo~ spect~al bands 

have been made at the fou~ GMCC obse~vato~ies since 1977. The meas~ements 

a~e only ~eco~ded when an obse~ve~ ve~ifies that visible clouds a~e not 

influencing the meas~ement. Obse~vations a~e taken nominally t~ee times a 

day, nea~ local noon and 2 hou~s befo~e and afte~ . Results f~om these meas~ements fo~ 1977 t~ough 1981 we~e p~esented by Bodhaine and Ha~~is 

(1982). The p~eviously ~epo~ted ~esults a~e up to 6% in e~~o~ because an inco~~ect sun!ea~th distance co~~ection fo~ was applied. A ~eanalysis of the 

data fo~ that time and subsequent yea~s is given in tabula~ fo~ in fig . 3. 

Also, co~~ected data fo~ 1977 t~ough 1981 a~e p~esented he~e in fig . 4, which ~eplaces fig . 23 in Summa~y Repo~t No. 10 (Bodhaine and H~~is, 1982). These 

26 
"" ,..,,, '917-1986 AV(UG( OVER AlA ""'55 ,NT(RVAl "" ""''' 1911-'986 AVov.cC OVER AlII W.SS INT(RY.o.l 

""" ~ OUAATZ SO "" SO "" SO '" SO " "'" ~ OUAATZ SO "" SO '" '" '" SO 

l,n_ 19I1! '.' 91 .19 2.119 n. ' 11 2.J~ ~ • . ~J I .g ~ ':LJ' I. 7J 1~2. '971_19111 U 112 .Jl 2.39 112 .3" 2. It 68 . • ~ 1. ,. SIl , S" I,ll n • . 

1911- 19111 ,. , 11 , " J . H n,98 l . 81 ' 11 .18 1 . <7 J9,U 1.25 ". \9n-19&1 '-' ".51 • . 35 78 . 116 J.52 n,83 J .1l S6 . 11 J.n ". 1982 ... 98.65 J , n 59. IS 1.19 ., • • .)7 1 , 98 <S.la , , oJ 'J. 1982 U 96.U 2.15 77. oJ I.H 5S.J' I . • , SII . 2' ' . 36 ". 1982 '-' 7S . n .l . 6' "9,n 1.71 <1 . ' 6 2.16 J9. ' S \.77 ". 19ft) '-' U.S5 ' ,7 5 7$. '7 l.82 6l.17 3 . 52 $ ... 91 ' . 'S ' J . 

1981 '.' IIII.S6 _ ,II n.Ol 2.91 S2 . 6.) 2 . " 'J.91 2. 17 ". nIl J.' U.t.l .. . !l1I 10 .0 _ J. ,l9 63.2.9 2.!Iit 56. oJ 2 . <1. " . 19111 , .. n . u 2. 16 56.9' 1." '5. 1& 1 .8& n .S5 I.1.l ". 191I ' U , •. J5 .n ''',68 .J' 63 .9' .. , "'.5" .J> , '9114 .. . n .8l. 1. 2' 68.6' 1.71 Sl .IIS I. U H,e ' Ll' ". 198' J.' 81i .... 8 .211 7',H 6 .62 sa. 98 ::' .!>3 "'.7' 6 . H " . 195' , .. 7~. I I 2 . ~6 ~5 M 1 . 2' '6 . 6 1 1.'1 U . S7 l.ll J. 195~ '-' 97 . " I . H 77 . HI 1. 7~ 6<.71 1.75 ~1. HI 1 . 51 , . 

195 ~ .. , 91.1J 2 . 55 '9.H 2 . 6J ~I. 25 2 . 21 ~. 27 1.91 ". I'lIU '-' n.n I . I~ 7). 00 J.U U . SJ l. 15 ~6.25 2 . 95 ,. 

~ ""''' 19 77- 19~6 AV(IIIoG( OV(ll AlII w.ss INT[RVAl "" fWIP 1971·1936 AV(U,C;E OV[l All MASS IIIHRYAl 

"'" ~ OUARfZ s.o "" SO '" SO '" so "" M CUUfZ stI "" " "2 '" ". ., 1171_1151 '. , 91 . 11J ' .11 1l.Bl J. O~ 55 . " 1. ~O 5 1 . 01 2.26 ". 19n· 195\ .. , II~." 2." 8S.4J ~.87 68.96 2.06 "'." 2.11 a16. 19"-1951 '-' 77 7 5.59 55 .50 J " 55 . J2 J .12 · Q.56 l . IIJ -.. 19n- 19&1 ,. , 10S.29 2.S2 &l .n 2.'~ 67.92 2.la "'." 2.17 lb. 19" U ,-

" 1. 2' 57 9~ 1.61 5' . " 1.5::- " . 01 L~J ". "" L1 96.02 1.92 7l." 6.12 60.17 5.02 5J.'! ,.U 10J. 1952 U 71 . 95 I . D 61 U 1.51 52.75 1. ,. " " ." ,. 1982 1. , a9.24 12.26 71.10 9.56 58.14 7." 51.74 '.OJ .. 195J U 77. I~ 1.15 62. .. LOJ 58.1:) 1. 1 1 I • . 98 '~5 ". \9&1 ,., ~.47 1.94 &3.46 ,,7] 61. is '-.. 60.14 1.5a lB. 198J 2.' 51'1 . M 5.68 50 .10 • . 01 ' 1 . 88 J 09 Je . aJ 1 . U ,. 19a1 2. , 97." 1.7l n.ao 2 .~4 63.89 2.16 S6.M 2.15 198 ' U a6. 0l1.. 6.5 ' 68.91 5 .85 5 1 .11 J.ae 19. 15 7 . 71 n. ". '''' '-, III.M l.lO M.22 2." 70.0S I. U I 61.99 , ." 210 . 198' U 71 85 11.6' U.19 , " 50.5J I . ' 6 15.n J.JJ .. "" 2. , 101.n l.'" aL04 1.27 ".19 }. " 60 .97 3.25 <. 1155 '. , 89 .11 • . JI 11. } ' , " " " 1.99 5e. I, 1.55 ,. 19as '-, 111.16 2.61 as.14 2." 69.6& 2.16 61.61 2.J6 1955 U 5J OJ 9 . e. 15 . 21 1.77 lS . 2J Ii. J~ }' . 58 Ii . U -. ". 

Figu~e 3.--Mean di~ect beam sola~ flux (mW cm-2) and standa~d deviation 

(SO) fo~ the 5-y~ pe~iod of 1977-1981 and each individual subsequent yea~, 

Values a~e fo~ two selected ~elative ai~ mass values (AM). N is the numbe~ 

of obse~vations . The spect~al inte~vals ua~tz, OG1, RG2, and RG8 a~e the 

same as desc~ibed in fig. 4. 

measurements establish an absolute level fo~ confirmed clea~-sky backg~ound 

sola~ measurements. The va~iability in the data indicates the degree of 

va~iability of ~adiation attenuato~s such as wate~ vapo~, ozone , and 

ae~osols. The distinctly diffe~ent ~esults betVleen the fou~ sites a~e due to 

altitude and latitude diffe~ences, which cause diffe~ent amounts of Rayleigh scatte~ing and wate~ vapo~ abso~ption. Two global ext~emes a~e ~ep~esented by 

South Pole , at 2. 8 km and ve~y d~y, and Samoa , at sea level in the t~opics . 

BRW Radiation Budget 

Figu~e 5 shows p~elimina~y ~esults of the ~adiation budget measurements 

at BRW . The three graphs show daily totals of the net longwave, net sho~twave, and the net all-wave ~adiation flux, whe~e downwa~d flux is 

positive. Each of the fou~ components of the ~adiation budget (up and down, 

longwave and sho~twave) was individually measu~ed with an Eppley the~mocouple 

inst~ument. The inst~uments we~e periodically inte~calibrated by turning the no~mally downwa~d-facing inst~uments up fo~ a few hou~s each week. The 

absolute calib~ation of the data is dependent on the manufacture~'s 

calib~ation and on in-house calib~ation of the solar inst~uments. No 

inte~calib~ation between the longwave and sho~twave inst~uments was made. 

Also, py~geomete~ dome sola~ heating was not co~~ected for. The py~geomete~ 

output signal was taken di~ectly f~om the batte~y-compensated ci~cuit, and no 

tempe~ature co~ ~ections we~e applied . Additional p~ocessing and calib~ation 

of these data are necessa~y to ensure the most accurate possible ~esults. 

27 
• • 

o 

8Ri, 1977 - I SS I fWN I P 

RVG OVER AjR t',. 3 [NT(R'/AL 

• -o 5 ~o-6 C-7 -o-C--C )0 

1':[;":;-;1':[ .:. ;, :-;,"i.JJ 

SMO 1977 -1 981 f WNI P 

AVG OVER AI R Mi=-,SS l NT::::f\VRL 

r II" 

T r ,. 

1 PI' 

. , iI" ', 

:~1 ~ :+-k- [ a 

:;; I-f--i _~. l--f-.j~ LOI 

'" - l-f-.t- ' . -Lr, . . ~ ~. hf- -I-~_L~ ~ ~r RG2 -' L~ RGS 

• 

.+-----c---~o_--~----_c----~ , , R[LAi!V( A;~ MASS 

r!LO 1977 - 193 i 

.~ 

FHNI P 

NT [RV~,L 

o 

OOl 

P::i2 

RGB 

• 

.+---------, o-------~---- , -----, 

RELATIvE AL'l: r.ASS 

S?O 1977 -I S81 f~N I P 

" ... 'I F:V;; OV :::: ~ AIR r:;SS !N:-C'VF:1.. 

Figu~e --Di~ect beam solar i~~adiance in fou~ spect~al bands, (Q) 0.28-

3.0~ , (OG1) 0. 53-3 .0 , (RG2) 0.63-3.0 , and (RGB) 0.695-3 .0 ~m fo~ a 5-y~ pe~iod f~om each obse~vato~y as indicated . Data a~e plotted and ave~aged at the midpoint of each 0.2 ai~ mass inte~val. 

o 

:J 

R 

The ~adiation budget at a given l ocation such as BRW is determined by 

many va~iables : sola~ position, cloud cove~, su~face ~eflectivity, su~face and ai~ tempe~atu~e , and atmosphe~ic composition . By meas~ing each of the fou~ 

budget components sepa~ately , it will be easie~ to determine which va~iables 

a~e ~esponsible fo~ any obse~ved changes in the ~adiation budget . Identification of ~adiation budget pe~t~bations and thei~ causes is the goal of 

this meas~ement p~oject . C~~ently the data ~eco~d is too sho~t to war~ant 

pe~t~bation analysis. 

28 
NET SriORHIAVE 

BP>! 1985 

, . 

. ' 

' .. .. 

" . :,', ~ .' . ' . 

" ' , .. ' .., .. . ,"' 

IIET LO GWAVE 

BRH 1985 

..J :.:'.',,':~ .. 5 o+--------~~~~"'·· ~ ..... ------- o+-----, .. ~( -.. - .-C. - .--:.:.-. :'C-•• ,.' "'--.~. ~~~,", :'. "":'P':""""·~·· :':'" :. "': I- :. ,. '.' . , ~ :~ .. ~ . ~~ 0 

';+.---- JUN __ ---_-_~1~98-5~~~~~~~~ JUL AUG = ~ 1m ooc ;j+---~ ----------'O--8-5----------_~ ~ _ = OCT ~ ace 

MOtnH 110lHH 

~IET RAO I AT I 011 

BRei 1985 

.... '/-", .... .. . . 

. ," . " '~. .'. : ....... . 

...... , 

8 o-i---------~--"'.~'~:'T-,;;:-:> :.&.o/'r~'?: 

~ 

Figure 5.--Net shortwave, longwave, and all-wave radiation 

fluxes for 7 months of 1985 at 

BRW . Positive flux is taken as 

downward. The measurement 

technique is described in the 

text . 

.::~ 

<c' 

o 

JUN JUL AUG SEP 

MONTH 

OCT NOV OEC 

MLO STRATOSPHERIC AEROSOL LIDAR OBSERVATIONS 

Lidar observations continued at MLO at a rate of once per week. In late 

November a new stratospheric aerosol cloud appeared and continued to be quite 

evident into early 1986. This stratospheric cloud appeared first at around 

27-km altitude and later between 20 and 23 km. It has tentatively been 

attributed to the 13 November 1985 eruption in Columbia of the volcano Nevada 

del Ruiz. Figure 6 shows the six lidar observations taken in November. The 

strong scattering layer above 25 km on 26 and 27 November is believed to be 

the Ruiz plume. 

29 
w 

c 

35 

30-

::::J 20- ~ 

H 

~ - J 

~ T 

15+ 

, INTEGRATED NR95 COEF. !6-33KM 

INDICATES RVIi . MEASURED PROFILE 05 - '22~.O · as 

10..,. ! OSNOV' as liNOy"aS 'lONOV'as 22NQV'SS 

1.0Xl0-\,.-1~ .1 1. 2XIO-".,. -1. o. 9XIO·-t.,. -1. 

26NOV'BS 27NOV'SS 

L 7XI0-\,. -1. 1 . • XI0·<4.,. -It 

,-+-<:++++++:+ __ :;'.:.' c:H'.:::,3 ..,.::';.::.6.....:';: .• :.-+2;:.2:.,+2:;:.5:..,.--+-+:;1.:.' ....:;1.:::,3 ...,.:';.::.6.....:';: .'....,:2:;:. 2'.-+2~5~-:;-.:;1.~' ~1.,:,3 ~';.::6.....:';: .• ....,:2:;:. 2~2';:,5 5~ 

'---_'_.'_'_.3 __ ' ._6 _'._' _2 .:..2=---2.:...5_=---'_.'_':....3=---':....6_.:.' . .:,' ,:.2.",2 ~2i5---"c::'-'--1.3 _ 6 ~~2:~_ -=- ___ '"0 _ __ I 

asp RATIO 

Figure 6.--Six lidar backscatter profiles taken at MLO in November 1985. 

A total of 367 lidar measurements was acquired at MLO from 1974-1985. 

These measurements were summarized in terms of yearly averaged profiles of 

optical thickness per kilometer and the standard deviations that are mainly 

composed of the natural variability and the measurement uncertainty. The 

number of observations per year has varied considerably. For example , in 1974 

the number was 4 (the lowest of all years) and in 1982 it was 67 (the highest 

of all years). Figure 7 displays average optical thickness profiles for 1974-

1985. To facilitate plotting, the abscissa is scaled to accommodate the large 

changes that occur between quiescent and perturbed years. The years having 

the lowest optical thickness are 1976-1979. Only five profiles were obtained 

in 1979, so the result may be questioned somewhat for its representativeness. 

DeLuisi et al. (1986) gave the numerical values and standard deviations 

in tabular form for the profiles displayed in fig. 6. These data should be 

quite useful for studies of stratospheric aerosol effects on climate and 

optical remote sensing. More details on summaries of lidar observations can 

be obtained from NOAA data reports issued earlier by GMCC. 

GMCC SOLAR RADIATION FACILITY 

During 1985 , the NOAA SRF merged with the GMCC ARM group. Although the 

SRF has been located in Boulder since 1975, it operated independently when it 

was transferred from the NWS to ERL/ARL. 

The primary purposes of the facility are maintenance of NOAA radiometric 

standards, calibration of NOAA pyranometers and pyrheliometers for the NOAA 

national network, and maintenance of traceability of the NOAA standards to the 

World Radiometric Reference in Davos, Switzerland. 

30 
E 

::<-

OJ 

'" ::> 

t: 

!:i 

< 

29 29 29 29 

211 1974 28 28 '" 1975 1976 1977 27 27 Z7 Z7 

26 26 Z6 26 

2S 2S 2S 2S 

21 21 " 24 

23 23 23 23 

22 22 22 22 

21 21 21 2 1 

2. 20 20 20 

19 19 19 19 

18 18 18 18 

17 17 17 17 

l' l' l' l' 

15 15 15 15 

o~U~~~~~~~~~ °UU~~~~~~ n~uuuu u~nuuu 

29 

1976 1979 1980 28 1981 Z7 

2S ,. 25 21 2S 2S 

24 23 24 21 

23 23 23 22 22 21 22 22 

2 1 21 2 1 20 20 2. 20 

19 19 19 19 

18 18 18 '8 

17 17 17 17 

16 l' 16 16 

15 15 15 150 nnnn ~ tnOtn2~OLl10tlll'" 

O~H~~UU HUUU 8 §§§§§88iHi 8 ~ ~ ... . ~~O~.C: 

•• •• 31 .. 3B 1982 '" 1983 32 1984 "" 1985 " 

31 " 31 30 30 

32 32 28 28 

30 30 26 " 211 211 

26 

,. 24 26 

21 21 22 22 

22 22 2. 20 

20 2. 18 18 18 18 

16 16 16 16 

" 11 11 

8°88§§~~g~;;S 0 - N ~ 8 81! ~ 8!iI 1;1 1;1 ~ o~~~~~~~~~~~~~~~ "0 ~ n ~ ON... ID 

" ....... .. . ~ ~ ~ ~ 6, 

Figure 7.--Plots of annual average aerosol profiles: altitude vs. optical 

thickness per kilometer (6,) for years 1974-1985 . Note that the abscissa 

scale changes according to the magnitude of the aerosol cloud maximum. 

31 
Ppimapy pefepence instpuments of the facility ape two absolute cavity 

padiometeps, a TMI Mapk VI (SN 67502), and an Eppley model HF (SN 157~5). 

Tpaceability to the Wopld Radiometpic Refepence Scale is by means of the TMI 

SN 67502 and its papticipation in the IPC held in Davos in 1975, 1980, and 

1985. Both the TMI and the HF have also papticipated in seven NRIP events 

dating fpom 1978 held in New Rivep , Api zona , at the DSET labopatopy 

facility . Histopically, the NRIP's have been scheduled apppoximately evepy 2 

yeaps duping the month of Novembep. Theip purpose is to establish a check on 

pepfopmance of papticipating absolute cavity padiometeps by compapison with a 

designated pefepence i nstpument (SN 67502) . A second purpose has been to 

allow papticipating padiometeps to compape with padiometeps with IPC histopies 

and establish unofficial tpaceability to the wopld pefepence . At ppesent, no 

officially sanctioned mechanism exists fop establishing such tpaceability. 

Plans fop 1986 include installation of peplacement instpument tables on 

the poof and installation of a new data acquisition system and micpocomputep 

fop data collection and analysis. 

Suppopt activities fop the NOAA national netwopk during 1985 included 

dpafting of the RFP fop new "smapt" solap tpackeps, scheduled to peplace those 

cuppently in use, and the initial ppototype testing of the new netwopk IBM PCbased data acquisition system . 

TURBIDITY 

The 10 NOAA atmosphepic turbidity stations within the contiguous United 

States wepe bpought undep the GMCC ARM Gpoup at the beginning of 1985 . Turbidity obsepvations continued at these stations and at the foup baseline 

stations duping 1985. A list of the 1~ stations and the wavelengths at which 

turbidity is measuped is given in table 3. 

The wopking instpument at most of the 1~ stations is the NOAA J-sepies 

sunphotometep. A new calibpation ppocedure initiated in late 198~ was pefined 

and continued in 1985. In the ppevious calibpation scheme, a designated 

standapd J-sepies instpument was calibpated pepeatedly by the Langley pl ot 

method in Bouldep . The othep J-sepies sunphotometeps wepe calibpated in 

intepcompapisons with this instpument. In the new scheme, a high-ppecision, 

automated, tempepatupe-stabilized PMOD-type sunphotomete~ is calib~ated daily 

at MLO whe~e mo~e accu~ate and consistent Langley plot calib~ations ape 

possible . The PMOD-type sunphotomete~ is ~eturned to Boulde~ about evepy 4 

months fop inte~compapisons with the J-se~ies inst~uments . This p~ocedure 

ensures gPeate~ accuracy in the calibpations assigned to field instpuments. 

Howeve~, it delays the p~ocessing of field measurements because of the cycle 

time of the PMOD-type inst~uments between MLO and Bouldep . 

While this new p~ocedure is supepio~ to the p~evious p~ocedure, the~e ape 

still some p~oblems associated with it and with the instpuments themselves . Two of the filte~s in the PMOD-type sunphotomete~ failed in Appil 1985. It 

took until Septembep to obtain ~eplacement filte~s and get the instpument back 

in the system. This inte~~upted the scheduled cycles of inte~compa~isons fo~ 

summe~ and fall 1985. Even aftep ~eplacement of the bad filteps , an unusually 

32 
Table 3.--GMCC turbidity monitoring sites and filter wavelengths 

for sunphotometers used at each site 

Station Sun photometer wavelengths (nm) 

Barrow, AK* 380 , 500, 778 , 862 

Mauna Loa , HI* 380 , 500 , 778 , 862 

Samoa* 380 , 500 , 778 , 862 

South Pole* 380 , 500 , 778 , 862 

Alamosa, CO* 380, 500 

Atlantic City , NJ 380 , 500 

Boulder , CO 380 , 500 , 778 , 862 

Bismarck, NO 380 , 500 

Cari bou, ME* 380, 500 

Huron, SO 380, 500 

Meridian, MS* 380 , 500 

Salem , IL* 380 , 500 

Tallahassee , FL 380, 500 

Victoria, TX* 380, 500 

*BAPMoN stations 

high, but acceptable drift was observed in the replacement f i lters. In-house 

design and oonstruction of two new preciSion sunphotometers oontinued in 

1985 . Once these are working, the calibration process should be less 

vulnerable to the breakdown of a standard instrument. 

Apparent shifts in filter transmission also proved to be a problem with 

many of the J-series instruments. The result of these shifts is a substantial 

change in calibration constants over the period of a year . Fortunately, in 

many instances , the change is linear with time (see fig . 8). A partial 

solution to the data analysis problems associated with calibration changes is 

recycling and recalibrating instruments every 4 to 6 months. GMCC is seeking 

ways to reduce the filter decay rate so that calibrations can be done at 

longer time intervals . 

The data analysis software for the turbidity project was completely 

revised in 1985. Data for 1983-1985 for Boulder, CO (see fig . 9) , and 1983 

through February 1985 for the nine remaining stations in the U.S. network have 

been processed. 

Data for Boulder and other stations show a clear annual cycle with maxima 

in the spring or summer months and minima during November, December , or 

January . The impact of the eruption of El Chichon is visible at many stations 

and appears as a slow downward trend in optical depths since the beginning of 

the record in early 1983 . 

33 
. 

ci 

, 

, .. 

~.-; 

, 

a 

~~ 0-

I • ci ~ 

o 

1302 JeD M1 Ll eR"' I!O rl f1 [S I LR) 

""'0 - --c --- -, 

I 

"'ID I 

, 

, 

z 

~ 2000 

i 

J 

< 1500 ~ ---------~ u 

1000 

. 

J '"0 ,~, , .. , , ... , .. , ,- "" nAR 

Figure 8.--Linear drift in J-Series sunphotometer calibrations . 

IlCL n[RDSQ. OPT I Cfl.... I)[ PTlt5 : ·mn tlM 

yt..:rn 

OQ R[ROSD... Of'11 CIlL 1111 ' 111"" : 77B tlN 

Figure 9.--Daily average 

at Boulder for 380, 500 , 

. 

" 

o 

ci 

un... A[R05£l. OPT I Crt! IIn 'lIt" : ' ,nu NN 

.. : 

: ?,ji4;v.;i~;:,/jj.t/~;~: r. :".~;\;';~::~ .----.--,--..--~ •• ~ •• • ••• , • • • .• I 

6 1 Ir.> lib 

rrm '-------

Bo... P£ROS(L OI'TICIl orr II 15: IJb2 NN 

11.1'R 

aerosol optical depths 

778, and 862 rum. 

34 
3.2 Special Projects 

AEROSOL CORRECTION TO THE UMKHER OZONE PROFILE 

AT MLO, a long-term series of concurrent Umkehr observations of 

stratospheric ozone and lidar observations of stratospheric aerosol from the 

EI Chichon eruption of March-April 1982 permitted an empirical analysis of the 

error to the Umkehr ozone profile caused by a significant optical effect of 

the stratospheric aerosol. The effect is due to the separation of the 

effective primary scattering layers near twilight, where the short wavelength 

(311.4 nm) is near 40 km and the long wavelength (332.3 nm) is near 25 km, 

which is often directly located in the aerosol layer. The aerosol layer near 

25 km attenuates the solar UV radiation at 332.3 nm, traveling a tangential 

path, and this is interpreted by the Umkehr inversion algorithm as less ozone 

above the ozone maximum. The error becomes increasingly worse with increasing 

altitude . 

Theoretical calculations for all orders of scattering by Dave et al . (1980) modeled the physical processes of the error; some experimental 

verification was done by DeLuisi (1979) and Reinsel et al. (1984). However, 

the concurrent lidar and Umkehr data provided a unique data set for 

experimental investigation of the error. The error analysis is an iterative 

regression on the departure of the Umkehr stratospheric ozone from a normal 

condition that exists after the volcanic aerosol has diminished. 

Figure 10 compares results from Dave et al. (1980) , Reinsel et. al. 

(1984) , and the present study. The outcome is encouraging because the 

experimental results closely match the theoretical results, thus providing 

confidence in the methods used in the theoretical calculations for a spherical 

atmosphere. The great value of the present result is that it lends further 

credibility to the use of theoretical stratospheric aerosol corrections to 

long-term Umkehr measurements for detecting trends in stratospheriC ozone . 

10,-,-,-,-,-,-,-,-,-,-.-", 

9 

8 

es 7 

:; '" 6 ::> 

z 

0: 5 w 5 4 

3 

2 

----THEORETICAL 

--EMPIRICAL 

REINSEL [l Al . 

ERROR % PER 0.01 OPTICAL THICKNESS 

Figure 10.--Percent error to the Umkehr 

ozone profile per 0.01 optical thickness of stratospheric aerosol at 700 nm 

for layers 1-9: theoretical (Dave et 

al., 1980--dashed); experimental 

(Reinsel et al., 1984; Mauna Loa, this 

study--solid). Two different ozone 

profiles having total ozone amounts of 

300 milli-atm-cm are given as 300-1 and 

300-2. 

35 
3.3 Refer'ences 

Bodhaine , B. A. , 1979. MeasUr'ement of the Rayleigh scatter'ing pr'oper'ties of 

some gases with a nephelometer' . Applied Optics 18 :121-125. 

Bodhaine, B. A., and J. J. DeLuisi , 1985. An aer'osol climatology of Samoa. 

Jour'nal of Atmospher'ic Chemistr'Y 3 :107-122. 

Bodhaine , B. A., and J . M. Har'r'is (Eds .) , 1982 . Geophysical Monitor'ing for' 

Climatic Change , No . 10 : Summar'Y Repor't 1981 . NOAA Envir'onmental Resear'ch 

Labor'ator'ies, Boulder' , CO, 158 pp. 

Bodhai ne, B. A. , J. J. DeLuisi, J. M. Har'r'is , P. Houmer'e, and S. Bauman, 

1986. Aer'osol measUr'ements at the South Pole . Tellus , in Pr'ess. 

Bodhaine , B. A. , J. J. DeLuisi , J. M. Har'r'is , P. Houmer'e , and S. Bauman , 

1987 . PIXE analysis of South Pole aer'osol . Nuclear' Instr'uments and 

Methods, in pr'ess . 

Dave, J. J. , J. J. DeLuisi , and C. L. Mateer', 1980 . Results of a 

compr'ehensive theor'etical examination of the optical effects of aer'osols 

on the Umkehr' measUr'ement. Paper's pr'esented at the WMO Technical 

Confer'ence on Regional and Global Obser'vation of Atmospher'ic Pollution 

Relative to Climate , Boulder' , CO , 20-24 August 1979 , WMO No. 549 , Spec. 

Envir'on . Rep . No. 14, WOr'ld Meteor'ological Or'ganization, Geneva , Swi tzer'land, 15-22. 

DeLuisi , J. J., 1979 . Umkehr' ver'tical ozone pr'ofile er'r'or's caused by the 

pr'esence of str'atospher'ic aer'osols. JOUr'nal of Geophysical Resear'ch 

84:1766-1770. 

DeLuisi , J., T. DeFoor' , and D. Longenecker' , 1986 . Li dar' obser'vati ons of 

str'atospher'ic aer'osol over' Mauna Loa Obser'vator'Y : 1984-1985. NOAA Data 

Repor't , NOAA Envir'onmental Resear'ch Labor'ator'ies , Boulder' , CO , in pr'ess . 

Hanson, K. J . (Ed .) , 1977 . Geophysical Monitor'ing for' Climatic Change , No . 5 : 

Summar'y Repor't 1976. NOAA Envir'onmental Resear'ch Labor'ator'ies , Boulder' , CO , 110 pp. 

Mi ller' , J. M. (Ed.) , 1975 . Geophysical Monitor'i ng for' Climatic Change , No . 3: 

Summar'Y Repor't 197 4. NOAA Envir'onmental Resear'ch Labor'ator'ies, Boulder' , CO , 107 pp. 

Reinsel, G. C. , G. C. Tiao , J. J. DeLuisi , C. L. Mateer' , A. J. Miller' , and J. 

E. Fr'eder'ick , 1984. Analysis of upper' str'atospher'ic Umkehr' ozone pr'ofile 

data for' tr'ends and the effects of str'atospher'ic aer'osols . Jour'nal of 

Geophysical Resear'ch 89 :4833-4840. 

36 
4. CARBON DIOXIDE GROUP 

4.1 Continuing P~ograms 

CONTINUOUS ANALYZERS 

The in situ NDIR CO2 analyze~s at the fou~ GMCC obse~vato~ies continued 

to ope~ate in 1985. The p~elimin~y monthly and annual means fo~ each of the obse~vato~ies fo~ 1985 a~e shown in table 1. The complete ~eco~d fo~ each 

station is shown in fig. 1. Daily ave~ages fo~ 1985 a~e shown in fig. 2, 

showing the dec~eased amplitude of the seasonal cycle and dec~eased 

va~iability when moving f~om no~th to south. 

Data acquisition p~ocedu~es ~emained 

the CAMS data acquisition units in 1984. ~ef~bished in Decembe~. 

the same since the installation of 

The SPO analyze~ system was 

The in-house calib~ation of C02-in-ai~ ~efe~ence gases fo~ GMCC continued 

in 1985 ; 170 calib~ations we~e pe~fo~ed. The GMCC second~y standa~ds we~e 

calib~ated by SIO in 1985 , and ~esults we~e ~epo~ted in the WMO X85 

p~ovisional scale. A new Ult~amat 3 NDIR CO2 analyze~ , manufact~ed by 

Siemens Co~po~ation of West Ge~any, was pu~chased. The Ult~amat 3 will be 

used fo~ the tank calib~ation p~og~am . This analyze~ exhibits greate~ 

stability and p~ecision than the URAS 2T analyze~s c~~ently being used . 

m , r __ - __ -_-____ - _ _ , 

1

.-·····. 9'1W 

I"ILO 

"'r = SnO 

'" ,., 

~ J15 

U 

'" 

~"', : : 

( \ji! 

i :. 11 m . \.1 

J 

, !' .. : . ./ ~ 

:; y 

j 

, 

'" ,",,;;,,;,-,;-.,,;,-, 7.";;;",",,,c;o,,",. 7.",;;""',0;,,.-',70,,-;;;,,"'7,;;;,,;;', ,-;;";;;""'7";;;,,;'-,-;;,,.;-;,';";,,;;; .. :-",:;;,,,,.1, 

YEAR 

Fig~e 1 --P~ovisional selected 

monthly mean CO2 concent~ations 

f~om continuous meas~ements at BRW , MLO , SMO , and SPO. Values a~e in ppm 

with ~espect to ~y ai~ (1973-1984, 

X81 mole f~action scale; 1985, x85 

mole f~action scale) . 

37 

"'r : a ... .. _. '~, ::""'

-.' .... . I' 

U I .~~ .... . 

Ill S 

Figu~e 2. --Daily ave~ages of p~o

visionally selected continuous meas~ements at BRW, MLO, SMO, and 

SPO. 
Table 1 P~ovisional selec t ed monthly and annual mean CO2 concentrat ions fo~ continuous meas ~e ents at BRW, MLO , SMO , and SPO 

Yea r' 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 34 1.5 34 1.0 340 .8 339 .4 332 .6 327 .7 327 .4 332 .1 338 .8 339 .4 336 .7 1979 340.1 341 .3 342 .5 342 .4 342 . 9 342 .0 333 .6 327 .7 329 .3 333 . 1 338 . 1 3'11 .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 . 1 348 . 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 1985 349 .8 349 .5 350 .5 351. 4 352 . 5 349 .9 343 . 4 337 . 4 338 .2 344 .3 34"1 .7 349 .7 347 .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 . 'I 343 .0 345 .3 345 .9 345 . 4 344 .2 342 . 1 340 . 1 340 .2 3'11 . 4 343 .0 342 .9 1984 343 .6 344 .5 345 .1 347 .3 346 .6 34~ 0 342 .7 340 .9 341 .1 342 .8 344 .3 344 .2 1985 344 .9 345 .6 347 .2 347.6 348 .5 347 .9 346 .0 343 .9 342 .6 342 .6 34 1' .1 345 .5 345 .5 

SMD 

1973 

197 4 

1975 

1976 332 .4 331.9 331· 3 331. 2 330 .6 33 1. 3 331 .1 331 .1 331 .3 331 .5 331 .9 331 .9 331 .5 1977 33 1. 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 1981 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 3

'

10 .1 340 .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 1984 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 1985 343 .8 344.0 344.1 343.8 34 4. 3 344 .2 344 . 1 343 .7 344 .3 344 .2 344 .2 344 .5 344 .1 

SPO 

1973 

1974 

1975 329 . I 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 .6 331 .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 341.8 34 1.7 341. 4 341.4 34 1.5 341.7 34 2.0 342.7 343 .1 343 .4 343 .2 343 .0 342 .2 1985 342 .9 342.7 342 .6 342.7 342 .9 343 . 3 343 .7 344 .2 344 .7 345 .0 3"5 .0 344 .5 343 .7 

Note : fo r' 1913 -1 98 ~ the values are i n the X81 mole f raction scale , for 1985 in the x8S scale . The scale discontinuity is on the o rde r of a f ew hundredths of a ppm . 

38 
FLASK SAMPLE CO2 MEASUREMENTS 

The dete~mination of the tempo~al and spatial dist~ibutions of atmosphe~ic CO2 concent~ation by collecting whole ai~ samples in glass flasks 

continued in 1985. Fo~ details of the sampling and analysis methods and an inte~p~etation of the 1968-1982 CO2 data see Komhy~ et al . (1985) . 

In 1985 the flask sampling netwo~k was modified by the addition of fou~ 

and the deletion of two sampling sites. Sampling was begun at Ale~t, N.W.T. , 

Canada in coope~ation with the AES; Shemya Island, AK; in coope~ation with the 

U.S. Ai~ Fo~ce; Midway Island in coope~ation with the U.S. Navy and ITT; and 

South Geo~gia Island in coope~ation with the B~itish Anta~ctic Su~vey. 

Sampling was discontinued at Kaito~ete Spit , New Zealand, afte~ compa~isons 

with samples collected at Cape G~im, Tasmania, confi~ed that the new Zealand 

site was too heavily influenced by local sou~ces and sinks to be ~egionally 

~ep~esentative . Sampling at Cape G~im continues to give excellent ~esults. 

The Kitt Peak, AZ , site was ~opped f~om the netwo~k because of inf~equent and 

inconsistent sampling and the difficulty inhe~ent in obtaining ~ep~esentative 

flask samples in a continental ~egion . Samples may be collected occasionally 

at Kitt Peak to p~ovide s~face meas~ements in suppo~t of a total column CO2 measu~ement p~og~am by Battelle No~thwest Labo~ato~y. 

The flask sampling netwo~k in 1985 consisted of 26 sampling sites (fig. 3 

and table 2). The p~esent fo~ of the netwo~k is the ~esult of an ongoing 

evaluation of the CO2 data to dete~ine whe~e gaps in cove~age may exist 

(e .g., Ale~t and South Geo~gia Island) o~ whe~e a site fo~ a given latitude 

zone may be ~eplaced by anothe~ site bette~ suited to meas~ing ~egionally 

~ep~esentative ai~ at that latitude (e .g ., Shemya and Midway Islands as 

opposed to Cold Bay and Key Biscayne). Also, some ove~lap in sampling with 

othe~ labo~ato~ies (e.g. AES at Ale~t and CSIRO at Cape G~im) is desi~able to 

help monit ~ and imp ove the compa~ability of meas~ements made by diffe~ent 

g~oups . 

" 

20' S 

,,' , 

sevr"PQl£ 

• 

• SOUl" Clc;:H;U. 

' .. "" 

Figu~e 3.--Locations of GMCC flask sampling netwo~k sites in 1985 . 

39 
Table 2. --GMCC flask netwopk sampling si tes dUl"ing 1985 

Code Station Lati tude Longitude Elevation 

(deg) (deg) (m) 

ALT Alept , N.W. T., Canada 82 . 50N 62.33W 6 

AMS Ams tepdam I. 37.95S 77 . 53E 150 

ACS Ascens i on 1. 7. 92S 14 . 42W 54 

AVI St. Cpoix , VI 17 . 75N 64.75W 3 

AZR Tepcei pa 1. , Azopes 38.75N 27 . 08\01 30 

BRW BarTow, AI< 71.32N 156.60W 11 

CBA Cold Bay, AI< 55 . 20N 162.72W 25 

CGO Cape Gpim , Tasmania 40.68s 144.73E 94 

CHR ChPi s tmas 1. 2.00N 157. 30W 3 

CM) Cape Meapes, OR 45.00N 124.00w 30 

COS Cosmos , Pepu 12.12S 75 . 33W 4600 

GMI Guam , MaPiana I. 13 . 43N 144.78E 2 

HBA Halley Bay, Ant. 75.67S 25 . 50\-1 0 

KEY Key Biscayne , FL 25.67N 80 . 171-1 3 

KUM Cape Kumukahi, HI 19 . 52N 1 54 . 82\01 3 

MBC Mould Bay , Canada 76.23N 11 9. 33W 15 

MID Midway 1. 28.20N 177.38\01 4 

MLO Mauna Loa , HI 19.53N 155.58w 3397 

NWR Niwot Ridge , CO 40 . 05N 105.63W 3749 

PSA Palmep Station , Ant. 64.92S 64.00w 10 

SEY Mahe I ., Seychelles 4.67S 55 . 17E 3 

SGI South Geopgia I. 54 .00S 38 . 00W ? 

SHM Shemya 1. 52.75N 174 . 08E 40 

SM) Cape Matatula, Am . Samoa 14.25S 170.571-1 30 

SPO South Pole, Ant. 89 .98S 24.80w 2810 

STM Station M 66.00N 2.00E 0 

Fop compapison pUl"poses , a small shipment of flasks was sent to Tohoku 

Univepsity , Japan , fop collecting samples at Syowa Station , the Japanese 

Antapctic pesearch site. The data from these flasks will be compared with the 

Japanese in situ continuous analyzer and flask measUl"ements. Similaply , the 

GMCC CO2 data for Amsterdam Island have been compared with in situ 

meaSUl"ements made by the CFR . The results indicate good agreement between 

GMCC and CFR following the introduction of the GMCC battery-powered portable 

sampling unit in 1982 . Prior to that time the GMCC data are -1 ppm higher and 

are more scattered than the CFR data (Gaudry et al .; CFR, France, unpublished 

manuscript, 1985) . 

Provisional annual mean CO2 concentrations for 1985 are given in table 

3. Sites for which a full year is lacking (Alept, Midway, Shemya, and South 

Georgia) are not included. The 1985 Halley Bay samples had not been received 

in Boulder at the time this report was written. The annual means in table 3 

are the result of preliminary data selection and CUl"ve fitting. The values 

ape also subject to revision based on final analysis of the calibration gases 

used for flask sample analysis . The annual means for 1981-1984 in table 3 

have been adjusted by -0.1-0.2 ppm on the basis of a reanalysis of the data 

Conway et al. ; NOAA/GMCC , Boulder; unpublished manuscPipt , 1985) . 

40 
Table 3.--Pr'ovisional annual mean atmos pher'i c CO2 concentr'ations 

(ppm r'elati ve to dr'Y air'--X83 mole fmction scale) for' the flask networ'k sites 

sat !on 1965 1969 1910 1911 1972 1973 191 U 1975 1976 1911 1918 1979 1980 1\I!1 1982 1983 198q 1955 

At!S 0 0 0 0 0 0 035.9 ) 337.8 339. ~ 339. ~ 3_1.1 3~2.) 3~3. 7 

.so 0 0 0 0 0 0 [337 . 3J 338. II 339. II 3~O. 7 )QZ.7 3~3. 7 )H. 7 

An 0 0 0 0 0 0 0 0 331. 1 339 .6 )~o. 3 3_0.9 3~2.0 3~3·2 3~S.O 

co 0 0 0 0 0 0 0 0 0 0 338. Q H9.~ 3~1. 3 3'3.0 3=~. ~ 3~6. 0 

e~w 0 0 321 ~ 3)0. 2 332.0 33. ~ )B.O 333.9 335.0 336.6 331. 7 )QO.l 3~1. ~ ]~2.1 ]Q).8 )Y5.2 3~6.5 

'" 0 0 0 0 0 0 331. II 3~9.8 3Y\.O 3~1. II 3Y3. t, JUS. ~ 3Qt;. ~ 

'''' 0 0 0 0 0 0 0 0 0 0 0 3~2. 0 ;~ 3. u 

CO" 0 0 0 0 0 0 0 0 0 0 0 0 ) .:., II ]t5.7 

"'" 0 0 0 0 0 0 0 0 0 0 0 3'1 . 3 ]Y). O !I.S.O 346.6 

'" 0 0 0 0 0 0 0 0 0 0 339.7 0 0 0 0 

c.!'I! 0 0 0 0 0 0 0 0 0 331.1 3~O.O 3Q1.2 31,0 . ., 3~2. 7 3~t,.2 3~5. 6 

'" 0 0 0 0 0 0 0 0 0 0 0 0 0 ~". t, 31,2.6 [ J 

'" 0 0 0 330.7 (3n.~1 0 33Z.7 33S.2 336 . 7 338.8 (lUO.2 ) 3'1.7 3tl. 6 3Q3.~ )'5.0 3Q6.1 

ru. 0 0 0 0 0 0 )31.3 3)t . Q 335.7 H7.' :B9.3 3QO. (, )tl. <' )t2.6 Jut. 1 3Q5. Q 

"" 0 0 0 0 0 0 0 0 0 0 3tO .3 31, I. II 31,2. Q 3~3. 7 JU5.6 3Q6. ') 

I'!KO 0 0 0 0 0 0 0 0 0 0 0 337 . 3 0 0 0 0 0 <., 0 (3n8J 325 . 2 0 , 0 , 0 332.1 333.6 330; .2 336.1 336.9 3~0.' 3~1.0 3"".0; 3~~.0 3115 . 2 

~",!I 3B. I 32~. I 320;. ~ 32S . .. 326.3 330.2 33~. 0) 0 332. I 33~ .6 33~. 1 337 . 0 335.1 339.9 3~0. 9 3~2.0; 3:t . 6 3~S. 6 

!I!t 0 0 0 0 , 0 , 0 0 0 0 0 0 0 0 3_0.7 3~2.3 0 

'" 0 0 0 0 0 0 0 , 0 , 333. 9 330;.2 O J!.o;) 3~0. I 339.7 3~1.0 3~2. 7 3~3.S 

Stt 0 0 0 0 0 , , 0 0 0 , 0 339.] 3tO.l 3~0.S 3'1.1 3~3. 1\ 3~~ 6 

'"' 0 , 0 0 , DlO.2] ))0. IS HO.l 33' .S ;)2.8 33~, 3 3]6.0 335.1 339.3 3~O. ~ 3~1.5 3"}. t 3~~ . 3 

'"' 0 0 0 0 0 0 , 32;. ~ 330.2 331.5 333. 7 335.5 336.7 336.0; 339. :; 3t O.S ~. 1 3t 3. ~ 

no 0 3Z~. 0 326. t 326.~ 327.6 , , 0 0 0 0 0 0 0 0 0 0 0 

'"' 0 , 0 0 0 0 0 0 0 0 0 , 0 3~1. 6 3 ~1. 7 3~2.6 3~~ . 6 )'0;.0; 

"Ole: () • nUIOoe,. of Ln~erP'JIHed P'Jlnt3 ~ one- niH of lotil nuo:t>er or polnu : [1 • ,neoa:,lete year. 

Annual mean CO2 concentr'ation is plotted ver'sus sin(latitude) in fig. 4 

for' 1981-1985. It is appr'opr'iate to plot against sin(latitude) since equal 

inter'vals of sin (latitude) cOr'r'espond to equal ar'eas on the sUr'face of the 

ear'th . The CUr'ves in fig. 4 ar'e cubic spline curves fit to the data using the 

smoothi ng spline of Reinsch (1967). In this method the stiffness of the 

spline is deter'mined by the weights, Dy(i), assigned to the points . These 

weights should be the uncer'tainty associated with the annual mean value. For' 

1981-1984 the weights wer'e taken to be 30 , wher'e 0 is the statistical standard 

er'r'or' of the annual mean determined by an objective statistical method (Conway 

et al .; NOAA/GMCC Boulder' ; unpublished manuscr'ipt, 1985). Although this 

weight , and thus the ±30 er'r'or' bar's in fig . 4, over'states the uncer'tainty of 

t he annual mean at a given site, the smooth cUr'ves thus obtained suggest that 

30 is a r'easonable value for' the var'iability due to longitudinal gr'adients and 

indicates how well a site r'epr'esents a given zone. 

The over'all nOr'th-to-south gr'adient of -3 ppm is fair'ly consistent fr'om 

1981 thr'ough 1985. However', consider'able var'iability is obser'ved in the 

appear'ance of the equator'ial hump in CO2 concentr'ation. This feature in the 

annual mean gradient has been ascr'ibed to an equator'ial ocean sour'ce of 

atmospher'ic CO2 (Mook et al ., 1983; Pearman et al ., 1983 ). The near' absence 

of this "hump" in 1982 has been attr'ibuted to the inter'r'uption of the normal 

upwelling of cold water' with high CO2 super'saturations dUr'ing the 1982-1983 

ENSO event (Keeling and Revelle , 1985; Feely et al ., 1986). In 1983 a par'tial 

r'ecover'Y is obser'ved , and in 1984 the hump is well defi ned r'esulting in par't 

fr'om the addition of Chr'istmas Island to the networ'k in 1984. The latitude 

gradient for' 1985 is inter'esting in that only a slight equator'ial enhancement 

is obser'ved . Since 1985 was not an ENSO year' , these r'esults suggest the 

possi bility of significant var'iation in the equator'ial source of atmospher'ic 

CO2 not r'elated to ENSO events . 

41 
"7 . , I i I "1 '" ,,> , ~~r----rT j )<14 ------r -1--...---- J 30 i:iaS J J., 

3<15 [ 1 

;ii!~~~1 ". 

3<J 

3<, 

3<, 

3<0 

JJO 

- , -. 5 0 . > Si:-;(LATI7UDC) 

Figure 4.--Annual mean CO2 concentrations vs . sin (latitude) 

for the GMCC flask sampling 

network . Data plotted with the 

symbol (+) have not been included 

in fitting the curves. The 1981 

annual mean for AMS has been 

adjusted by -1 ppm on the basis of 

comparisons with CFR data. 

The 1984-1985 global CO2 grow~h rate was -1.2 ppm yr- 1• This rate is 

somewhat lower than the 1. 5 ppm yr 1 average of the past decade , which may be 

related to a decrease in the equatorial source . The 1984-1985 growth rate is 

still 2 times higher than the low growth rate associated with the 1982-1983 

ENSO event. 

FLASK SAMPLE METHANE MEASUREMENTS 

Measurement of methane in air samples from the NOAA/GMCC cooperative 

flask network continued through 1985. During this year , flask sampling was 

initiated at four additional si tes (Shemya Island , AK ; Alert, N. W. T., Canada ; 

Midway Island; and South Georgia Island), and terminated at Kaitorete Spit, 

New Zealand . The active sites in the network during 1985 are shown in both 

fig. 3 and table 2. 

Methane concentrations continued their l ong-term increase at all sampling 

sites. This is illustrated by monthly mean data fr om t wo sites (South Pole 

and Mould Bay) through January 1986 (fig. 5). The corresponding 12-mo r unning 

42 
1130 

Mould "1 0 

, ' 0 

1120 ", 0' , 00°0 0 

17 10 , ,,0 

, 

a 1100 Mou ld ... , 

lHO 000 1 a a 

0 000 CH, 00 a a 000 a (PPb) , a 00 " .. 00 000 a 000 SOllth Po l . 

a a 1590 

00 

• • • • "'" ". 1 sao .. • •• (PI'~1 ... • • • 

""" ~O\I h Pole 0°0°0 

00 " , , , 0° 0 " " , , 00 0 0 

"'" , , 00 

"" , ... 19115 

Figure 5.--Monthly mean background 

methane concentrations at SPO and 

Mould Bay, Canada. 

1570 .. •• 

• • 

1560 

1983 1984 1985 

Figure 6.--Twelve-month running mean 

methane concentrations at SPO and Mould 

Bay, Canada. Values are plotted at the 

midpoint of the appropriate interval. 

means (plotted at the midpoint of the appropriate interval) are shown in fig. 

6. The seasonal variations and the significant latitudinal difference in 

concentrations are apparent in fig. 6, where the vertical axis is unbroken. 

To emphasize features of the long-term increase, the vertical axis was 

broken in fig. 6. In particular , the 3-yr record of data at the South Pole 

shows clearly that the growth rate of methane has not been constant over this 

period. Twelve-month averages calculated directly from the background flask 

data are 1560 ppb (Feb 1983-Jan 1984 inclusive), 1576 ppb (Feb 1984-Jan 1985), 

and 1588 ppb (Feb 1985-Jan 1986), yielding respective 12-mo increases of 16 

ppb and 12 ppb. The average annual growth rate is 0.88% when referenced to 

the concentration at the midpoint of this 3-yr period. This long-term slowing 

of the methane growth rate has also been seen at other sites from middle to 

high latitudes of the Southern Hemisphere, and is most obvious in the long 

record from Cape Grim , Tasmania (see Steele et al., 1986). The reason for 

this slowing of the methane growth rate is not yet understood. 

If any slowing of the growth rate in methane is occurring at Mould Bay, 

it is not yet apparent from the data. However, any such change will be more 

difficult to detect at sites in the Northern Hemisphere, since the seasonal 

variations are not as well defined as in the Southern Hemisphere, and the 

magnitude of the seasonal variations may change from year to year. Thus, the 

12-mo running means used in this analysis are not able to completely suppress 

the seasonal changes . Nevertheless, the overall increase seen in methane at 

Mould Bay is comparable to that at the South Pole. 

43 
4. 2 Special Projects 

1985 OCEANOGRAPHIC ACTIVITIES ABOARD NOAA SHIP DISCOVERER 

The CO2 Group participated in the EPOCS and CO~ cruises aboard the NOAA 

Ship DISCOVERER during 1985. The cruise track is snown in fig . 7. A total of 

1199 hours of atmospheric air and 1101 hours of air equilibrated with surface 

ocean water were sampled for CO2 measurements between 24 May and 19 July . 

The Weiss-design custom-built gas chromatograph was set up aboard the 

ship prior to the ship 's departure on EPOCS leg 1 by GMCC personnel. The 

equipment was activated in San Diego prior to sailing on EPOCS leg 2. The 

monitoring program was operated on the CO2 cruise in the North Pacific between 

Honolulu and Kodiak by PMEL personnel . 

The 1985 monitoring program was identical in most respects to the 1984 

mode of operation Csee Nickerson , 1986 , p . 41) . Preliminary results are 

graphically depicted in figs . 8-10 . The mean atmospheric CO2 concentration is 

represented by a straight line and is intended to be a reference level for 

illustrating the CO2 undersaturation and supersaturation in the ocean surface 

waters. 

• 

• , 

Figure 7.--1985 DISCOVERER cruise C·· · ··). The solid circles 

show the locations of the GMCC flask network sites. 
'" 

... 

... E ". ~ 

~ '" N ". 0 

u 

~ '" 

'" 

'" 

no 

'" 

Figu~e 8 depicts the ~esults f~om 24 May-5 June f~om San Diego to about 

50 S, mostly along 1100W longitude. The equato~ial pa~tial p~ess~e of 

dissolved CO2 (pC02) peak exceeds 490 ppm at -2°N and -500 ppm in the inte~val 

4-5°S. Inasmuch as 50S ~ep~esents the southe~n t~ning point fo~ the c~uise 

t~ack , the equato~ial high p~ess~e feat~e was not fully ~esolved. It 

appea~s that the supe~satu~ation feat~e is split into two peaks at this 

longitude and is slightly skewed to the south with ~espect to the equato~ . 

These peaks ~ep~esent the highest de~ee of equato~ial supe~sat~ation so fa~ 

seen in ~ meas~ements in the Easte~n Pacific . F~om this one t~ack it is 

not clea~ hethe~ the high peak ~ep~esents the usual de~ee of supe~sat~ation 

fo~ this ~egion , o~ hethe~ this is an abno~mal condition seen in 1985. 

Fig~e 9 depicts the ~esults fo~ the westwa~d ~un along 50 S between 1100W 

and 1400w longitude with an excu~sion to 60 S nea~ 1400w to ~et~ieve an 

inst~umented buoy . It is clea~ that the unusual ~pC02 values that we~e seen 

on the 1100W t~ansect appea~ to be confined to the a~ea east of -113°W. West 

of this point the ~pC02 ~anges f~om 50 to 110 ppm with an ave~age of about 70 

ppm, typical of the usual diffe~ences obse~ved on p~evious t~ansects. The 

easte~n limit of the 500-ppm a~ea of high values is unknown, although pC02 values appea~ to be back in the 420-450 ppm ~ange at 95°W (Weiss; SIO, La 

Jolla , CA ; unpublished manusc~ipt , 1984. 

Figu~e 10 shows the equato~ial t~ansect at 1400w, the ~un into Honolulu , and the Hawaii to Alaska t~ack. The no~th side of the equato~ial t~ans t is 

nea~ly identical to the two ~eco~ds obtained in 1984 (Nicke~son, 1986, p. 41 , figs. 11 and 12) between the equato~ and 7-8°N. F~om -looN to -40 0 N, the 

rnos Lly unde~satu~ated ~egion seen in 1984 dUr"ing Ap~il-May has changed to an a~ea whe~e ai~ and sea su~f ce a~e in equilib~ium o~ slightly supe~sat~ated . 

The un~esolved plunge to about 300 ppm at 400 N obse~ved in 1984 can now be 

identified as the sub-A~ctic f~ nt in the 1985 data . 

DI SCOVERER 1985 

\A. 

" 

~ : ~ : ~ ~ , . , : : : 5 LAT (deg) 

'" 

'" 

'" .. ... ~ 

~ '" N ... 0 

u '" ~ 

'" 

'" 

'" 

: . . : )I'~ 

N N 

" -

DISCOVERER 1985 

n n 

. : n • 

LONC (de g] 

: 

N 

Figu~e 8. --pC02 the along N-to-S 

t~ack at 1100 W longitude. 

Figu~e 9. - -pC02 along the E-to-W t~ack 

f~om 50 S, 1100W to 60 S, 140oW. 

45 
E 

~ 

~ 

ru 

0 

u 

~ 

." 

.n 

.,' 

' R 

.,' 

.n 

.n 

.,' 

.R 

.,' 

In 

~ ~ : ~ ~ 

5 

DISC OVERER 1985 

~\A ~ 

~ • ~ ~ ~ 

LAT [degJ 

~ 

~ ~ • • ~ 

N 

Figure 10 .--pC02 along the S-to-N 

t rack at 140 0W longi t ude , into 

Honolulu , then north to Kodiak 

Island , AK . 

4. 3 References 

Feely , R. A., R. H. Gammon , B. A. Taft , P. E. Pullen , L. S. Waterman , T. J . Conway , and J. F. Gendron , 1986. Distribution of chemical tracers i n the 

eastern equatorial Pacific during and after the 1982-83 El Nino/Southern 

Osc i llation event . Journal of Geophysical Research (submitted). 

Keeling , C. D., and R. Revelle , 1985 . Effects of El Ni no/Southern Oscillation 

on the atmospheric content of carbon dioxide. Meteoritics 20(2) :437-450 . 

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 CO2 distribution and 

variations from 1968-1982 NOAA/GMCC CO2 flask sample data . Journal of 

Geophysical Resear ch 90(D3) :5567-5596. 

Mook , W. G., A., M. Koopmans , A. F. Carter , and C. D. Keeling , 1983 . 

Seasonal , latitudinal , and secular variations in the abundance and 

isotopic ratios of atmospheric carbon dioxide : 1, Results from land 

stations. Journal of Geophysical Research 88(C1S) :10, 915-10 , 933. 

Nickerson , E. C. (ed . ) 1986. 13: Summary Report 1984. 

Boulder , CO , 111 pp. 

Geophysical Monitoring for Climatic Change , No . NOAA Environmental Research Laboratories , 

Pearman , G. I ., P. Hyson , and P. J . Fraser , 1983 . The global distribution of 

atmospheric carbon dioxide : 1. Aspects of obser vations and modeling. 

Journal of Geophysical Research 88 (C6 ) : 3581-3590 . 

Reinsch, C. H., 1967 . Smoothing by spline functions. Numerische Mathematik 

10 :177-183. 

Steele , L. P., P. J. Fraser, R. A. Rasmussen , M. A. K. Khalil , T. J. Conway, 

A. J . Crawford , R. H. Gammon , K. A. Masarie , and K. W. Thoning , 1986. The 

global distribution of methane in the troposphere . Journal of Geophysical 

Research (in press) . 

46 
5. TRACE GASES GROUP 

5.1 Continuing P~ograms 

TOTAL OZONE 

Routine total ozone obse~vations we~e made with Dobson spect~ophotomete~s 

du~ing 1985 at 14 stations that constitute the U.S. total ozone station netwo~k (table 1). Of the 14 stations, 4 a~e ope~ated by GMCC pe~sonnel; 3 a~e fo~eign coope~ative stations; 3 ~e domestic coope~ative stations; and 4 ~e ope~ated by the NWS. 

Table 1.--U.S. Dobson ozone spect~ophotomete~ station netwo~k fo~ 1985 

Station 

Bism~ck, ND Ca~ibou, ME S~ 

Tallahassee, FL 

Nashville, TN 

SPO 

Wallops I., VA 

Huancayo, Pe~u 

F~esno, CA Boulde~, CO Poke~ Flat, AK ~O 

Pe~th, Aust~alia 

Haute P~ovence, F~ance 

Pe~iod of ~eco~d 

01 Jan 1963-p~esent 

01 Jan 1963-p~esent 

19 Dec 1975-p~esent 

02 May 1964-p~esent 

01 Jan 1963-p~esent 

17 Nov 1961-p~esent 

01 Jul 1967-p~esent 

14 Feb 1964-p~esent 

22 Jun 1983-p~esent 

01 Sep 1966-p~esent 

06 M~ 1984-p~esent 

02 Jan 1964-p~esent 

30 Jul 1984-p~esent 

02 Sep 1983-p~esent 

Inst. no. 

33 

34 

42 

58 

79 

80, 82 

38 

91, 87 

94 

61 

63 

76 

81 

85 

NOAA 

NOAA 

NOAA 

Agency 

NOAA; Fla. State Univ. 

NOAA 

NOAA 

NOAA; NASA 

NOAA; Huancayo Obs. 

NOAA 

NOAA 

NOAA; Univ. of Alaska 

NOAA 

NOAA; Aust. Met. Dept. 

NOAA; Obs. Haute P~ov. 

Daily 1985 total ozone amounts applicable to local appa~ent noon fo~ 

stations in the U.S. Dobson inst~ument netwo~k have been a~chived by the Wo~ld 

Ozone Data Cent~e, 4905 Duffe~in St~eet, Downsview, Onta~io M3H5T4, Canada, in 

Ozone Data fo~ the Wo~ld. Table 2 lists p~ovisional monthly mean total ozone 

amounts fo~ 1985 fo~ the NOAA obse~vato~ies and coope~ative stations. 

D~ing 1985, GMCC pe~sonnel continued to pa~ticipate in the WMO Global 

Ozone Resea~ch and Monito~ing P~oject to upgrade the quality of Dobson ozone spect~ophotomete~s t~oughout the wo~ld. Table 3 lists the inst~uments that we~e ~ecalib~ated ~elative to Wo~ld Stand~d Dobson Inst~ument No. 83 

maintained by GMCC in Boulde~, CO. 

In Novembe~ 1985, Dobson inst~ument No. 82 was shipped to the South Pole 

so that inst~ument No. 80 could be ~et~ned to Boulde~ fo~ ~ecalib~ation. 

Dobson inst~ument No. 87, installed at Huancayo, Pe~u, is automated fo~ Umkeh~ 

obse~vations. It ~eplaced inst~ument No. 91, which was in ope~ation at 

Huancayo since Septembe~ 1982. 

47 
Table 2.--Provisional 1985 mean total ozone amounts (mi 11 i -atm-cm) 

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

Bismarck, NO 325 360 361 349 327 339 311 335 299 297 336 345 

Caribou, ME 402 414 385 405 387 370 341 331 309 309 327 371 

SMC 264 264 257 262 263 245 254 263 270 275 274 268 

Tallahassee, FL 274 278 285 320 333 316 321 304 293 294 287 

Boulder, CO 329 338 322 339 328 315 297 298 295 278 314 301 

Poker Flat, AK 446 435 473 392 352 325 313 304 352 

MLO 231 232 250 272 282 280 281 266 264 254 260 251 

Nashville, TN 325 324 312 340 358 328 331 311 296 282 287 315 

spa 288 278 245 213 236 234 207 161 238 314 

Perth, Australia 283 267 272 276 276 263 286 296 304 310 292 278 

Wallops I., VA 328 329 317 333 335 336 324 315 302 281 289 323 

Haute Provence, 353 336 367 363 370 332 325 326 304 289 312 314 

(France) 

Huancayo, Peru 252 253 250 258 262 257 260 256 

Fresno, CA 305 324 333 333 334 321 308 306 305 289 297 310 

Table 3.-- Dobson spectrophotometers calibrated in 1985 

Country Station Instrument number 

Peru Huancayo 

United Kingdom Bracknell 

Uni ted States Boulder, CO 

United States South Pole, Antarctica 

Uni ted States Wallops Island, VA 

A new round of spectrophotometer calibrations in the global 

instrument station network was undertaken in March 1985 by means 

standard lamps. Results from all stations are expected in 1987. 

program was conducted in 1981 (Grass and Komhyr, 1985). 

87 

41 

72 

82 

38 

Dobson 

of traveling 

A similar 

Plans were formulated for conducting an international comparison of 

Dobson spectrophotometers and Brewer ozone photometers in Arosa, Switzerland, 

during summer 1986. 

TOTAL OZONE DECREASE AT SOUTH POLE 

Analysis of South Pole total ozone data for the years 1964-1985 (Komhyr 

et al., 1986a) showed that ozone has decreased at South Pole by 25% since the 

mid-1960's (fig. 1). Largest ozone decreases occurred during the months of 

October and November; smaller decreases occurred in other months, except 

48 
February months when ozone slightly increased. A similar decrease in ozone at 

Halley Bay , Antarctica , was attributed to ozone destruction by gas phase 

(Farman et al ., 1985) and heterogeneous (Solomon et al ., 1985) reactions 

involving CIOx and NOx photochemistry, which no doubt occur. However, 

analysis of tne South Pole data indicated that the decrease in ozone may be 

due predominantly to a change in atmospheric circulation and the transport of 

ozone into Antarctica . This change in ozone transport is manifested in a 

delay in recent compared with past years in the time of stratospheric warming 

in Antarctica (fig . 2), as well as in ozone decreases that have occurred 

periodically in Antarctica. These ozone decreases are probably related to the 

4-yr oscillation (FYO) in ozone (Hasebe 1980, 1983), and are influenced by 

Hadley and Brewer-Dobson circulations. In past years , substantial ozone 

recovery occurred (fig. 1) within 1 to 2 years following onset of an FYO 

event, but such recovery did not occur following the FYO event of 1980. 

Figure 3 presents additional evidence for a change in the transport of 

ozone to Antarctica. The latitudinal source regions of 10-day isobaric back 

trajectories of air parcels that arrived at McMurdo, Antarctica (78oS, 166°E) 

at 50 mb in October and November 1978 and 1985 are plotted in the figure. The 

trajectories were computed using the ARL/GMCC Trajectory Program (Harris , 1982). The marked difference for the 2 years in the frequency of outbreaks of 

subtropical , ozone-rich , stratospheric air transported to McMurdo is readily 

apparent. 

The slight increase in ozone at South Pole that has occurred in February 

months during 1964-1985 appears to be due to an increase with time in ozone 

trilllsport Lo Antarctica from the subtropical, stratospheric ozone production 

region . Vertical distribution ozone measurements have indicated that the 

transport occurs at pressure altitudes of 30 mb and above. As shown in fig. 

4, an episode of transport of an unusually large amount of ozone to South Pole 

occurred in early February 1984 (Komhyr et al., 1986). The increase in ozone 

measured at that time at South Pole was comparable in magnitude to ozone 

changes that occur during October and November months when large amounts of 

ozone are transported each year to Antarctica. 

OZONE VERTICAL DISTRIBUTION 

In late 1984, funding was obtained from NESDIS to conduct ozonesonde 

observations at three stations and Umkehr observations at fi ve stations to 

obtain atmospheric ozone vertical distribution data for validation of SBUV 

ozone data obtained aboard the NOAA F satellite. The ozonesonde observations 

are made with balloonborne ECC ozonesondes (Komhyr , 1969), and the Umkehr 

observations are made with automated Dobson spectrophotometers (Komhyr et al., 

1985). In addition, ECC ozonesonde observations were made as part of the SAGE 

II satellite ozone validation program from Boulder, CO; Laramie, WY; and 

Fai rbanks, AK . 

Weekly ECC ozonesonde flights began at Boulder, CO and Hilo, HI, in 

January 1985. The sounding program was expanded later in 1985 to include 

observations at Edmonton, Canada, in a cooperative endeavor with the AES . 

49 
325rrTlTTTTlITT-,-rrTT-,-rrrT"-' 

::j 

e-

" c 

0 215 N 

0 

a; 

" >-

250 

160.U. 

L 

4.1yr 4.7yr 6.3 yr .8 yr 

I 

64 66 68 70 78 80 82 84 86 

Year 

Figure 1.--South Pole 12-mo running 

plot of mean monthly total ozone data. 

Long vertical bars indicate times of 

of abrupt downward shifts in ozone. 

Short vertical arrow denote magnitudes 

of the shifts. 

E --ocr. NOV.-

w 30 1918 

0 

~ ~ .. 0 

V> 

50 

E, --OCT. 

w ; 30 ''''' 0 

~ .. ~ 0 

'" 

DAY 

Figure 3.--Latitudinal origin and 

frequency of 50-mb, 10-day, isobaric 

back trajectories arriving at 

McMurdo, Antarctica (18°S, 166°E) 

1 October to 18 November 1918 and 

1985. Hatched bars and crossed bars 

denote arrival times of 0000 and 

0012 GMT, respectively. 

50 

0; 

e. 

. 

~ 

~ 

~+-~--~--~~--~--~~--~--~~~ 1!lSi 1966 1964 1910 1912 \971 1976 191& I~ J9al l!IIIt 

'EAR 

Figure 2.--Differences in times of 

onset of stratospheric warming at 

South Pole during 1964-1985 

compared with the time of warming 

in 1918. The slope of the best 

fit line is 0.53 ± 0.48 day yr- 1 

"" Feb. 198-1 

"" 

.., 

'" 

"" 

"" --GIOUdy+ ---Clear 

"" 

0., 

Figure 4.--Sudden total ozone increase at SPO during 3-6 February 

1984. Total ozone observations 

were made with a Dobson spectrophotometer on cloudy sky and CC ' 

wavelengths (0); direct sun and CD 

wavelengths (~); and focused image 

of the s un and CD wa velengths (D) . 
Mean Boulde~ and Hilo 1985 seasonal ECC sonde data , fo~ mandato~y 

atmosphe~ic p~ess~e levels, a~e p~esented in table 4. Plots of the data e 

shown in figs. 5 and 6. All data we~e no~malized to Dobson spect~ophotomet e~ 

total ozone. Mean no~alization facto~s we~e 0.993 ± 0.038 fo~ Boulde~ and 

1.003 ± 0.059 fo~ Hilo, whe~e the indicated va~iabilities (standa~d 

deviations) include effects caused by nonsimultaneity of the ECC sonde and 

Dobson spect~ophotomete~ obse~vati ns, and imp~ecision in total ozone measu~ements that occu~ when obse~vations a~e made on cloudy sky. 

Table 4.--Seasonal ozone pa~tial p~ess~e data* fo~ mandat o~ y atmosphe~ic 

p~essu~e levels obtained f~om ECC ozonesonde soundings in Boulde~ and Hilo in 1985 

es~u:"e 60ulder H!lo 

(::It,) -,,! ntet' Spl" in~ S!.nr.er Aut.u:m Winter Spr ing SUm:er Auttr.J1 

,co " (37 . 71 '1.3 IJ(]9 . 5J 10. 7 " ( 31 ·8) 11 . , 111 (215 . 6) 11.0 9 (27 · 31 115.5 " (23 · 9) 10. 0 " 115. 1) 9.2 · 2 r' 6.1l 10.3 

lCCO 9 (]1. 7) 13. 5 " (26 . 1) 10. 0 " ( 15.8) 8.5 12 (13.]) 10. 2 

n:o " (}6 , :·1) a " 09. 9J 6. 3 " ( 39 . 11) 12 . 2 '" (~2 . 9) 3.8 9 () 1. Z1 12.0 " (33.5) 9. 6 " (28 .3) . 3.0 12 (25.71 ' . 3 

seo " 'z6 . :?) 1.8 · " ( }0.2) 6. ') " (29 . 7) 5.1 '" (2a .6) 10. 1 9 (24 , 3) 8.2 11 (28 .5) 8.8 " (20.3) 5.lI '2 121 .51 :'.3 

leO 11 25 . 3) 17. J '4 (21.5) 9. " " (18 . 8) 8.0 " (18 ,11) 12 .2 9 ( 15.]) lJ , 1 11 (21 . ::)) 5.6 11 (8. ) 2.2 '2 . 3.S} 9. :t 

,eo '1 '5' . J) 31 .3 · ~ (119 . 21 }6.0 " ' 7.3) 'I. ] ' ll (29.9) 21. 5 9 ( 13. 8) 5. , " I PI, 2) 1.6 11 (II,9) 1.5 · , 9.5) 1; •• 

'50 ' 1 6-:" . 21 52.9 · " (63.1) }lI , 1I ' " 21 .9) 15.2 ' , 139 . 7) 23.9 9 ( II. 9) 'l.9 11 f20.9) 111 . 5 11 (6.2) 2. 1 · , " 2.11 . ~ 

' 00 11 ' 53. 2) 36. '5 p (7;. J) 33. J '" ' JI . ~J 15.1 '" (60 . 7) 29.6 9 ( Pl . 4) 7. ~ 11 (26 . 9) 8. II ' 1 ( 16.B) 3.7 · , ' I ~.a) " . .) 

70 11:' 09 . J) ~1.! · " (as. 1 2l1 . 2 1 " 35 . ;) 12 · 3 . , (98 . 9) 2~ . ~ , (35 . 3) 12. 1 11 (58 . 0) 21.3 11 (1I9 .0; ~.1 ., ~5. "' 1 . .,. ~ 

" . F ' 35.9) :2. 6 · lI( 1 1;. ;'I' ': . ? " l' . _ . 9. 2 • ~(1: a. 51 .~ . 2 9 (71 . 7) 16 .3 l' '87 . ~, 11.0 " \ 96. 5~ 6. - , , -:: .: ) 

JO 11: · ... 6.9) . 2. ~ Ill" !6 . 0), 6. ? '" .... 2. 9) 9.3 , It( 1;' 3.3) . 0·3 8(101).6) 1?6 11(130.1} 1. J . 1 (131.8' 5.9 · 2~·23 2) -.-

" 11" ct. 3) 3. 6 1 ~(123 .. ~o. s ' !I(' 33. 7j -.6 111( 119. 1) 15.2 B( 121.1.9 ) 11. 3 11( III~ .. ) 6.1 l'(JlII.1 . Z) 5.5 · 2" ~2.; ' , . , 

10 11 • ':,1.1 . 5) 5.0 III (80 . 6) 3.9 Iii (-z . -;" ) a.7 '" (64 . 9) 8.8 8 (73 .9) S. lI 11 (85 .d) 5. ~ l' (89 . 3) J.3 · 2 79 . OJ 9.5 

11 4"7 . ) ". 6 III (53· 9) 3· 9 '" (J? . ) 9. 7 '" (lIlI.1) ~. 1 8 (51 . 5) 6. " 11 (Su .. ) . 5 11 : 511 . 9) 2.3 12 '52.5) 6.2 

5 11 (29 . 5) iI . 2 '" (32 . 5) 3·1 " 27 . ]) j . 0 .. (30 . 1) >" 8 (29.9) 9 .8 10 32. 7 ) 6.0 9 (32.]) lI . 3 ' 2 '31.3) 5.5 

" '12 · 3) 2.Z 3 (10 . 7) J. l 6 (II .S) J. l 1 ( 1 h. 0) , ( 11.0) 2. , 

":aLes 1:1 braci<e:.s are o':One ;,artial press,Jre in nanooar-s (nb ) . '13.:~s preced! ne; anc oll ~t:ig each brac~eted '/aL_e are :~e nl..o.""::':ler- of 

obse:-'lat!ons ~:- s~ason and t~~ s t andard ..!ev!'1t:on of the 5ea3onal ::;ean '/aloe , ('e3yecti·,e1i'. 

Umkeh~ obse~vations we~e made in 1985 at five stations: Boulde~ (BDR), Colo~ado, 40oN, 105°W; Mauna Loa Obse~vato~y (MLO) , Hawaii, 20oN, 156°E; Obse~vato~y Haute P~ovence (OHP) , F~ance, 44°N, 6°E; Poke~ Flat (PKF), Alaska, 

65° N, 148°W; and Pe~th (PTH) , Aust~alia, 32°S, 116°E. Table 5 shows the numbe~ of conventional and sho~t Umke~ obse~vations made at each of the 

stations . 

Ozone ve~tical dist~ibution at the five sites, de~ived f~om conventional Umke~ obse~vations, a~e plotted in fig. 7. Mean annual ozone pa~tial 

p~ess~es fo~ the va~ious Umke~ laye~s a~e indicated on the plots, togethe~ 

with standa~d deviations of the laye~ annual mean values. 

SURFACE OZONE 

At least 10 yea~s of continuous s~face ozone meas~ements have now been 

obtained at all fou~ GMCC obse~vato~ies. The ~eco~d of monthly mean su~face 

ozone values t~ough 1985 is shown in fig. 8. All meas~ements a~e ~efe~enced 

51 
• 

" 

• 

• 

1 

1 

1 

, 

\ ., \ 

"\ 

-' " ; 

, 

i / ( , 

\/ 

,\ 

; ! 

, \ " 

\\\ 

))\ 

SJAT1Qlol, IIIIWIOl om, ."8S 

10Tl'l. OZ()€, ]20. 

.. .... 005. , " 

' . 

. \ 

'\ " , 

\. '. 

~ " 

I I .;:;-/ , " ...... -

) " , 

.' /' 

so 100 I~ 200 2SO lOO 

elc)< PfVHIft. PR(SSlRCCtn'f'.lllYlSl 

SJ.I\IlOll, 8().J..DOI: 

DATE, SiJIlIS 

TOil\.. DZ()(: . 296. 

to NO. 005.1 Ii 

so 100 ISO 200 2SO lOO 

OZIN: P''1U11\. PRCSSlf!£.ltwQlMSI 

1 

1 

1 

1 

1 

5 

1 

so 

1 

51ATL()O(, 8ClJ...OOII 

01'11(, Y/as 

tOT"- OUJ<. llJ. 

\ to /CO. 085.' " 

" " ~ ~ ":. , 

lO 

~~, ,,/ / 

2S 

1/'/ [i' 20 

f I) / 1 ! 

/ 

:\~ ","/" 

1 

\ \ 

, 

\ ' , 

/ ' 

5 

, so 1 00 IS' 200 2SO 1OO 

STAlI()f, 

om, .,," """"" 

" 

TOll\. DU)£. lOO, 

\ .. ". 005. , " 

\ " ' :-';', 

... ~ ... ' 

.' .... ,-. K,. 

lO 

:,/ 

"> , 

. ./ ! 

2S 

/;, J 20 

,/'/ / 1 ,-

, 

, 

l({ 1 , , \ 

, 

)( 5 

, so 100 ISO 200 2SO lOO 

OICJC: rr"HlI\. rRtS5lRCt~1 

Figure 5.--Mean seasonal ECC-sonde ozone vertical distribution data for 

Boulder, 1985. Data are plotted for mandatory atmospheric pressure levels 

(table 4) . Dotted lines denote variability (±1 standar d deviation) . 

52 
o 

o 

\ 

i 

I , i 

; \ \ , , . 

\ : 1\ : 

I \ 

\ .... \\\ 

I

i !): \/ 

f .: 

so 

so 

100 ISO 2DO 

100 ISO 2DO 

SJAtl(lH, MILO 

CATC' \/HIes 

TOTAl. OICK, 220. 

NO. 005.' , 

JOO 

STIITlQroI, HllO 

OAIC , SU/6S 

TOTIl. OIO"<, 272. 

NO. 005. . II 

2SD JOO 

STATION. HILO 

OI\TC, es 

TOIIl. DIM, 290. 

o 

,

\ ! so 

-to HO. 005. . II 

100 ISO 200 2SD > 

OZI)-(: PAAT 1 i'll PRC5SlRt nfitJ6MSl 

. 5 

STATION. HILO 

CATt . AU/6S 

2S 

IS 

LO 

TOTAL OID<. 219. 

i O NO. 005.. 12 

5 

ljl' SO,I _-+c-7'/:2. / +._

i

'_)+_+-_l--1-1 

'r 1/" 

/0' lOOI~~4----+---4----~--~---+~ 

200~--+---~--4---~---+ __ ~~ 

o 

\ \ 

, 

\ 

j f so 100 ISO 2DO JOO 

lS 

3D 

2S 

IS 

LO 

Figure 6. --Mean seasonal ECC-sonde ozone vertical distribution data for 

for Hilo , 1985. Data are plotted for mandatory atmospheric pressure levels 

(table 4) . Dott ed lines denote data variability (±1 standard deviation). 

53 
Table 5.--Record of conventional and short Umkehr observations made at 

the automated Dobson spectrophotometer stations in 1985' 

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

BDR 15/18 4110 3/12 6/13 14/15 18/18 15/16 20/23 17/1825/24 10 /11 19/17 

MLO 45/45 19122 11 III 717 23/26 39/42 35/37 36/37 33/49 23/24 27/29 38/41 

OHP 11/12 13/17 13/11 22/28 417 012 317 23/24 30/29 15/16 20/18 17121 

PKF Oil 12/16 16/19 213 14123 516 1/6 0/4 

PTIi 40/43 32/34 32/37 25/26 17118 9/12 16/17 10/12 26/28 26/28 28/29 31/31 

'Number of Umkehr observations: conventional/short. 

to a net work standard Dasibi ozone monitor that is periodically calibrated 

against an NBS standard ozone photometer maintained at Gaithersburg , MD. 

Calibration of the network Dasibi in December 1985 showed its calibration to 

be unchanged from a previous calibration made October 1983. 

",<lLU 5,11(1.9) 

11.a<I." 18.20,6> 

4l.7<'.I) .) . ...:, . ., 

el . ...:1.u 83.z(6.71 

1~.~7.J) L21.~('.') 

11 1 .:;0: I' " 11'.3(11.9) 

54.IXI$.') 78.&l:!3.l) 

~.I(!I.:!) ,2.6(\ ' .3) IiZ.SU5,t> 

:?2 .lI' .9) 11.IK!I.D 2"3.9(1.01 ze.1K11.n 

Figure 7.--Mean 1985 ozone vertical distribution profiles obtained 

from conventional Umkehr observations at the NOAA/GMCC automated 

Dobson spectro photometer station network. 

54 

'.X'.&' 

\& •• '<1 .1) 

37.)(2.7) 

n.;J(4.l) 

IIl. (~.') 

1:.>2.1 0 5,' 

1111 . 2Ul.'5 

11_,4("",2 

, •. 9(1'.1) 
Linear regression analyses applied to the data of fig. 8 indicate longterm increases in surface ozone at BRW and MLO (table 6). At SMO, there has 

been a statistically insignificant (at the 95% confidence interval level) 

ozone decrease with time , while at SPO essentially no trend in ozone is 

observed. 

Trend estimates , including 95% confidence intervals, for the monthly 

anomalies are given in table 6 for the GMCC stations. Also given for BRW and 

MLO are trends for time periods endi ng in years other than 1985. The 

influence of large surface ozone values at these stations in late 1982 and 

early 1983 is reflected in the trend estimates. Lower surface ozone val ues at 

;;; 

~ 

< 

~ 

0 

~ ;:. 

w 

!C 

~ 

~ 

w 

~ 

.. 

:i 

~ 

... 

~ .. 

~ 

< BARROW 

• 

,. 

g 

~ 

• 

~ 

• 

~L\U:{A LOA 

• 

,. 

g 

~ 

2 

< 

" SANOA 

" 

< 

• 

• 

saunt POLE 

~ 

2 

< 

• 

n--C"--, -- --~,,~- --~,,-----~ ------,,--~-.--~--~~ 

YEAR 

Figure 8.--Recor d of monthly mean surface ozone values 

at the NOAA/GMCC baseline stations for 1973-1985 . 

55 
MLO during 1984 and 1985 have reduced the magnitude of the upward trend, 

compared with the magnitude of trend computed following 1983. The long-term 

surface ozone increase at MLO remains , however , highly significant. 

Table 6.--Trends and 95% confidence intervals for 

surface ozone anomalies at the NOAA/GMCC observatories 

Station Years Trends (% yr- l ) 

1973-1983 1. 17 ± 0.61 

BRW 1973-1984 0.76 ± 0. 61 

1973-1985 0. 78 ± 0.52 

1974-1982 1. 15 ± 0. 81 

MLO 1974-1983 1. 74 ± 0.71 

1974-1984 1.37 ± 0.61 

1974 -1985 1. 20 ± 0. 52 

SMO 1976-1985 -0. 70 ± 0. 80 

SPO 1975-1985 -0.05 ± 0. 32 

STRATOSPHERIC \-lATER VAPOR 

Stratospheric water vapor profiles from balloonborne frost-point 

hygrometers were obtained during 1985 in Boulder , CO; Palestine , TX; and 

Fairbanks, AK. Plots of the water vapor mass mixing ratios of the 

stratospheric portions of the soundings are shown i n fig . 9 . The six soundings made in Boulder were part of an ongoing program begun 

in 1981 to monitor the water vapor content of the stratosphere over Boulder. 

The two soundings made at Palestine concluded a series of correlative 

measurements begun in 1983 to test the concept of long-term, satellite-based 

monitoring of trace gases in the stratosphere using a multidetector infrared 

spectrometer and a solar occultation technique. The solar occultation 

experiment , involving balloonborne instrumentation , was designed by 

NOAA/NESDIS . The measurements at Fairbanks were part of a continuing series 

of soundings made to validate water vapor profiles obtained from the SAGE II 

instrumentation carried on board the Earth Radiation Budget satellite. 

A NOAA Data Report (Oltmans , 1986) presents tabular and graphical 

stratospheric water vapor data from Washington, DC ; Boulder, CO ; Palestine , TX; Laramie , WY ; and Fairbanks , AK . The data for Washington , DC from 1974-

1980 represent the completion of the sounding program conducted by personnel 

of the Naval Research Laboratory, Washington , DC at that location . The data 

from Boulder for 1981-1985 are from the monthly sounding program that began in 

1981. Profiles from Palestine, Laramie , and Fairbanks are from vari ous 

intercomparison programs conducted during 1981 - 1985 . 

56 
0 

5-

2 0 

'F 

.. 

.0 

§ 4 

.s 

~ 6 

'" i!! '"B 

0 

0 

0 

rrf--

f--

OC- Cl. 

10 

= 

150 = 

2 

, 4 6 BOULDER , CO 

,I "'" 1 MAY 18 MAY 31 ocr 20NCN 

85 85 85 85 85 

II 

\ \ 

19 DEC 

85 

, 

PALESTINE TX FAIRBANKS ,AK 

5 JUL 5 JUL 7 AUG 9 AUG 9 AUG 30 

85 85 85 85 

/ / 

'-- I? "7 

< 

85-

- 2 B 

-

2 6 -

- 2 4" - .!J 

2 2 ~ 

.2 O;g. -

-2 

, 

- , 

-

- , 

E 

8 .~ 

I 

6 

4 

"- ! \ ......... ) -"-- ~ II -, 200 - 012222222424222 

Mass Mixing Ralio (ppmm) 

2 

'!- , ~ 

Figure 9.--Profiles of stratospheric water vapor mass mlxlng ratio (ppm) for 

1985 at Boulder , CO; Palestine, TX; and Fairbanks, AK. Numbers along the top 

of the plot for the first wat er vapor profile are volume mixing ratios in ppm. 

HALOCARBONS AND NITROUS OXIDE 

Two new people were employed in 1985 : A group leader , with specific 

expertise in calibration gas preparation, dissolved gas measurements , and 

infrared spectroscopy , who will arrive i n 1986 ; and a CIRES employee, who 

began work in Mayas operations manager for field measurements . 

Air samples continued to be collected weekly at BRW , NWR , MLO, and SMO , 

and weekly in January , November , and December only at SPO. These samples were 

returned to Boulder where CCl,F (halocarbon F-11), CC1 2F2 (F-12) , and N20 

concentrations were determinea by an EC-OC. 

Our calibration standards for F-11 and F-12 were tied to the OOC scale . 

N20 calibration standards were made at GMCC in Boulder and based on diluting a 

precisely known mixture of N20 in CO2 into a CO2- and N20-free air mixture , 

measuring the CO2 concentration , and thereby yielding the N20 concentration . Cylinder 3072, which has been used exclusively as the source of calibration 

gas for sample analyses since 1977 in Boulder , was replaced by cylinder 3088 

on 20 September because of low pressure. The SPO gas chromatograph was 

operated twice a week , analyzing air for F-11 , F-1 2, and N20 concentrations . 

Calibration gas came from cylinder 3083 . Calibration standards wi ll be 

produced by gravimetric techniques in the future . 

Work on the RITS Project began with the design of an automated gas 

chromatograph and data processing system to measure the in situ air 

concentrations of N20, F-12 , F-11 , CH3CCl 3, and CCl4 at the baseline 

stations. Hardware and software were subsequently purchased, modified, and 

57 
tested. Installation of the system will begin in 1986 at SMO , BRW , and MLO. 

The system consists of a Hewlett-Packard Model 5890 EC-GC , a Nelson Analytical 

interface box , an HP9816 computer \-lith Thinkjet printer, and an HP9133 hard 

disk and floppy drive. 

Selected N20, F-12, and F-11 data from BRl-I , NWR, MLO , SMO, and SPO are 

shown in figs. 10, 11, and 12 for the period 1977-1985. The data from 

September 1984 through February 1985 have been excluded from the record 

because of problems with the detector's response. Least-squares regressions 

using a quadratic model fit to the data are represented by the solid lines in 

the figures. Estimated growth rates and associated standard deviations are 

also shown. 

N20 data have been corrected to account for the influence of CO2 on the 

gas chromatographic analyses of air when it co-elutes with N20. Increasing 

levels of CO2 in the atmosphere have enhanced our EC-GC 's response to N20 by 

approximately 0.2 ppb per ppm of CO2 over the CO2 range of 315-355 ppm. 

Yearly means and standard deviations for the three constituents at the 

five stations are shown in Table 7. Years where data are missing have means 

estimated by the regression equation at midyear . The N20 data record ~~ows no 

significant (95%) change in the average rate of increase (0. 64 ppbv yr ) for 

the 9 years for any of the stations . The rate of increase at SMO is 

increasing more rapidly than at other GMCC stations. The F-12 data likewise 

increase at a constant rate. However, in the Southern Hemisphere , F-12 

concentrations are increasing 9% faster than in the Northern Hemisphere . All 

the stations except SPO show a significantly (99% confidence level) decreased 

rate of F-11 growth. The rate of growth of F-11 at SPO is also decreasing , 

but the large scatter in the data make it less significant (83% confidence 

level). Southern Hemispheric F-11 concentrations are growing 5% faster than 

at Northern Hemisphere sites. This is probably due to inter-hemispheric 

exchange rates being higher than Northern Hemisphere source rates. 

Table 7. --Mean annual concentrations' of N20 and halocarbons F-11 and F-12 

1977 1978 1979 1980 1981 1982 1983 1984 1985 

~ (ppbv) 

BRW 301 .8 301.5:1:0 . 2 301 .9,0. 2 301 .6, 0 . 3 302 .8, 0 .2 303.4,0.1 303.3,0 .2 30~ 4 304 .9 

,\Ill 300 .5 301.1,0.3 301 .9, 0 .2 303 . 3,0.3 303 .3,0 .2 304 . 6:1:0 .2 305 . 2.10 .2 305 .8 306 .2 

MLO 300.8 300.2tO.3 301 .5,0. 2 302.0,0 . 3 302 .8,0 . 3 303 .8,0 .2 30) .8,0.2 305.3 306 .0 

So'1O )02.0 302.6:1:0.3 301l .1.tO. 2 30'.5,0.) )05 .5,0.3 307.110.2 301.4,0 .2 308 .8 309 .5 

spo 299.' 300 . 1 300 .8 301 . 4 )02 .0 302.5 302 . 9 303 . 3 303 .7 

F-12 (pptv) 

BRW 263.7 281 . 1tl . 5 295 . 3,0. 9 310 . 811. 2 329 .9,1. 5 345 .211 .0 360 . 2:1:1.2 375 .5 390 .7 

mrn 263 .3 281l . 7±:2 .6 295 .5±1.0 306 . 011 .0 322 . 1 ±1 . 1 339.6:t1 .0 357 . 1:1: 1.1 369.4 384.5 

MLO 261.9 278 . 1I:!:.1 . 1 293 . 1±1 .1J 305 . 9: 1.2 324 .8,1. 4 336.',0.8 350 .6,1 .3 367 .0 381 .7 

SMO 239.3 259.6,0.8 273 . 8:t0.6 286 .6:1:0.7 308 .0,' . 1 325 . 3,0.6 3113 . 8:!:1 .2 358 .0 374.3 sPo 230.3 250.1 269 . 1 287 .2 30' . 6 321 .3 331.1 352.1 366 . 4 

F-l1 (p ptv ) 

BRW 154.1 165.0tO.7 113 .9,0 .6 183.8,0.5 19).5,0 .7 201.B±0.5 212 . 1 iO . 7 219.4 227.4 

""R 151 . 1 162.311.0 169 .0,0. 7 180 . 1:0 .7 188. 1,0.5 197.8:t0.7 208 .4,0 .6 215.2 223.7 

MLO 145.1 156.310 . 6 166 . 7tO . 7 117 .110.6 186.0,0. 5 193 .8,0.5 205 . 0.10 .7 212 . 6 220 . 5 

So'O 135.7 148 .2±0 .6 158 .3±O.5 167 1t.O ~ 118 . 1±0 .1 188 . 4:t0 . 1I 198 .1 :to .6 205 .' 213 . 1 

spo 139.1 150 . 1 160.7 171 .0 180.8 190 .3 199 . 3 208.0 216 .3 

·Values '.Iithout standard deviations '.Iere calculated at midyear from the least-squares quadratic regression fits 

to the data. 

58 
U1 

'-D 

320 

3 10 ~ BRIv .. ... J ~~~ f ';-" 04~ ±0;03 fPB~ Y1 280 -

': .. -.: 

320 .--'---.--'---r--.---r--'--.--~ 

310 NWR . . _" . . 

300 ., .:; • ':: ~. ..... . -

290 0.68 ±0.04 PPBV/ YR 

280 

~20 r--r--,--.r--r--,--,---r--,--, 

& 00 310 Mill . ' . • _:,. . ..... 'M 

OJOO • ,'v">: ." • " . • 

2290 0.66 ±0.04 PPBV/ YR 

Z280 ' 

320 

310 SMa ........ 300 ,. : .••... 

290 0.92 10.04 PPBV YR 

280 _L-__ L ........; 

ill '~o , .. ~;; ,:;;"v 1 

280 ' , I l-

?7 78 79 80 81 82 83 84 85 

Figu~e 10 .--Selected N20 data 

~eco~d, and estimated growth ~ates 

and associated standa~d deviations . 

N~, f\ .~~-. 

320 

270~ 220 

15.14 ±0.18 PPTV/ YR 

~~ . 

~ t = Mill .,- "J' ~320 

~270 14.96 ±0 15 PPTV Y 

U 220 ' , 

U

420 

370 SMa . ~ , '~ . 

320 ~ 

270 16.85 ±O.IO PPTV/ Y 220 l.-L.l.JJll 

·120 [ -'- T 370 spa 

320 

270 " .... '."':';' 

??O -"i' J 

77 78 79 

T , T --, 

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

.... 

.1. 

~ 

. .:.a,. 

16.76 

" 

I 

10.

j 

32 PPTV ,J 80 8\ 82 83 84 85 

Figu~e 11 .--Selected CC1 2F2 (haloca~bon F-12) data ~eco~d, and estimated g~owth ~ates and associated 

standa~d deviations . 

260 f I 

BRI\" ........ 

1 

225~ ~!oo: • 

190 l 

155l ~ 9. 12 ; 0.07 1'1''1'\' l ' I! _I 

'-1 

\ I~ 120 .I 

260 r I 

225 190 f _ NII"R ' , 1 

155 :#.~'.I->K.""·-~~ ... ~ ~ b120 lin J [ :-J08 j 

200 

f I ' . I 10;08 I,'!>'I'\' YI 

15: 22 ~ " ~ MI.O j • I , , 

0..

'90 

~ , 1 

u ]155 l ~ -.. ~.. . " ... P 

- -"'" ~ -~. . , .,..,...j . 1 

U 120 L I () I I I' . ·10 t 0.07 1'1'"1'\ • I \Ij 

260 

,,,0 f "'1(') ..... ,) r ' -''!\-

HJO r' I:):) . . ~.-.-~ I:!O tf ~ 

~ 'J.G7 10.07 1'1''1'\ 

:"!(jO r ' 

sl'O :.!:"::) :- ' 

~)() ~ 

1:6 ~ :, , \ :..!(} t:. 

77 

I I 

.:.c . . .IJ"'"'' ~ .: 

... ,',' ~ 9,(; 1 . o.:m 1'1''1'\ 

78 79 80 81 B:.! In 8·1 

1 

-1 

\ ~ 

1 

~ 

\1< 

J 

H"") 

Figu~e 12.--Selected CC1 3F (haloca~bon F-ll ) data ~eco~d, and estimated g~owth ~ates and associated standa~d deviations. 
5.2 References 

Farman, J. C., B. G. Gardiner , and J. D. Shaklin, 1985. Large losses of total 

ozone in Antarctica reveal seasonal CIOx/NOx interaction. Nature 315 :207-

210. 

Grass , R. D. , and W. D. Komhyr , 1985. Traveling standard lamp calibration 

checks on Dobson ozone spectrophotometers during 1981-83. In 

Atmospheric Ozone, Proceedings of the Quadriennial Ozone Symposium. 

Halkidiki, Greece, 3-7 September 1984 , D. Reidel, Dordrecht, Holland, 376-

380. 

Harris, J. M. , 1982 . The GMCC trajectory program. NOAA Tech. Memo ERL ARL11 6, NOAA Environmental Research Laboratories, Boulder , CO, 30 pp. 

Hasebe, F., 1980. A global analysis of the fluctuation of total ozone : II , Non-stati onary annual oscillation , quasi-biennial oscillation, and longterm variations in total ozone . Journal of the Meteorological Society of 

Japan 58:104-117. --

Hasebe , F., 1983. Interannual variations of global total ozone revealed from 

Nimbus 4 BW and ground-based observations. Journal of GeoP1ysical 

Research 88:6819-6834. 

Komhyr, W. D., 1969. Electrochemical concentration cells for gas analysis. 

Annales de Ge0P1ysique 25(1):203-219 . 

Komhyr, W. D., R. D. Grass, R. D. Evans, R. K. Leonard , and G. H. Semeniuk, 

1985 . Umkehr observations wi th autanated Dobson spectrophotaneters. In 

Atmospheric Ozone , Proceedings of the Quadrennial Ozone Symposium held in 

Halkidiki, Greece, 3-7 September 1984. D. Reidel, Dordrecht, Holland, 

371-375. 

Komhyr, W. D., R. D. Grass, and R. K. Leonard , 1986. Total ozone decrease at 

South Pole, Antarctica , 1964-1985. Geophysical Research Letters (in 

press) . 

Komhyr, W. D. , R. D. Grass, J. M. Harris, and R. K. Leonard, 1986b. A South 

Pole, Antarctica, ozone high. GeoP1ysical Research Letters (in press). 

Oltmans, S. J., 1986. Water vapor profiles for Washington, DC; Palestine, TX; 

Laramie, WY; and Fairbanks, AK during the period 1974 to 1985. NOAA Data 

Report ERL ARL-7, NOAA Environmental Research Laboratories, Boulder, CO , 360 pp. 

Solomon, S. , R. R. Garcia , F. S. Rowland, and D. J. Wuebbles, 1985. On the 

depletion of Antarctica ozone . Nature 321 :755-758. 

60 
6. ACQUISITION AND DATA MANAGEMENT GROUP 

6. 1 Continuing P~og~ams 

STATION CLIMATOLOGY 

Int~oduction 

The inte~p~etation of meas~ed values of ae~osols , t~ace gases, and tu~bidity ~equi~es the measu~ement of ancilla~y meteo~ological va~iables to 

assess the influence of local pollution sou~ces. These va~iables include wind di~ection , wind speed, station p~ess~e, ai~ and dewpoint tempe~at~e , and a dete~mination of bounda~y laye~ stability. The main c~ite~ion used in 

selecting the senso~s was ~uggedness , conside~ing the st~ess of the pola~ 

envi~onment at two of the stations . Whe~e app~op~iate , comme~cially available inst~umentation was chosen and WMO-~ecommended expos~e standa~ds we~e 

followed. A complete list of the senso~s , model numbe~s, and the heights appea~ in Nicke~son (1986) . 

With the installation of CAMS units at all stations d~ing the latte~ 

half of 1984 , downtime of t~e data acquisition activity was significantly ~educed. As a ~esult of the new daily ~outine of p~inting hou~ly ave~ages and 

compa~ing them with obse~ved conditions, the quality of the data imp~oved as 

well. The p~intout known as the daily weathe~ ~epo~t was used fo~ this 

p~pose. It contains hou~ly ave~age values fo~ the wind meas~ed at app~oximately 12 m height , ai~ and dewpoint tempe~atu~e measu~ed at 2 m, ai~ 

tempe~atu~e meas~ed at about 12 m, and station p~ess~e. The ~epo~ts a~e 

sent to Boulde~, checked , and sto~ed on mic~ofiche fo~ futu~e ~efe~ence. The 

nume~ical values, f~om which tables 1-4 a~e gene~ated , a~e also sto~ed on 

tape. 

Ba~~ow 

A desc~iption of the Ba~~ow site, its s~~oundings , and climate can be 

found in p~evious GMCC Summa~y Repo~ts e.g., (DeLuisi, 1981). Wind ~oses of 

the hou~ly ave~age ~esultant wind di~ection and speed a~e p~esented in 16 di~ection classes and 4 speed classes. The dist~ibution of the wind by 

di~ection fo~ 1985 is quite consistent with the ave~age fo~ the 1977 th~ough 

1984 pe~iod (fig. 1) . The p~edominant wind di~ection is again f~om the II ~ep~esentati ve sampling secto~, II NE-SE , and all othe~ di~ections a~e less 

than 5%. This was not the case in 1984 when an unusually large pe~centage of 

southweste~lies we~e obse~ved (Nicke~son , 1986). _The 1985 wind ~ose contains 

15 . 5% of the wind equal to o~ g~eate~ than 10 m s as cont~asted to 9% fo~ 

the long-te~m ave~age. New maximum wind speeds we~e obse~ved fo~ the months 

of Ma~ch and July (table 1). The month-to-month changes in p~evailing wind di~ection a~e significant. In 1985 , easte~lies (NE-SE) , gene~ally conside~ed 

to be the p~efe~~ed di~ection fo~ baseline ai~ sampling , occu~~ed in excess of 

92% of the time in Janua~y as cont~asted to only 31% in Feb~ua~y . These pe~centages a~e the monthly maximum and mini mum fo~ the yea~ . The long-tenn ave~age pe~centage of easte~ly winds is 61% ; they occu~~ed 59% of the time in 

1985. 

61 
BARRO ..... 

1985 

IV 

• ,NO SP£ED(W S) 

_..5$ ~ 

~$$ U) 

o S~ O 

N WIND ROSE 

• 

s 1I'ISD rMIl;! 

BARROW 

77 - 84 

IV 

WIND SP£t:D(1I 5) 

:;$ S<~ 

czz:::I ~~n IO 

o · SlIO 

N 

s 

W[No ROSE 

liND FRIlQ 

, 

Figure 1. --Wind rose of surface winds for BRW for 1985 (left) and 1977-1984 

(right) . The distribution of the resultant wind direction and speed are in 

units of percent occurrence for the year and 8-yr period . respectively . Wind 

speed is displayed as a function of direction in three speed classes. 

Table 1 . --BRW 1985 monthly climate summary* 

Jan Feb fur 'pr I"ay Jun Jul 'ug Sep Oct Nov Dec 1985 

Prevailing .... ind ENE ;'(S fi ENE "E E EtjE ENE E E 11',./ ESE EtlE ENE 

direction 

Average '.,ti:ld 

speed {m 3- 1} 

9. 2 5.9 6.0 6. 6 5. 9 6. 1 6.0 6.6 7 .0 7.5 7 . 5 7.5 6.8 

I-':ax imum .... ind 

speedf (m $-1) 

I. '" 22 15 13 '" 15 13 18 16 20 19 22 

Direction 0 :- max. 55 280 105 75 115 260 250 105 285 265 115 65 105 

windt (deg . ) 

Average station 1017 . 2 1021 . 2 1009 . 4 1020. 3 1011 .7 1014.6 1016.2 1012 . 4 1008 .5 1010 .8 1020 . 1 1017.1 10111 . 9 

pressure (mb) 

Maximum pressuret 1031 10110 1028 1035 1030 1027 1029 102u 1031 1029 1037 1042 1042 

(mb) 

Minimum pressuret 993 998 985 1003 995 997 996 998 99' 98' 982 99' 982 

(mb) 

Average air -22 . 2 -28 . 0 -26.0 - 23 . 1 -6.B -0 . 7 2· 3 -2.9 -2 .0 -12 . 11 -16.8 -22 · 3 -12 . 6 

temperature (Ge) 

Maximum temperaturet -11 -7 -16 -12 -, 7 12 20 5 0 -6 20 

(Oe) 

Minimum tempera turet - 35 -'3 - 36 -33 -20 -3 -2 -. -1 7 -26 - 32 -39 -'3 

(Oe) 

Average dew point -5.5 -15 .0 -19.7 -25.5 

temperature ( Oe) 

Maximum dew pointt 2 -, -1 0 

temperature (OC) 

Minimum dew pointt -35 -20 -29 -36 -" temperature (OC) 

'Instrument heights: wind , 17 mi pressure, 9 . 5 m (HSL) . air and dewpoint temperature. 3 m. Wind and temperature 

instruments are on a tower located 25 m oortheast or the main bullding. 

t~4ximum and minimum values are hOurly averages. 

62 
Following the unusually cold winter and spring of 1984, with monthly 

average temperatures as much as 11°C below normal, 1985 pressure and 

temperatures were generally close to normal. The average pressure for the 

year was 1.6 mb above the average for the previous 8 years. The average 

temperature was only O. 1°C cooler than normal. All frost-point measurements 

were converted to dewpoint. The hygrometer failed in mid-January and was not 

returned to service until mid-September. 

Mauna Loa 

A description of the MLO site and its general climatology can be found in 

previous GMCC Summary Reports. The MLO 1985 monthly climate summary is shown 

in table 2. Keep in mind that for most variables, the average values are not 

representative of median values because of the bimodal distribution of the 

wind direction based on the time of day. The effect of the Mauna Loa volcano 

is to redirect stronger, predominantly easterly or westerly winds aloft, down 

the slope with a more southerly component. The winds were again predominantly 

from the south in 1985 as in earlier years (fig . 2). A typical number of 

spring storms was reported in February and March, but the number of storms and 

days with above-normal winds speeds in November was unusual. The maximum wind 

speed and the minimum pressure observed in November set new records for that 

month. The pressure is also a new low pressure for MLO for the period 1977 to 

present. The average pressure for 1985 was 1.3 mb below the 8-yr average for 

the period 1977-1984. Furthermore, the individual monthly averages were all 

below the comparable monthly averages for this period. Although there were a 

large number of storms at MLO in 1985 (precipitation amounts of 463 mm, i.e., 

2.5 times that in 1984, were reported), it is difficult to believe this 

pattern would last 

MAUNA LOA 

1985 

[w 

.I>;D SPEF.Il(W S) 

~S ~ 

c.:::::J~~ IO 

o I S ~ 10 

N Wl:-:D ROSE 

I 

s " I \ D FlUXI 

\I ,\U ~A [.OA 

?7 84 

w 

wr>; D SPE:EO(W S) 

_ !\S I S < !I 

c:::::zJ !> , I S < 10 

==:J 'IS ~ 10 s 

~ 

WI ND ROSE 

.ISD flUX! 

, 

Figure 2.--Wind rose of surface winds for MLO for 1985 (left) and 1977-1984 

(right) . The distribution of the resultant wind direction and speed are in 

units of percent occurrence for the year and 8-yr period, respectively. Wind 

speed is displayed as a function of direction in three speed classes. 

63 
Table 2. --MLO 1985 monthly climate surrunary* 

Jan reb "ar Apr May Jun Jul AUS Sep Oct Nov Dec 1~85 

Prevailing wind SW SE SE SW SSW SE SE SE SE SE SSW SW SE 

direction 

Average wind 

speed (ms-' ) 

5.6 5.5 5. 9 4.8 5.1 3. 9 4. 6 4.6 5.1 3. 8 5. 5 5 . 1 5.0 

Maximllll .... ind 

speedf (ms-') 

21 17 16 14 15 12 13 12 13 13 20 14 21 

Direction of max . 215 190 140 230 1)0 140 130 130 220 135 190 220 215 windt (deg.) 

Average station 679.1 678.1 678 . 6 679 . 0 679 . 7 680.6 680.9 681.0 680.0 680.) 678 .2 679 . 6 679.6 

pres5ure (mb) 

Maximum pressuret 683 682 683 68) 684 683 68) 685 683 684 682 683 685 

(mb) 

Hiniml..l!l pressuret 671 674 674 674 674 678 679 679 676 675 668 673 668 

(mt» 

Average air 5.6 4.1 3. 2 4.3 6.1 8.2 B,Il 8.1 7.9 7. 7 6. 6 6 . 0 6.4 

temperature (Ge) 

Haxim1.lTl temperaturet 14 16 14 12 15 16 19 18 16 14 14 13 19 

( DC) 

HinimLJ'll temperaturet -) -2 -3 -) -1 0 2 -) -3 -3 

( DC) 

Average dewpo int -111.11 -6.1 -10.1 -6 . 5 -8 .0 -8 . 6 -5 .8 -4.6 -5 . 3 - 11.2 -8 . 6 

temperature (DC) 

Maximum dewpointt 7 5 5 6 7 8 8 9 9 6 9 

temperature (DC) 

Hinimun dewpolntt -29 -27 -37 -29 -31 -29 -24 -25 -26 -)2 -)7 

temperature ( DC) 

Preclpl tation (rrrn) 14 125 140 15 32 2 20 39 3 22 46 5 46) 

IInstrument heIghts: wind, 17 m; pressure. 3399 m (I-'SL ) ; air and deo,.polnt temperature, 3 m. Wind and temperature 

instruments are on a tower located 25 m northeast of the main building . 

tMaximum and minimum values are hourly averages . 

for 12 months . The other explanation is a measurement error. The pressure 

sensor is checked against the mercu~ial barometer at the station twice weekly 

and the two are in good agreement . Thus, a recheck of the me~curial barometer 

is necessary befo~e this difference can be resolved. Both ai~ and dewpoint tempe~atures were within normal ranges for the year . 

Samoa 

A comparison of the wind rose for 1985 to that for the preceding 8 years 

shows a very similar distribution except for the shift in the predominant wind 

dir~9tion to SSW and the higher percentage of wind equal to or greater than 10 

m s (fig. 3). This is a ma~ked change from 1984 when the distribution 

contained a higher percentage of winds from the northwest. Whereas the longterm a~T~age occurrence of wind speeds in the class greater than or equal to 

10 m s is 3% , it was about 8% in 1985. The average wind speed for the year 

is 5.8 m s-1, which is 1.4 m s-1 above the long-term average . Table 3 shows 

that new maximum wind speeds were observed for the months of January , May , and 

September. In January, wind speeds of 10 m s-1 o~ greater were reported 12% 

of the time as compared with a normal of less than 1%. Early in the year , the 

stronger winds were northerly ; later, southeasterly. In February the st ation 

staff reported the clearing of underbrush on the southeast slope of Lauagae 

Ridge , upwind of the sampling tower . This contributed to the increase in 

occurrence of stronger wind speeds in the trade wind direction . A discussion 

of the topography and climate of Cape Matatula, Samoa, can be found in 

previous GMCC Summary Reports. For example , the September occurrence of wind 

speeds in the ~10 m s-1 class was 17% compared with a normal occurrence of 

only 1% . The winds were from ESE-SSE 78% of the month. 

64 
SAMOA 

1985 

w 

WIND sPEEIl(lII / Sl 

_~ .S <~ 

m:z::I 5 ~ WS < 10 

c:::::J U ~ 10 

N 

s 

WI NO ROSE: 

tlSO rR~ 

, 

E 

SA MOA 

77 - 84 

w 

WI NO SPEEil(W/ S) 

_5~.S 5 

~5S .S IO 

o _ 8 ~ LO 

N 

s 

WIND ROSE: 

WISD rRfJQ 

, 

E 

Figu~e 3.--Wind ~oses of surface wind fo~ SMO fo~ 1985 (left) and 1977-1984 

(~ight). The dist~ibution of the ~esultant wind di~ection and speed a~e in 

units of pe~cent occu~~e ce fo~ the yea~ and 8-y~ pe~iod, ~espectively. Wind 

speed is displayed as a function of di~ection in t~ee speed classes. 

Table 3.--SMO 1985 monthly climate summa~y* 

Jan feb "oar Apr May Jun Jul Aug Sep Oct Nov Dec 1985 

Prevailing wind NW SE N SSE SSE SSE SSE SSE SSE SSE SSE NW SSE 

direction 

Average wind 

speed (m 5- 1) 

4.9 5.2 5.3 4.9 5.7 5.9 7.0 8. 3 7.6 6.1 5.4 3.5 5.8 

Haximtml wind 

speedt (m 5-') 

16 12 13 13 16 13 13 18 13 12 10 9 18 

Direction of max. 335 350 5 155 155 150 110 160 150 120 160 100 160 

windt (deg.) 

Average station 998 . 9 999.5 999.0 1000 . 11 999 . 9 1001.6 1002.7 1003.0 1002.5 1001.11 999.4 998.9 1000.6 

pressure (mb) 

Haximllll pressuret 004 1003 1004 1003 1005 1006 1006 1007 1006 1006 1004 1003 1007 

(mb) 

Minimum pressuret 995 995 993 997 996 995 998 999 999 995 995 995 993 

(mb) 

Average air 27 . 0 21.2 28.0 27 . 2 26.8 26 .11 26 . 1 26.2 25.9 26 .6 26 . 6 27 .8 26.8 

temperature (Oe) 

Haximllll temperaturet 31 31 31 30 30 29 30 30 29 30 30 32 32 

( Ge) 

Minimum temperaturet 23 23 25 24 23 23 " 23 23 24 23 23 23 

(Oc) 

Average dewpolnt 25.8 26. 1 25. 9 26. 9 26 . 2 

temperature (fie) 

MaximllJl dewpointt 28 30 29 31 31 

temperature ("e) 

Miniml.J1l dewpolntt 24 23 22 21 21 

temperature ("e) 

Precipitation (mm) 355 211 89 246 210 207 78 147 347 140 105 2135 

*lnstrument heights: wind , 1~ mj pressure , 30 m (MSL) ; air and dewpoint temperature, 9 m. "Hnd and temperature 

sef150rs located atop Lauagae Ridge, a distance 110 m northeast of the station. Pressure sensors are located in the station. 

W.axlmun and mlnlmun values are hourly averages. 

65 
The remainder of the meteorological variables measured in 1985 were 

reasonably close to seasonal and annual norms (table 3). The station pressure 

of 1000.6 mb was only 0.3 mb above the long-term average . The average air 

temperature, measured at a height of 9 m above the level section on the east 

end of Lauagae Ridge, was 26 . 8°C, just 0. 2°C below normal. In the case of 

both pressure and temperature, the extreme values are within normal limits. 

Early in 1985 the dewpoint hygrometer was returned to the manufacturer for 

repair and recalibration. It was returned and installed in September. The 

average monthly precipitation for the year of 194 mm is only 19 mm below 

normal. 

South Pole 

The most distinguishing feature of the distribution of the surface wind 

directions at the South Pole station is the large percentage (80%) (wind flow 

from the NE quadrant (N-E). As shown in fig. 4, the distribution of surface 

wind with direction is very Similar to the distribution for the preceding 8 

years. The main difference in 1985 is that the predominant wind direction was 

grid northerly. For five of the months, the prevailing wind direction was 

also northerly (table 4). A second feature of the 1985 wind rose is the 

relati~rly large number of occurrences of wind speeds equal to or greater than 

10 m s : 8% as compared with 3% in the pr~ceding 8 years. N~netheless, the 

average wind speed for the year of 5.9 m s 1 was only 0. 6 m s 1 greater than 

the long- term average. New maximum wind speeds were observed for the months 

of February, June July, and August. The strongest winds were observed on 25 

July at 17.2 m s-1 in association with a storm that established a new record 

low station pressure of 641 mb at the GMCC facility. The previous low 

pressure was 643 mb. Two hours earlier a new record high temperature for July 

,------

SOUTH POLE 

1985 

IV 

. 1100 0 SPUD(W 5) 

)~ $ 

czm$~ IO 

o 'IS ~ 10 S 

• 

~ 

.. 

WI ND ROSE 

EI 

.. J . 11'0 f'IIDQ 

, 

SOUTH POLE 

77 84 

IV 

.1 SO SPUD(W S) 

_ :; "",S < $ 

c::::::IS' . S< IO 

o WSillO 

N 

s 

• 

.. 

WIND ROSE I 

'1ISD rR~ 

, 

E 

Figure 4.--Wind roses of the surface wind for SPO for 1985 (left) and 1974-

1984 (right). The distribution of the resultant wind direction and speed are 

in units of percent occurrence for the year and 8-year period, respectively. 

Wind speed is displayed as a function of direction in three speed classes . 

66 
Table 4.--SPO 1985 monthly climate summary* 

Jan Feb Mar Apr Kay JI.01 Jul Aug 50p Oct Nov Dec 19B5 

Prevailing wind NNE N E lINE E N NNE N NNE N E N N 

direction 

Average wind '.3 5.0 5.5 6.5 6.3 7.7 7.3 6.2 6.5 6.9 ' . 7 ' . 1 5.9 

speed (m 5-') 

HaxlmlZll wind 9 " 12 13 13 " 17 17 " 16 11 8 17 

speedt (m 5-') 

Direction of max. 20 15 5 15 10 350 5 300 360 15 285 360 5 

windt (deg. ) 

Average station 692 .2 681.5 682 .0 683.2 679 .6 680 .' 662 .7 677 .8 672 . 5 6111.9 673.2 682 .5 678.5 

pr essure (mb) 

l".ax lm\..ll1 pressure t 699 69' 693 699 691 696 67' 69' 689 692 683 69' 699 

(rr,b) 

Mi nimum pressuret 68' 670 67' 669 661; 659 6" 66' 660 655 663 677 6" 

(mb) 

Average air -27 . 6 -'3.2 -53.6 -55.8 -59 . 1J -53 .0 -60 . 3 -57.8 -60 . 1 -50 .5 -39 .0 -29 . 3 -'9.2 

t empe rature (OC) 

Maximum temperaturet -19 -28 -32 -36 -'0 -35 -3' -35 -39 -33 -30 -22 -19 

( OC) 

Min imum temperaturet -33 -52 -66 -72 -76 -70 -76 -75 -71J -67 -'6 -36 -76 

( OC) 

*Instrument heights: wind, 12 mj pressure , 2841 m (MSL ) : air temperature , 2 m. The anemcxneter and thermaneter are 

located on a tower 100 m grId ESE of CAL Pressure measurements are made insl de CAt. 

tMaximl.lll and mlnImllll values are hourl y averages. 

was set at -34.1°C. The ave~age p~essu~e fo~ the yea~ was 678.5 mb, which is 

0.9 mb above the ng-te~ ave~age. The average tempe~at~e fo~ the yea~ was 

-49.2°C, less than 1°C above the climatological ave~age. The -53°C ave~age 

for June made it one of the wa~mest on ~e co d and a -35°C maxi mum was 3°C 

above the previous maximum. Because of a series of equipment problems, no 

reliable f~ost-point meas~ements we~e made in 1985. 

DATA MANAGEMENT 

Between August and Novembe~ 1984, CAMS units we~e installed at each of 

the GMCC stations , eplaci ng the aging ICDAS. Details of this changeover can 

be found in Summa~y Repc~t No. 13 (Nicke~son, 1986). Most of the difficulties 

encounte~ed with the hardware were ~esolved by the end of the yea~. The one 

persistent p~oblem was the batte~y backup to the CAMS memo~y. As a ~ule, the 

charging ci~cuit did not ope~ate p~operly, causing the boards to fail. By the 

end of the year , the memory at two stations had been replaced with ZRAM, which 

does not use batte~ies. The remainder we~e changed early in 1986. This is 

the only significant hardware change that has been requi~ed to date. The CAMS 

that operates the CO2 analyze~ is described in Herbe~t et al. (1986). 

Table 5 gives the number of ho~s each CAMS was inope~ative in 1985. A 

total of 926 hours of downtime was ~epc~ted, slightly over 1% of the CPU ho~s 

in the yea~ . By compa~ison, the fo~ ICDAS units in continuous operation 

averaged 1556 hours of downtime pe~ yea~ between 1980 and 1984. Of significance is the ve~y low number of hours of downtime at Samoa and the relatively 

67 
large number at the South Pole. This comparison points out the importance of 

having a reliable power system. The majority of downtime is caused by power 

outages or brownouts. The CAMS units in Samoa use power from the solarpowered uninterruptible power supply . At SPO , the number of power failures 

and brownouts has increased dramatically in the past few years. Although the 

average number of hours of downtime in the worst case was 83 hours at SPO , this is considerably less than the average reported for ICDAS for a comparable 

period . 

Table 5. --GMCC CAMS downtime* for 1985 (h) 

Program BRW MLO SMO SPO Total 

ASR 145 112 21 101 379 

CO2 34 65 6 1 31 236 

M03 25 83 65 138 311 

Total 204 360 92 370 926 

*Downtime is the number of hours in the year for which the data tally 

indicates less than 80% of the expected number of data points for that hour. 

6.2 Special Projects 

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; Nickerson, 1986, pp. 71-75). This section describes new development of 

the trajectory programs that permitted trajectory computation over the 

southern polar regions and a case study of seasalt transport to SPO . 

Table 6 lists most of the trajectories computed during 1985. These were 

provided for atmospheric researchers within GMCC and ARL as well as scientists 

at numerous universities and research institutes of foreign governments 

affiliated with GMCC. 

Input data for the Northern Hemisphere model (65 x 65 grids) consist of 

E-W and N-S wind components from 1975 to the present. Data for the global 

model (2.5° grid) begin 2 years later in 1977 and extend until the present. 

Beginning in January 1986, access to the input data will be improved. Data 

wi ll be available on a monthly rather than yearly basis so that trajectories 

can be produced in a more timely manner. Beginning March 1986, the 70- and 

50-mb levels will be added to the input data set to . make 12 mandatory levels 

of meteorological data (from 1000 to 50 mb) available for trajectory 

computation. 

68 
Table 6. --GMCC t~ajecto~ies calculated in 1985 

Destination 

Arnste~dam Island 

Bemuda 

Weste~n Medite~~anean 

Kathe~ine , Aust~alia 

Palme~ Station 

1984 

1984 

1984 

1984 

Oct 1983 

Date 

A~ctic locations 

spa 

Jan 1984, Jul 1985, Feb-Ap~ 1984, Jun-Jul 1984 

Summe~ 1979, 1982 Anta~ctic locations 

Equato~ial Pacific C~uise 

Poker' Flat , AK 

Ascension Island 

SMa 

MLO 

BRW 

Miami 

McMu~do 

Char'lottesville , VA 

Okushi~i Island U~umqui , China 

Beijing, China 

Niigata, Japan 

Atlantic locations 

Tallahassee , FL 

WATOX locations Ko~olev C~uise 

v~iteface Mountain , NY 

1984 

1984 

1984 

1983, 1984 

1984 

1984 

1984 

1984 

1984 

Jul , Dec 1977 

Nov, Dec 1984 

Aug 1980 

Apr' 1980 Ap~ 1980 

1978-1979 

Sep, Oct 1984 

Ap~ 1984 

1983 

Summe~ 1985 

A new fo~m was developed fo~ plots of isent~opic t~ajecto~ies. Figur'e 5 

shows tables beside the map with the isent~opic t~ajecto~ies. These tables 

give the time of ar~ival, 0000 Or' 1200 GMT , and the height, p~essu~e, and tempe~atu~e fo~ each day back along the t~ajecto~ies. The tables aid in the 

inte~p~etation of isent~opic t~ajecto~ies , p~oviding info~mation about ve~tical motion. 

The fi~st GMCC t~ajecto~ies fo~ the southe~n pola~ ~egion we~e p~oduced 

this yea~ afte~ ove~coming a computational p~oblem. The p~oblem ~elates to 

the method of conve~ting the wind displacement f~om meter's to deg~ees of 

latitude and longitude . In the t~opics and midlatidues , the displacement fo~mulas used fo~ the 2. 50 global data a~e 

DLAT 

DLON 

-SV * 10800 . /111198.4 

-SU * 10800 . /(111198 .4*COS(ABS(TSLATO*.017453 ))) , (1) 

whe~e DLAT and DLON a~e the displacements in deg~ees of latitude and longitude ~espectively, SU and SV a~e the E-W and N-S components ~espectively of the 

wind displacement in mete , and TSLATO is the latitude of the sta~t point of 

the t~ajecto~y segment . 

69 
10' Ni l 

I I 

I I 

o,s~ , J ,,,,,.,,-~-----;--~ 180 ' w 

00 Z 

OAY M I.(B K 

o 32694V9 

1 :i7 &19273 

2 " 6 ~86<:66 

3 5 511 255 

4 52 ::.282~ 

5 4 6 57~2fi4 

6 37 ~273 

7 33 (l8JV8 

,., z 

[MY K~! ~II K 

o :15 6r.227!, 

I :\96:n272 

2 5 4 51~2~ 

3 664010245 

4 79 359231 

5 72 J92237 

6 63 ~247 

759474250 

870~1I240 

Figure 5.--MLO isentropic trajectories arriving 25 April 

1979 on the 310-K surface at ( A) 0000 GMT and (8) 1200 GMT. 

In polar regions, the cosine of the latitude in the denominator in (1) 

can cause invalid results. For this reason we have reverted to the 65 x 65 

stereographic x, y grid for Arctic trajectories, but data in this form are not 

provided for the Southern Hemisphere. The solution for the Southern 

Hemisphere polar regions is to transform each 3-h latitude and longitude along 

the trajectory to an x, y point on a similar 65 x 65 grid overlaying a 

stereographic projection of the Southern Hemisphere. The 3-h wind 

displacement is then converted from meters to x, y units and added to the 

start point to get an end point in x, y units. This end point is finally 

transformed to latitude and longitude. 

Isentropic trajectories to SPO were produced for a study of seasalt 

events during the austral winter of 1982. Detailed results are reported in 

Bodhaine et al. (1986). These events are seen as peaks in the plot of hourly 

averages of aerosol scattering extinction at 550 nm (fig. 6, upper), which 

correspond to peaks in elemental Na (fig . 6, lower). The Na data were 

obtained by PIXE analysis of Nuclepore filter streakers with an 8-h time 

resolution. Figures 7 and 8 show trajectories arriving at SPO on 10 and 11 

September 1982, during a strong seasalt event . The tracks indicate rapid 

transport (1-2 days) from the vicinity of the Ross Sea. The 500-mb heights 

(fig. 9) for 10 September 1982 at 1200 GMT, show a strong low to grid south of 

SPO. This well-developed storm produced winds as strong as 40 kt at 500 mb 

near SPO. The position of the low was fairly stationary throughout the 

seasalt event. It appears that it is strong winter storms such as this that 

provide the transport of Na from the coast to SPO. During austral summer 

these events are rare. 

70 
SOUTH POLE 

2 

';-E 

~ 

, 

~ 

~ 

~ 

~ 

b 

0 

100 r 

N M 

, 

E 

~ 50 

-=-

• z ~~ f', 

o I I , I I, ,\1\ , , I , j II I I 

5 10 15 20 25 

SEPTEMBER 1982 

o· 

60' 'If 

90' E 

12.0' E 

60' S -

180' VI 

Figure 7.--SPO isentropic trajectories arriving 10 September 1982 

on the 270-K surface at (A) 0000 

GMT and (B) 1200 GMT . 

ill I 

Figure 6.--(Upper) Hourly averages 

of aerosol scattering extinction 

at the 550-nm wavelength , September 1982, SPO . (Lower ) 

Elemental Na , September 1982 , SPO. 

30 

71 

:lO' W 

o· 

60' S -

180' 'Ii 

Figure 8.--SPO isentropiC trajectories arriving 11 September 1982 

on the 270-K surface at (A) 0000 

GMT and (B) 1200 GMT. 

60' i: 

90" r: 
Figure 9.--Contours of 500-mb heights over 

Antarctica on 10 September 1982 at 1200 GMT. 

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. 

Bodhaine , B. A., J. J. DeLuisi , J. M. Harris , P. Houmere, and S. Bauman , 1986. Aerosol measurements at the South Pole. Tellus (in press). 

DeLuisi, J. J. (Ed.), 1981. 

9: Summary Report 1980. Boulder, CO , 163 pp. 

Geophysical Monitoring for Climatic Change , No . NOAA Environmental Research Laboratories, 

Harris, J. M. , and B. A. Bodhaine (Eds.), 1983. Geophysical Monitoring for 

Climatic Change , No. 11: Summary Report 1982. NOAA Environmental 

Research Laboratories, Boulder , CO, 160 pp. 

Harris, J. M., and E. C. Nickerson (Eds .), 1984. 

Climatic Change , No . 12: Summary Report 1983. 

Laboratories, Boulder, CO, 184 pp. 

Geophysical Monitoring for 

NOAA Environmental Research 

Herbert, G. A., E. R. Green , J. M. Harris, G. L. Koenig, and K. W. Thaut, 

1986 . Control and monitoring instrumentation for the conti nuous 

measurement of atmospheric CO2 and meteorological variables. Journal of 

Atmospheric and Oceanic Technology 3:414-421. 

Nickerson, E. C. (Ed.), 1986 . 13: Summary Report 1984. Boulder, CO 111 pp. 

Geophysical Monitoring for Climatic Change , No. 

NOAA Environmental Research Laboratories , 

72 
7. AIR QUALITY GROUP 

7.1 Continuing Programs 

NATIONAL ACID PRECIPITATION ASSESSMENT PROGRAM 

NAPAP is sponsored by the Interagency Task Force on Acid Precipitation. 

It was formed by Congress to address the complex issues associated with acid 

deposition in the United States. The Air Quality Group continued its 

participation in NAPAP during 1985. 

This program was divided into task groups entitled (A) Natural Sources , (B) Man-Made Sources , (C) Atmospheric Processes, and (D) Deposition 

Monitoring. The Air Quality Group contributed to Task Groups A and C during 

1985. 

Contribution of Gulf Area Natural Sulfur to the North American Sulfur Budget 

To assess the sulfur contribution of the Gulf of Mexico, possibly one of 

the major natural sources to the North American sulfur budget, a series of air 

sampling flights were conducted over the Gulf. The data , collected during 

late summer of 1984 , revealed that, within the experimental uncertainty, the 

carbonyl sulfide (COS) concentration was nearly constant at 440 ± 35 pptv. 

The dimethyl sulfide (DMS) level varied significantly, was not detected above 

the boundary layer, and had an average concentration of 27 ± 30 pptv or 7 ± 3 

pptv during onshore or offshore flow, respectively. 

As a result of its large atmospheric emission rate and its short 

atmospheric life time, DMS is one of the major sources for atmospheric sulfate 

aerosols and, therefore, for natural acidification of precipitation. On the 

basis of our data, the bio~enic annual emission from the Gulf can be estimated 

to be about 0.1 Tg (S) yr-. The actual amount of sulfur from the Gulf area 

transported into North America is a function of two major parameters: the 

atmospheric lifetime of the sulfur compounds and the volume of the air mass 

entering through t~~ corridor between Texas and Florida. The only removal 

mechanisms for S04 in the troposphere are wet and dry depOSition. The rates 

of these processes can vary significantly according to the prevailing 

meteorological conditions, and therefore, only upper and lower limit estimates 

for these variables can be made. Table 1 summarizes the estimates made by the 

Air Quality Group. 

The results of this study indicate that the potential contributi on of 

biogenic sulfur to the overall North American sulfur budget is minimal 

(between 0. 25% and 1.5%). Cloud water pH's evaluated from the lower limit 

estimate (3.7 to 5.1; see Luria et al., 1986) are identical with those 

calculated by Charlson and Rodhe (1982) from theoretical considerations. The 

upper'limit estimate of natural sulfur transport into the continent may cause 

acidification of rainwater. 

73 
Table 1.--Upper and lower limit estimates of natural sulfur 

entering North America through the Texas-Florida corridor 

Parameter 

Boundary layer depth, m 

Texas-Florida corridor width, m 

Wind speed (IBL) , m s-1 

Southerly airflow (IBL), % yr- 1 

Annual volume of air mass, m3 yr- 1 

S042- atmospheric lifetime (kw+kd),h* 

Average {S042-}, ~ m- 3 

Average S042- flux , ~g m- 2s-1 

Annual sulfur flux, Tg (S) yr- 1 

Upper li mi t 

estimate 

1000 

1 .57 x 106 

5 

50 

1.24 x 1017 

530 

6.1 

30.5 

0.251 

Lower limi t 

estimate 

1000 

1 .57 x 106 

5 

50 

1.24 x 1017 

530 

1.0 

5.0 

0.041 

*kw and kd represent wet and dry deposition in terms of first-order rate 

coefficients. 

Computer Simulation of the Oxidation and Removal of Natural Sulfur Compounds 

in the Marine Atmosphere 

To test our understanding of the natural sulfur cycle in the marine 

atmosphere, and its contribution to the atmospheric sulfur burden, a MPBL 

chemistry model was developed. The major focus of this study was a comparison 

between model predictions based on laboratory rate measurements and actual 

field data . Simulations were performed for clean-air conditions and for 

several polluted air scenarios. Figure 1 presents a schematic illustration of 

the chemistry model. A description of the model is given in Luria and Meagher 

(1 986) . 

Solar 

Radialion 

Oceanic Emission 

74 

Figure 1.--A schematic representation of the MPBL chemistry 

model. 
It is gene~ally accepted that OMS is the most impo~tant ~educed sulf~ 

species in the ma~ine atmosphe~e. Its concent~ation is dete~ined by the 

balance of oceanic emission and atmosphe~ic ~emoval . Since OMS concent~ation 

data a~e available, the model was used to estimate the oceanic emission ~ate 

~equi~ed to sustain the obse~ved ave~age level of 27 ppt . To_~uPpo~l this ave~age concent~ation an oceanic emission ~ate of 60 ~ (S) m day was 

~eq~~~ed. This emission estimate is lowe~ than the value of 290 ~g (S) m-2 

day ~epo~ted by An~eae and Raemdonck (1983) but is in good ag~eement with 

the wo~k of Gammon and Bates (1985) who ~epo~ted an emission ~ate of 80 ~g (S) 

m- c day- 1. As expected , t he model p~edic ed a signifi cant di~nal cycle fo~ 

OMS , with levels a~ying by a facto~ of 4 f~om the dayti me low to the 

nighttime high. And~eae and Raemdonck (1983) ~epo~ted a simila~ di~nal 

va~iation, albiet with a lowe~ amplitude (max./min . = 1.6). Plots of the 

model p~edictions fo~ OMS and othe~ sulfu~ species a~e p~esented in fig . 2. 

100 

80 

~ 

15. 

-=0 60 c 

0 

~ 

~ ~ 

c 

'" u 

c 40 0 

'-' 

20 

SO/-

S02 

OMS 

MSA (I) 

6 12 6 

Loca l Time (hours) 

Figu~e 2.--The model-p~edicted concent~ations 

of DMS and othe~species as a function of time . 

12 

The photochemical model developed was found to ~ep~oduce accu~ately the 

majo~ featu~es that cha~acte~ize the sulfu~ cycle in the ma~ine atmosphe~e. 

In pa~ticula~ , the model p~edicted 03 ' S02 ' S042-, and N03

- levels in good 

ag~eement with field obse~vations. The DMS emission ~ate necessa~y to 

~ep~oduce obse~ved ma~ine concent~ations was found to be consistent with othe~ 

estimates. The model was unable to ~ep~oduce ~epo~ted methane sulfonic acid 

75 
(MSA) levels without the inclusion of an unreasonably high removal rate. The 

atmospheric fate of MSA requires additional research before this inconsistency 

can be resolved. 

Diurnal fluctuation in DMS was predicted to be greater than that 

observed. The model assumes a constant DMS emission rate throughout the day, 

but changes in ocean surface temperature, wind speed, and atmospheric 

stability between day and night may serve to reduce the amplitude of the 

diurnal cycle. The model confirms the observation of relatively low levels of 

DMS in coastal areas influenced by anthropogenic emissions. However, under 

certain specific pollution conditions, the model predicted a short-term 

abatement of the DMS removal reactions. 

Aerosol Enhancement by Cloud Evaporation 

Clouds can dramatically alter the aerosol distribution in their 

environments. It is well known that nucleation- and accumulation-mode 

aerosols may be removed by cloud droplet nucleation and scavenging. As well, 

coarse-mode particles may be removed by precipitation scavenging. Researchers 

are only now beginning to explore how clouds may release aerosols as they 

evaporate. In this study the results of some preliminary measurements made 

atop Whiteface Mountain, NY, during two cloud evaporation events are 

presented. 

An ASASP was used to sense aerosol particles in the diameter range 0.1 to 3~. The ASASP probe consists of a laser imaging mechanism that examines a 

known sample area as particles pass through it. Its operational 

characteristics are described by Pinnick and Auvermann (1979) and Garvey et 

al. (1984). It was operated continuously during the sampling period, and 

complete spectra were recorded at 5-s intervals. 

A stratiform cloud formed atop Whiteface Mountain during the night of 3 

August 1983 (0200 GMT, 4 August 1983). It dissipated at about 0410 GMT only 

to reform at about 0515 GMT. The ASASP-derived particle spectrum 

conc~~tration and mass prior to the onset of the cloud were 3486 cm- 3 and 31 

ug m ,characteristic of a polluted air mass. 

The 5-min-average particle spectra obtained using the ASASP before cloud 

formation and after cloud demise were compared. The differences between a 

particle spectrum measured between 0100 and 0105 GMT (before cloud formation) 

and particle spectra made during cloud evaporation are shown in fig. 3. They 

are plotted in a log difference vs. log diameter format. The ordinate is the 

decimal logarithm of the difference between the spectrum at the times 

indicated and the spectrum measured prior to cloud formation. The abscissa is 

the decimal logarithm of particle diameter. 

The difference spectrum valid between 0345 and 0350 GMT was made prior to 

evaporation of the cloud. It shows that a marked depletion in the aerosol had 

taken place at diameters less than about 0.4~. This effect can be 

qualitatively explained as a combination of initial nucleation and in-cloud 

scavenging. 

76 
4 

3 

1 

I 

I 

-3 

-4 

4 

3 

1 

I 

-3 

-4 

4 

3 

1 

I 

I 

- 3 

-4 

J 

)v' 

J 

\.7 

J 

C7 

0345

1 

0350 Cone 3379 

Mass 17.3 

,~ 

• 

J 

r/ 

0400

1

04 05 Cone. 400 1 \ 

. ~ 

Mass 18.9 

~ 

--

I 

V 

" 

041 5 1 0410 Cone. 3791 \ 

Mass 19.9 

tt 

"" 

0350

1 

0355 Cone. 3367 0355 10400 Co ne. 3712 

Mass 17.4 Mass 18.1 

\t ~ 

J 

VV 

0405 10410 Cone. 4146 "41 0 I 0415 Cone. 3614 

Mass 30.1 Mass 17.6 

l 

I A.. r~.L , 

T 

J 

l.J 

I "'" \ I 

0410 0415 Cone. 5191 0415 0430 Cone. 6005 

Mass 41.6 1\ Mass 46.1 

\ \: ~ f----- v.. 

f----

4~~~----~--------~~~----~------~~~~-----r------~ 

3 "\ A 0430' 0435 Cone 6111 "- 0435'0440 Cone. 6519. ~ .... \0446 04 45 Cone. 7667 

Mass 1577 ... '\ Mass 51.1 "-. Mass 76.4 '- \ 1· --~,---l----.=.:.::..::....j ~-------=----..:; ~I-----------I 

\ ~ \J 1A '--~~-.lli\:~~---I f--~~---I-\~~-----1 ~ 

~ -I ~------+------___i 1------------+---------1 ~-------l----------1 

~ <5 -1 1------1--------1 1------l-------1 f-----+-------I 

------+_------~ ------_4------___I ------+------___i 

-4.l-______ ~ ______ ~L ______ ~ ________ L_ ______ ~ ______ ~ 

- I 0 I -I 0 I -I 0 

log Diameter (,~l. ) Log Dlamelel (I'm) 

Figure 3. --The diff erence spectra between a particle spectr um measured before 

cloud formation and t welve 5-mi n mean spectr a measured duri ng cloud evapor ation . 

77 
The difference spectrum valid- between 0350 and 0355 GMT demonstrates the 

regularity of the depletion while the cloud was still present. Then, between 

0355 and 0400 GMT, the cloud began to evaporate. Immediately, the difference 

spectrum shows that a significant excess of particles appeared at the smallest 

detectable sizes. Total particle concentration also increased, but total 

particle mass was relatively unaffected. 

The difference spectrum valid between 0400 and 0405 GMT shows that 

significant numbers of new particles continued to be detected. The new 

particles also seemed to be creating excesses at diameters up to 0.4 ~m. The 

diameter range above 0.4 ~ remained relatively unaffected . The spectral 

differences remained relatively unchanged until 0420-0425 GMT. At that time, 

excess particles began to fill in the accumulation mode, which had been 

severely depleted during the life of the cloud. Significant numbers of new 

particles appeared at the larger sizes as well. The combination of new 

particles at small sizes and those at larger sizes were filling in the 

depleted accumulation mode completely. This filling-in process was complete 

by 0430-0435 GMT. Two 5-min averages after this demonstrate the stability of 

this new enhanced aerosol distribution. 

We interpreted the facts presented in these distributions in the 

following way. Before the onset of evaporation, the nucleation-mode and 

accumulation-mode aerosol had been depleted by cloud droplet nucleation and 

in-cloud scavenging. As the cloud began to evaporate , a large number of new 

particles were created at sizes below our detection limits (0.1 ~m 

diameter). These particles grew rapidly by means of coagulation to fill in 

and later enhance the accumulation mode. Meanwhile, more new particles were 

continuously forming to replenish the supply lost through coagulation. As 

evaporation became complete, new larger particles began to appear as cloud 

droplets released the remaining particles contained within them. The final 

distribution was composed of the excess larger particles released by the 

droplets, and the new small particles created during the evaporation event. 

Thunderstorms: An Important Mechanism in the Transport of Air Pollutants 

Convection, as a means of vertical transport, is incompletely understood, 

although it is a key mechanism of circulation within the troposphere. The 

observations summarized here and presented by Dickerson et al. (1986) present 

the first unequivocal data in support of convective transport of photochemically active trace gases in a cumulonimbus cloud system. 

Several research aircraft were outfitted with instruments to measure 

meteorological parameters and the trace gases CO, 03, NMHC, and reactive 

nitrogen compounds. For high-altitude work, a Sabreliner (twin-engine jet), 

operated by NCAR, was used. For the midtroposphere and PBL, two propellerdriven aircraft , the NOAA King Air and the Brookhaven Queen Air, were used. 

The flights were conducted in collaboration wi th the NOAA PRE-STORM project, 

which supplied radar, satellite, balloon soundings , and standard meteorological measurements. PRE-STORM was conducted in the Central Plains of the 

United States during May and June of 1985. 

The gases CO and 0, were selected as primary tracers of air motion 

through clouds because Ehey are relatively insoluble in water, rapidly 

detected , and have atmospheric residence times that are much longer than the 

78 
detected, and have atmosphe~ic ~esidence times that a~e much longe~ than the 

lifetime of a thunde~storm. These gases gene~ally demonst~ate distinctive t~oposphe~ic altitude p~ofiles. CO is p~oduced p~im~ily by g~ound sou~ces 

and dest~oyed throughout the t~oposphe~e , and thus gene~ally dec~eases with 

altitude. 0

3 is p~oduced p~ima~ily in the st~atosphe~e and dest~oyed at the 

Ea~th's su~face, and thus gene~ally inc~eases with altitude. Any deviation f~om envi~onmental p~ofiles of these gases within the cloud du~ing the 

thunde~sto~m is presumed to be due to oonvection . 

Late on the night of 14 June 1985 , a la~ge mass of cold, d~y air moved 

south ove~ warm, moist ai~ f~om the Gulf of Mexioo. The ~esult was an intense 

band of thunde~sto~ms stretching f~om Ama~illo to Chicago . At dawn on 15 June 

the ai~c~aft flew to;la~d the expected inflow and outflow ~egions of the 

cumulonimbus. 

As the Sab~eline~ climbed in clea~ ai~, the mlxlng ~atio of CO fell 

smoothly (fig . 4) until the cumulonimbus anvil was penet~ated at 10 km. 

Within seconds, the CO level ~ose sha~ply. Soon it mo~e than doubled , 

~eaching ooncent~ations ~~ely obse~ved at this altitude. The in-cloud CO concent~ation was highe~ than that of the ai~ outside the cloud at all 

altitudes sampled . The maximum CO level and the co~e of the outflow appea~ed 

to be at about 10 km. 

The downd~aft of the thunde~sto~m can be 

The~e is a local minimum in CO at about 2 km. 

~egion was about -1 m s-1 As we expect, the 

f~om aloft down to the lower t~oposphe~e . 

0; 

~ 

.. 

CO CONTOUR PLOT 

12 

--' 10 ~ r---~---elo-________ -J 

Vl 

!: 8 ~ r-----~-ICIO---------/ 

"" 

~ 6 

w 

o 

=> 

I- 4 

15 JUNE 1985 

clea~ly identified in fig . 4. 

The ve~tical ai~ motion in this downd~aft ca~ries clean, d~y ai~ 

'::. 

SUrface~ 

"" 

2~~~_ 98°wt 97" 96- 95° 94° 

Figu~e 4.--The twodimensional CO field (ppbv) meas~ed using the ~esea~ch 

ai~c~aft on 15 June 1985 . 

Oklahoma 

City LONGITUDE 

93· 92· 

79 
Dickerson et al. (1986) presented the first observations of trace gases 

measured in a thunderstorm. The results clearly indicate that convective 

processes such as occur during thunderstorms can be an important mechanism in 

the vertical transport of air pollutants. 

Sulfur Dioxide Flux Measurement over the Western Atlantic Ocean 

During the winter months of 1985, aircraft sampling flights were 

performed by the Air Quality Group over the Western Atlantic Ocean and in the 

vicinity of Bermuda. One purpose of these flights, which were carried out as 

part of HATOX, was to determine the eastbound flux of anthropogenic emiss ions 

from the North American continent to the Atlantic Ocean atmosphere. The 

results, summarized here and presented by Luria et al. (1987), represent our 

continuous measurements of gaseous sulfur and the evaluation of these data to 

estimate the eastbound sulfur dioxide flux. Sulfur dioxide was measured with 

a Meloy 285 sulfur analyzer with an FPD. 

Galloway et al. (1984) estimated the flux of sulfur and nitrogen 

compounds eastward from North America using surface S02 measurements , 

climatologically derived wind speeds, and the coastal divisions established by 

Whelpdale et al. (1984). They estimated fluxes for eight coastal segments 

from the northern end of Newfoundland, Canada , to the southern tip of 

Florid~l According to their estimates, the total_fnnual S02 flux was 1.75 Tg 

(S) yr ,of which 0.30, 0.82, and 0.37 Tg (S) yr were transported eastbound 

from coastal segments 4, 5, and 6. The availability, for the first time, of 

in situ S02 and wind speed data encouraged us to repeat these calculations. 

They are based on a limited data set and therefore must be considered as a 

preliminary estimate. 

Since our study was performed within coastal segment 6, it was possible 

to compare our results with the estimates of Galloway et al. (1984). Our 

results are given in table 2. Our values and the estimates of Galloway et al. 

(1984) differ by a factor of 2.7. Nevertheless, the two estimates should be 

considered to be in good agreement, taking into account the different 

approaches. 

Table 2.--Parameters used in estimation of the annual S02 flux 

eastward from the North American coastal segment 6 

Parameter Average 

time (1 year) 3.15 x 107 s 

a* 82.0 

b* 1.44 x 10-3 

(r2)* 0.54 

8t 0.69 

lIxt 8.4x105 m 

flux (S02) 1 .01 tg (S) yr-1 

*Regression and correlation coefficients for exponential fit. 

tAfter Whelpdale et al. (1984). 

80 

Maximum 

3.15x107 s 

161 .0 

1.48 x 10-3 

0.55 

0.69 

8.4x105 m 

2.04 tg (S) yr- 1 
It is obvious that more measurements , with improved analytical methods , which would be carried out throughout the year and at the different coastal 

segments , are needed for accurate flux estimations. However , this work has 

demonstrated that a rough agreement between climatological estimates and field 

observat ions can be obtained . 

AIRCRA,T INSTRUMENTS 

Aircraft Instruments and Their Capabilities 

During 1983, the Air Quality Group acquired the use of a Beechcraft King 

Air aircraft from the National Park Service (NPS). Ownership of the aircraft 

has since transferred from the NPS to NOAA 's Office of Aircraft Operations. 

The Air Quality Group has engaged in an ongoing effort to install and upgrade 

a scientific instrument package aboard the aircraft. The package consists of 

a suite of scienti fic instruments, a power distribution system to supply power 

to them, and a data acquisition system to digitize and record the incoming 

scientific data for later analysis. 

Table 3 outlines the scientific instruments currently aboard the aircraft 

and gives their accuracies , response times , and precisions. In addition to 

the instruments outlined in table 3, several optical array probes are 

available for atmospheric aerosol measurements. They include an ASASP (0.1 to 

3 urn ), an FSSP (0.5 to 45 urn) and a two-dimensionsal probe (25 to 800 um). 

These pr obes can provide aerosol particle size and shape information within 

their respective ranges. 

Table 3. --Scientific instruments available aboard the King Air 

Parameter Units Accuracy Response Precision Description 

Photometer W m 2 lOllS Short wave sun photorneter 

TEeO S02 ppbv 1 ppbv 60 s 0 . 1 ppbv Pulsed fluoroscence 

Dynamic pressure mb 0 .1 mb 1 s 0.1 mb Pitot tube 

Temperature °e 0.1 °e 1 s 0 . 1 °e Rosemount wire 

Dew point °e 1.0 °C 5 s 0 .1 °C General Eastern 

cooled mirror 

Air flow lpm 0.1 lpm 1 s 0.1 lpm Kurz meter (3) 

Pressure mb 0 .5 mb 1 s 0. 1 mb Pitot tube 

Meloy S02 ppbv 2 ppbv 10 s 0.1 ppbv Photometric 

TEeo 03 ppbv o ppbv 10 s 0 . 1 ppbv Flame photometric 

Position degrees ±200 m 1 s Loran C 

True air speed m 3- 1 m 5- 1 1 s 0 . 1 m 5- 1 Computed 

Heading degrees deg 1 s 1 deg Magnetic compass 

Wind direction degrees deg 60 s 0.1 deg Computed 

Wind speed m 5- 1 m 5- 1 60 s 0.1 m 5- 1 Computed 

81 
The Efficiency of an Airborne Cloud Water Separator 

Numerous investigators have examined the chemistry and physics of dry 

atmospheric aerosol and water in clouds and precipitation . One problem to be 

addressed was the scavenging of atmospheric aerosol by cloud droplets. In 

order to examine both the cloud water and the interstitial aerosol, a 

combination cloud water separator and cloud water collector was developed. 

To test the efficiency of the cloud water separator, we assembled a 

l~~ratory apparatus consisting of (1) a high-VOlume air blower (100,000 cm3 

s ), (2) a hot-wire anemometer, (3) an ASASP aerosol sampler, and (4) an FSSP 

cloud droplet spectrometer . 

The ambient aerosol distribution in the laboratory was measured to 

establish a control . Then, the ambient air was drawn through the separator at 

various airspeeds and the resultant aerosol distributions were measured. A 

comparison between these distributions and the control was made . 

Figure 5 presents these comparisons . Each plot is the percent difference 

between the control distribution and the distribution sampled at a given 

airspeed after exiting the separator . The top left plot indicates t~~t all 

particles up to 3 ~m in diameter passed through the cyclone at 8 m s . The 

middle left plot shows that particles with diameters greater than 1.2 ~m were 

reduged in number by 20% or more after passing through the separator at 13 

m s-. This effect progresses to smaller and smaller diameters at the faster 

airspeeds. 

A more complete description of this work is given in Boatman and Wellman 

(1985) . The primary results produced by the laboratory tests are the 

following : 

(1) Dry aerosols traveled through the cyclone, provided their diameters were 

smaller than about 0.7 ~m if the airspeed through the separator was less 

than 24 m s-l . 

(2) All water drops larger than 0.5 ~ were ,emoved from the airstream by the 

cyclone at airspeeds as small as 12 m s- • 

(3) A substantial portion of the water passing through the separator was 

collected at the bottom. 

Data Display Capabilities 

The data collected using the King Air can be analyzed and displayed in a 

variety of ways. Tabulated values in engineering units for each variable 

measured are routinely produced. In addition, a variety of graphical 

presentations are available. 

Figure 6 presents the flight track from a typical aircraft flight. The 

aircraft departed from Boston , MA, made a number of sampling runs about 100 km 

offshore, and returned to Boston . Figure 7 presents the outside air pressure 

(mb) versus time for the same flight . Such plots can be made for any 

scientific variable measured . Figure 8 presents the pressure (mb) versus 

temperature (OC) for this same flight. Any measured variable can be plotted 

against any other measured variable for comparison purposes. 

82 
~ 50 c 

~ 

~ 

c O~ --~~~~tt-----~ 

c · .. ······· .... ········ .... ··· ................ . .. 

l:! 

&.. - 50 

- 100 L---'---'---'-LLl~ __ ..J..LJ.L-L.L.J..Ll~ 

- 1 0 

Log Diameter (;1m) 

13 m S - l 

100 '--,-,--.rn-m"'-''-r--'TTTT111 

c: 

.. 

l:! 

~ -50 

-100 ';--1-1-'-Ll.J--'-';';oL--Ll..1L.L..L-'-U~ -1 

Log Diameter (;1m) 

17 m 5- 1 

100 ,--.-...-rn-rn=::"-"-TTTTlTl 

.8{flm 

-'OO';--1~LL~LhlO~-1~~~~ -1 

Log Diameter (;1m) 

20 m a- 1 

100 ,--,-,..-rn-m-=:;---'TTTTlTl 

c: 

.. 

l:! 

&. - 50 

-c: 

.. 

l:! 

-, O~':-, ----L..J....L.L.L1JLLO':-----'--'..J--'-LLLL~ 

Log Diameter (;1m) 

24 m .-1 

100 ' -'--'''TTmr---"-T--,rrTTTIn 

8? - 50 

.. 

o 

c 

~ 

~ 

c 

c: 

.. 

l:! 

-,O~~,--..J....-'-.1....1..LJ..llO~-1-'-LJ...J....L~ 

Log Diameter (;1m) 

26 m 5-1 

100 ,--,-,--.rn-m-=:"--'TTTT111 

50 

Or-----------------~ 

&. -50 

100L--1-1LLLLLUi~-llLULLLLLL~ 

-1 0 

Log Diameter (;1m) 

r igur e 5.--Cornparison pl ots between the control aer osol spectrum 

and aerosol distributi ons measured after passi ng air through the 

coud water separat or at various speeds . 

83 
:0-

E 

'" ~ 

::> 

V> 

V> 

'" ~ 

C>-

Date; 860109 

Scale 

1 I , 

a 50 100 

(km) 

Date = 860109 

500,-r-,-.--,-.-,,-.-.-,--, 

600 

700 

800 

900 

1000 

0900 1000 1100 1200 1300 1400 

Time (EST) 

Figure 7.- -The atmospheric pressure 

(mb) as a function of time during a 

portion of the research flight 

depicted in fig. 7. 

Figure 6.--The flight track from a 

typical research mission conducted near 

Boston, MA, as a part of WATOX. 

Date Time (EST) 

860109 0909-0945 

500 I I I I , 

f- -

600 - -

-

E 700 - _ ..... - - 's . 

: ' '" ~ '. . ::> .. V> 

V> 800 - . , -

'" ~ . . C>- .' . 

900 - -: 

'- . . . 1000 l- . -

I , i . . -j- I , 

-9 -7 -5 -3 - 1 

Temperature (0C) 

Figure 8.- -The air temperature (Oe) 

as a function of atmospheric pressure 

(mb) during a portion of the research 

flight depicted in fig . 7. 

84 

1 
7.2 Special Projects 

SMALL-PARTICAL DRY DEPOSITION 

To predict possible environmental effects of air pollution, data are 

needed on natural removal rates as well as pollution emission rates from local 

and regional sources. The problem of acid deposition, for example, cannot be 

assessed unless both the dry and wet deposition values of strong acids can be 

determined reliably in remote as well as polluted environments. The removal 

rate of aerosol sulfur (S) from the atmosphere to an underlying surface is 

usually parameterized in terms of a deposition velocity, Vd--the ratio of 

particle S flux to its concentration at or near the surface of interest. 

Several measurements of particle S deposition have been reported (e.g., Droppo 

et al ., 1983; Hicks et al. , 1982 ; Sievering , 1982). These reported data_90 

not include any high-wind-speed cases (i.e., speeds greater than 6-7 m s ). 

The results summarized here and reported by Sievering (1986) are measurements 

of high-wind-speed S mass deposition (and also soil mass deposition as 

represented by AI, Ca, and Fe) over agricultural fields of moderate 

roughness . The measurements were taken during dry air (r.h. <40%) and 

relatively dry soil conditions , thereby avoiding the possibility of 

contamination by hygroscopic aerosol (especially sulfur-related) growth and 

decay , which has plagued some other aerosol deposition studies (Hicks et al ., 1982 ; Sievering , 1982) . 

The measurements were made on 6 June 1982 at the BAO during a chinook 

wind. The westerly wind was quite steady (265°-290° wind vector) and came 

from the clear-air Rocky Mountains source region located about 50 km west of 

the BAO. An undisturbed and adequate fetch has been observed for this wind 

sector (Schotz and Panofsky , 1980) to give logarithmic wind profiles up to 150 

m with a well-specified roughness length, zO ' of 4 ± 2 em during low and 

moderate wind speeds. A detailed description of meteorological 

instrumentation and general BAO site characteristics for particle gradient 

measurement is found in Sievering (1982) . 

Sulfur- and soil-mass-gradient measurements over agricultural fields 

dur'ing clean-air and high-wind-speed conditions indicate very large deposition 

rates , even approaching momentum transfer. Mass deposition rates for soilderived AI , Ca, and Fe were always greater than the rate of anthropogenic 

sulfur , as would be expected given the large MMD of soil particles relative to 

that of sulfur . These results, though somewhat preliminary owing to the small 

number of gradients observed , indicate substantially larger particle 

deposition velocities than predicted on theoretical grounds. For particle 

sulfur , no daytime surf~ge resistance (rs ) is calculated to have prevailed 

during the nearly 9 m s wind speeds encountered, although some surface 

resistance is suggested for the nighttime 6-7 m s-1 wind spe~9 data. This 

particular result is not in agreement with the rs = 1-3 s em obtained by 

others for small- particle, eddy flux measurements . Noting that the geometric 

mean (number) diameter for small-particle , eddy flux measurements has been 

several times smaller than the MMD for the particle S mass-flux gradient 

measurements here reported, the discrepancy in rs is not unexpected. The S 

mass deposition rates of 0.9 and 2. 65 cm s-1 , during stable and unstable 

periods , respectively, are applicable to anthropogenic sulfur deposition , 

85 
since its air concentration was 50-140 times that which could have been soil 

derived. The large deposition velocities for particle sulfur observed at this 

site may apply at other remote, overland sites under high-wind-speed 

condi tions and over landforms of at leas t moderate roughness and having 

closely spaced surface roughness elements. Since essentially all the sulfur 

at the BAO (Ganor et al ., 1983) is in the form of sulfate, these large 

depcsition rates should apply equally well to sulfate. 

WINDS IN THE GRAND CANYON 

The Air Quality Group has participated in a study, spcnsored by the 

National Park Service, to better understand the wind patterns in the Grand 

Canyon. The terrain near both the south and north rims of the Canyon is 

heavily forested; therefore, controlled burning has become necessary along the 

rims to meet resource management objectives. This burning is done during the 

spring and fall of the year when the forest is dry and cool. A significant 

amount of smoke is produced, creating the pctential for reduced visibility and 

a concomitant decrease in the Canyon's scenic splendor. Another problem is 

that the wood smoke , on occasion, could be transpcrted from the burn site into 

the small town of Tusayan, south of the Canyon 's rim, causing annoyance to 

residents and visitors alike . 

In 1984 and 1985, three permanent ground stations were utilized to 

provide temperature, humidity, moisture, and wind data on the North and South 

Rims and on Tonto Plateau within the Grand Canyon. The distance between the 

North and South Rim Stations is about 34 km. The distance between the South 

Rim Station and Tonto Plateau is about 23 km. The purpcse of the research was 

to determine wind patterns within and adjacent to the canyon. 

Figures 9 illustrates the hourly wind vector averages for the month and 

the constancy of the winds in 1984 and 1985 in UT (GMT), where UT = MST + 7. 

The South Rim Station data show an almost constant wind from the south to 

west quadrant. Winds with a northerly component occur mostly after 1800 UT 

except in January and February. The average wind is strongest in May and June 

and is also most constant in those months. This contrasts strongly with the 

North Rim Station where strong winds are more a function of time in April 

through November, but compares to the wind strength on the Tonto Plateau. 

On the North Rim winds tend to be light at night and strong during the 

day . The winds are extemely constant during August, especially during 0000-

1300 UT (1700 and 0600 MST). The very small vectors indicate that a light 

drainage wind from the north at speeds of 0-1 m s-l is present. This 

conclusion is drawn from the average winds in the raw data. 

On Tonto Plateau a downcanyon wind would be from the ESE. No such 

downcanyon winds are observed except in the winter months of December, 

January, and February. These winds are not confined to nighttime hours. 

Downslope winds at night, which might encourage downcanyon flow, would be 

expected around 0700-1200 UT, especially after hot days in the summer, and 

would be from the SSW. These are also not found in the canyon averages. The 

86 
At'G 

J Ut 

JUI'I 

." 

)lOV :lOV 

"" 

'"' Jl':1 '"' 

WAY 

'" 

,~, 

~,==~~~~::~==~,,~~,~,~~,.;=~,~,~~'" S1A11O)( : ]IIOR TH YI:AR : 1984 

-> 5.75 ms - 1 

JUI'I 

loUT 

'"' 

'"' 

STATIO)( : 1I0UTIl 

Figure 9.--South Rim, North 

Rim, and Tonto Station wind 

vector averages and constancy 

percentages. The monthly wind vecto~s a~e ave~aged by the 

hour . Constancy is expressed 

as the percentage ratio of 

vector to scalar mean wind 

speeds. Isolines represent 

20% increments of constancy. 

'" 

JUS 

IL\.!I. 

~====;=~~==:;::~~::~::~~~:::JJA~ 12 I~ 18 21 

STAno,,: 101'110 RAR: 198~ -> 5.35 ms- 1 

87 
constancy of the wind is lowest at 1800 UT in Novembe~ and all of Janua~y , and 

highest du~ing nighttime hou~s in Ma~ch-Oct be~. These combined facts ~eveal 

that the wind is p~im~ily upcanyon th~oughout most of the yea~ . 

Meteo~ological meas~ements we~e also made f~om an inst~umented ai~c~aft 

and included studies of tempe~at~e , dewpoint, wall and inte~face 

tempe~at~es , and ho~izontal and ve~tical wind speed and di~ection . The 

flight missions we~e made in the fall of 1984 and the sp~ing of 1985 (Ap~il , 

May , June , Septembe~, and Octobe~) . June and Septembe~ data indicate that the 

canyon is capable of scou~ing ~ cleansing itself, whe~eas Octobe~ data show 

that a st~ong new ai~ mass is needed to ~emove pollutants f~om the canyon . 

This is so because of dec~eased sol~ heating of the walls and inte~face as a ~esult of dec~eased sun angle and length of day in Octobe~. 

To f~the~ unde~stand the t~anspo~t patte~ns unde~ p~evailing 

meteo~ological conditions, a conceptual model fo~ the mean ai~ motions in the 

G~and Canyon was developed using cavity flow . This mode l was enhanced afte~ 

close examination of the G~and Canyon balloon-wind data available to us. Conve~sely , the wind data became mo~e unde~standable and consistent when 

placed in this f~amewo~k. 

Conside~ fi~st the case of coupled flow (whe ~e ai~ f~om above and below 

the Canyon 's ~im is inte~acting) eithe~ du~ing the day o~ at night. We 

p~opose that the mean winds in the G~and Canyon, unde~ these conditions , a~e 

of the type shown in fig . 10. Fig~e 10 is a plan view of the wind patte~n; 

fig. 10 is a c~oss-section view . Figu~e 10 suggests that ai~ below the level 

of the Canyon ~im moves p~edorninanLly pa~allel to the Canyon itself. The 

depiction indicates that the di~ection of this pa~allel motion is always along 

the di~ection of the ai~flow c~ossing above the Canyon . That is , ai~ within 

the Canyon moves eastwa~d (west wind) when the synoptic-scale winds a~e f~om 

the west . Figu~e 10 also indicates that the ai~ below the Canyon ~im is unde~going a sp ~al motion . This is due to the seconda~y cavity flow. Figu~e 

9b depicts this flow in c~oss-section . The second~y cavity flow is p~oposed 

to p~oduce upd~afts along the upwind walls of the Canyon and downd~afts along 

the downwind walls. The ai~ in the cente~ of the Canyon is p~oposed to have 

no ve~tical motion. A seconda~y ai~ cu~~ent counte~ to the p~evailing 

synoptic flow is p~oposed to occ u~ at the bottom of the Canyon. 

Conside~ second the case of decoupled flow whe~e ai~ f~om above and 

below the Canyon ' s ~im is not te~act ing) , eithe~ du~ing the day ~ at 

night . We p~opose that the mean winds in the G~and Canyon a~e of the type 

shown in fig . 11 unde~ these conditions. Fig~e lla is a plan view of the 

wind patte~n; fig. llb is a c~oss-section view . Figu~e lla suggests that ai~ 

below the level of the Canyon ~im is unde~going d~ainage flow. Fig~e llb 

suggests that no seconda~y c~oss-canyon flow is p~esent unde~ decoupled 

conditions. The potentially stable ai~ below the Canyon ~im is p~oposed to d~ain gently down~ive~ (into the pape~ in fig. llb). 

88 
Figure 10.--A conceptual view of 

the wind pattern in the Grand 

Canyon under coupled conditions 

for (a) a plan view and (b) a 

cross-section view. 

Figure 11.--A conceptual view of the 

wind pattern in the Grand Canyon under 

decoupled conditions for (a) a plan 

viw and (b) a cross-section view. 

The results, summarized here and given by Boatman and Henderson (1986) in 

support of this conceptualization, are as follows: 

(1) AirflOW below the rim level moves predominantly parallel to the 

Canyon during coupled flow conditions that may occur during any month 

of the year . (2) The secondary cavity flow suggested in our conceptualization occurs 

predominantly during coupled condi tions . These condi tions are mos t 

often associated with periods of clear days and nights. 

(3) A strong shear layer was often present near the Canyon 's rim level. 

Air below this layer appeared to be draining gently downriver. Above 

this layer, synoptic-scale forces predominated . (4) Winter months appeared more prone to decoupled (or drainage flow) 

behavior within the Canyon. It may be that potentially cold air from 

radiative cooling , frontal passages or snow at the rim is responsible 

for this. 

(5) Shear layers were present at lower levels within the Canyon. They 

may have been the product of a slow erosion process from above or the 

establishment of a radiation inversion. They appeared to act as an 

alternate bottom to the Canyon for airflow purposes . (6) At times , scouring occurred instead of secondary cavity flow. This 

may have been limited to very light wind cases or instances where 

shear layers established an alternate bottom to the Canyon. 

89 
7.3 Refe~ences 

And~eae, M. 0., and H. Raemdonck, 1983. Dimethyl sulfide in the su~face ocean 

and the ma~ine atmosphe~e: A global view . Science 221 :744-747. 

Boatman, J. F., and D. Hende~son, 1986. G~and Canyon wind study aids in smoke 

management. Pa~k Science 6(4):18-19. 

Boatman, J. F., and D. Wellman, 1985. The efficiency of an ai~bo~ne cloud wate~ sepa~ato~. P~oceedings 1985 Inte~national Symposium on Moistu~e and 

Humidity, Washington, D.C., 15-18 Ap~il 1985. Inst~ument Society of 

Ame~ica, Resea~ch T~iangle Pa~k, NC:143-146. 

Cha~lson , R. J., and H. Rodhe, 1982. Facto~s cont~olling the acidity of 

natural ~ainwate~. Natu~e 295:83-684 . 

Dicke~son , R. R., G. J. Huffman, W. T. Luke, L. J. Nunne~mache~, K. E. Picke~ing, A. C. D. Leslie, C. G. Lindsey, W. G. N. Slinn, T. J. Kelly, P. 

H. Daum, A. C. Delany, J. P. G~eenbe~g , P. R. Zimme~man , J. F. Boatman, J. 

D. Ray, and D. H. Stedman, 1986. Thunde~sto~ms: An impo~tant mechanism in 

the transport of ai~ pollutants. Science (accepted fo~ publication). 

D~oppo, J. G., J. C. Do~an, O. B. Abbey, and D. W. Glove~, 1983. D~y 

deposition field studies. Elect~ic Powe~ Resea~ch Institute Document No. 

EA-3096, Westlake Village, CA . 

Galloway, J. N., D. M. Whelpdale, and G. T. Wolff, 1984. The flux of S and N 

eastwa~d from No~th Ame~ica. Atmosphe~ic Envi~onment 18:2595-2607. 

Gammon, R. H., and T. 

sulfu~ compounds. Septembe~, 1985. 

S. Bates, 1985. Ma~ine sou~ce strength of ~educed 

Paper presented at the NAPAP Conference, Boulde~, CO, 

Gano~, E., R. F. Pueschel, and C. T. Nagamoto, 1983. Sulfates and nit~ates: 

Concent~ation as a function of pa~ticle size in easte~n Colo~ado. NOAA Ai~ 

Resources Lab . Rep., Boulde~, CO. (unpublished manusc~ipt). 

Ga~vey, D. M. , R. G. Pinnick, and G. Fe~nandez, 1984. Response characte~­

istics of the Pa~ticle Measu~ing Systems active scatte~ing ae~osol 

spect~ometer probe (ASASP-X) . U.S . A~my Electronic Resea~ch and 

Development Command Rep. ASL-TR-0156, Adelphi, MD, 24 pp. 

Hicks, B. B., M. L. Wesely, J. L. Du~ham, and M. A. Brown, 1982. Some di~ect 

measurements of atmosphe~ic sulfu~ fluxes ove~ a pine plantation. 

Atmospheric Envi~onment 16:2899-2903. 

Lu~ia, M. and J. F. Meaghe~, 1986 . Compute~ simulation of the oxidation and 

removal of natu~al sulfur compounds in the ma~ine atmosphe~e. P~oceedings 

6th Inte~national Clean Air Cong~ess , Sidney , Aust~alia, August, 1986. 

Lu~ia, M., C. C. Van Valin , J. F. Boatman, D. L. Wellman, and R. F. Pueschel, 

1987 . Sulfu~ dioxide flux measu~ements ove~ the western Atlantic Ocean, Atmosphe~ic Envi~onment (submitted) . 

90 
Luria , M. , C. C. Van Valin, D. L. Vie II man , and R. F. Pueschel, 1986. Contribution of Gulf area natural sulfur to the North American sulfur budget . Environmental Science and Technology 20 :91-95. 

Pinn i ck , R. G. , and H. S. Auve rmann , 1979 . Response characteristics of 

Knollenberg light-scattering aerosol counters . Journal of the Atmospheric 

Sciences 10 :55-74 . 

Reisinger , L. M., and T. L. Crawford , 1980. Sulfate flux through the 

Tennessee Valley region . Journal of the Air Pollution Control Association 

30: 1230-1231 . 

Schotz , S., and H. A. Panofsky , 1980. Wind characterstics at the Boulder 

Atmospheric Observatory . Boundary-Layer Meteorology 19 : 155- 164 . 

Siever"ing , H. , 1982 . Profile measurements of particle dry deposition veloc i ty 

at an air-land interface . Atmospheri c Environment 16 :301-306. 

Sievering, H., 1986 . Gradient measurements of sulfur and soil mass dry 

deposition rates under clean air and high-wind-speed conditions. 

Atmospheric Environment 20 :341-345. 

Whelpdale , D. M., T. B. Low, and R. G. Kolomeychuk , 1984 Advection 

climatology for the East Coast of North America. Atmospheric Environment 

18 :1311-1327 . 

91 
8. DIRECTOR'S OFFICE 

8.l Alkaline Aerosols 

IMPACT OF ALKALINE AEROSOL ON PRECIPITATION CHEfllSTRY 

It has been demonstrated that natural sources of alkaline material can have 

a significant effect on the chemistry of precipitation. Soil particles are 

often alkaline, particularly in the Western United Sta t es. These particles may 

act to neutralize the acidity of precipitation caused by pollutants such as the 

sulfur and nitrogen species produced by burning of fossil fuels in industrial 

plants and automobiles. The Alkaline Aerosol Project is concerned with estimating fluxes of alkaline aerosols and investigating their chemical properties. 

A goal of the project is to estimate, by region and on a monthly basis, the 

total atmospheric input of suspended soluble alkaline aerosol that ha s neutralizing potential fo r precipitation. The importance of the l-mon temporal scale 

and regional spatial seale is that alkaline source material is plentiful in some 

regions, par-ticularly in the Western United States, during some months but is 

not plentiful in other regions or possibly during other months. Source mechanisms such as wind erosion, dust devils, and vehicles traveling on unpaved roads 

are quite different and lead to differing temporal and spatial aerosol input. 

The sou r ce mechanisms for alkaline aerosol production may have seasonal maxima 

that should be included in models that consider neutralizing effects of alkaline 

aerosols. Solubility and neutralizing potential must be known along with mass 

input of suspendable alkaline aerosol to calculate the effect on acid precipitation. 

The Alkaline Aerosol Project is divided into efforts to assess the total 

input of aerosols from the various mechanisms of soil particle emissions and to 

analyze their c hemical properties. Work on the input by wind erosion is taking 

place in GMCC under the direction of D.A. Gillette, work on the input by 

vehicles traveling on unpaved roads is taking place at the University of 

Illinois under the direction of G. Stensland, and work on dust devil emissions 

is taking place at Colorado State University by P. Sinclair. Stensland is also 

leading the effort to chemically characterize the soil particles emitted by the 

above source mechanisms. 

Previous estimates of emissions of dust by wind erosion and by vehir.les traveling on unpaved roads have been shown to be too large when compared with 

a~tual depOSition of soluble alkaline particles. New methods are being developed in GMCC to estimate these inputs. For example, the National Resource 

Inventory (NRI) survey of U.S. farms and soils will be used along with l4 years 

of wind data recently compiled as the Wind Energy Resource Information System 

(WERIS). The fundamental approach of the dust emission studies will be to use 

an expectation integral 

E J g(V)p(V) dV 

V o 

92 
UNITED STATES ANNUAL AVERAGE WINO POWER 

" - . 

'\ ,or \ 

, ( 

Figure 1. --Wind energy in the United States. 

of Battelle, Pacific Northwest Laboratories.) 

shading indicates greatest wind energy. 

(Hap courtesy 

Da rke s t 

where g(V) is the dust flux for a given wind speed V, p(V) is the probability 

density function of the wind speed, and V is the threshold value of the wind 

speed at which dust emissions begin. Since this approach has similarities with 

wind energy mapping , it is instructive to see that the areas of maximum wind 

energy correspond to historical areas of severe dust production. 

Figure 1 shows that areas of maximum wind energy center on the Panhandle of 

Oklahoma. The areas of maximum land damage for 1935-1936 also center on the 

Panhandle of Oklahoma (see fig. 2.) The areas of maximum land damage for the 

drought of the 1950 ' s occurred in the high plains too, but because of land use 

differences the location was slightly different from that of the 1930's drought. 

Figure 2.--The general boundaries of the "Dust 

Bowl " from 1935-1936 (solid line). The region 

marked by slanting li.n2s received the most 

severe wind erosion. (Information from Hurt, 

1981.) 

93 
Chemically, some properties of the alkaline aerosols have been investigated 

by t he University of Illinois team. They have shown that alkaline elements 

increase in solubili ty with time and dilution ratio (mass of water to mass of 

solids). Since they have shown that dilution ra tio is typically on the order of 

100,000 to 200 ,000, it follows that alka line elements should be quite solub le in 

rainwater. That result was confirmed in samples of natural rainwater. 

A schematic diagram of the approach that the Alkaline Aerosol Project team 

is taking to estimate the neutralizing ef f ect of airborne alkaline aerosols is 

shown in Table 1. First, emiss ion factors from the three major sources of alkaline aerosols are grouped into the top level. Second, the fractio n of the total 

alkaline aerosol produced that is s uspe nded fo r t imes long enough to interac_t 

wi th acid precipitation must be estimat ed from knowledge of settling rates and 

atmospheric turbulence. Third, the f raction of the aerosols that is alkaline 

must then be found from knowledge of fractionation of air borne material from 

parent mate rial and composition of parent material. Fourth, the soluble fraction of the alkaline elements in the aerosols must be found. Finally, the 

neutralizing potential of t he soluble suspended alkaline materia l must be found. 

Each of these individual components is being researched by the project. 

Table 1. Alkaline aerosol fl ux estimations to be made by the Alkaline Ae rosol 

Project and methods for the estimation of the neutralization of acid rain* 

----------------------------------------- __ ----'F=lux Es timate.. _______________ _ 

Emission factor X source area 

Fraction suspended dust (for long time/ 

distance) 

Elemental fractio n of suspended dust 

(fractionation X composition) 

Soluble fraction of elemental suspended dus t 

Neutralization fraction 

Hethods 

Expectat i on integrals, 

experimental threshold 

velocities; Road dust 

experimentation; dustdevil experimentat i on 

Vertical turbulence model 

Fractionati on experimentation; chemical s urvey of 

U.S. roads; USGS soil 

composition data 

Experimentation on 

solubi Hty 

* Each succeeding level is a fraction of the next higher level. 

REFERENCES 

!-lurt, R. D., 1981. The Duss. Bowl: An Agriculs.uraJ. and ~o_cial !-listol]C. 

Nelson-Hall Inc., Chicago , 540 pp. 

94 
INTRODUCTION 

PRECIPITATION CHEMISTRY 

R. s. Artz 

Air Resources Laboratory, NOAA 

Silver Spring, MD 20910 

Routine and special precipitation chemistry measurements continued at the 

four GMCC sites and at the regional sites. Specia l studies continued at MLO 

using the ion chromatograph for anion analysis for Samoa and the Hawaii network. 

A new Dionex ion chromatograph was purchased and sh ipped to the Mauna Loa 

Laboratory. Cation analysis should commence sometime during 1986. A cooperative project with the University of Virginia was instituted in order to measure 

organic acids in precipitation samples collected at Mauna Loa Observatory. 

BASELINE MEASUREMENTS 

The five -site special network on the island of Hawaii and a sixt h site on 

Kauai continued to operate on approximately a weekly schedule, with the exception of the Cape Kumukahi site. (Site locations are discussed in previous GMCC 

reports.) Problems with rust and corrosion of equipment coupled with relatively 

frequent power outages have resulted in the abandonment of the Kumukahi site. 

As seen in Fig. 1, high sulfate and hydrogen ion concentrations existed 

during the months of June, September, and December at the Hawaiian sites. These 

observations can be explained by the very low precipitation received at the 

effected sites (Figure 2) and are probably not due to anthropogenic or volcanic 

activity. Typically, concentration increases sharply as precipitation amount 

approaches zero. Agreement for sulfate and hydrogen ion at Halai Hill and 

Kauai, sites with similar elevation and orientation to the trade winds, was very 

good throughout the year although Halai Hill values, as frequently observed in 

the past, tended to be 5 to 10 ueq / l higher. 

In Fig. 3 monthly precipitation weighted S04= and H+ means for the Hawai ian 

sites are presented. As usual, highest sulfate values usually occur at lowest 

elevations (Kauai and Halai Hill) due to the incorporation of sulfate laden sea 

spray. Sites at higher elevations are frequently decoupled from the marine 

boundary layer and therefore contain less sulfate. In addition, higher H+ concentration (lowest pH) are typically observed at the highest elevations. H+ 

concentrations near sea level are lower. 

In Fig . 4 Samoa H+ and S04= monthly precipitation weighted means are presented. With the exception of August, values are very constant. Missing data 

during May, June and July are due to a change in the staff at Samoa . It is not 

known whether the high concentration of S04= in August is the result of problems 

associated with the program restart or if, in fact, the value is correct. 

Snow sample data for BRW and SPO are shown in Fig. 5. SPO samples are 

exceptionally clean and constant, s howing concentrations of less than 2 ueq / l of 

S04= and approximately 8 ueq / l of H+. Barrow values are somewhat more eratic 

but remain consistant with measurements from MLO and other background sites. 

Shipping problems resulted in the loss of measurements at BRW after August, 

1985. 

95 
MAUNA LOA OBSERVATORY 1985 

.~ 

.~ 

." $ I ! 

I I 

I ! ~ 

» ! 

• 

1221- ~-

KULANI MAUKA t 985 

.~ 

~ 

~ 

1 .» 

I ~ 

H' 

I I .~ 

I ~ 

» 

• 

» 

" 

1ZZl"· ~-

22 MILE SITE 1985 

~ 

1 • 

~ 

I ~ 

» 

• 

» 

» 

" 

IZ2l ~ "'" -

REGIONAL MEASUREMENTS 

HALAI HILL 1985 

~ 

~ 

» 

• 

» 

~ 

KAUAI 1985 

» 

" I! Ip- I~ 

, , I~ I~ I! I ~ I~~~! " . " , , ; " . 

Figure 1. --Monthly precipitation 

weighted means for five sites on 

the islands of Hawaii and Kauai 

during 1985. 

All thirteen of the NOAA NADP / NTN regional precipitation sites remained in 

operation during 1985. No new sites were added to the network although tentative plans exist to establish a second site near Meridian, MS in an effort to 

quantify any effects a local pressed-wood facility may have on the existing 

site. Proposed site start- up time has been scheduled for sometime during 1986. 

96 
HAWAIIAN MONTHLY PRECIPITATION DATA 

Figure 2.--Monthly precipitation 

at Hawaiian sites for 1985. 

HAWAIIAN MONTHLY HYDROGEN ION DATA 

'~~----------------------------, 

1 

! 

I 

• 

~ 

~ 

" 

Figure 3b.--Monthly precipi tation 

weighted hydrogen ion means for 

the Hawaiian network. 

BARROW 1985 

~ 

" 

" • 1 ~ 

! " 

I " 

" 

Irn~o . ; • IZ2l •• "'" -

~ 

" ! 

I 

HAWAIIAN MONTHLY SULFATE DATA 

• 

1 

I " 

"'" .. =-

Figure 3a.-- Monthly pre c ipitation 

weighted sulfate means for the 

Hawaiian network. 

CAPE MATATULA 1985 

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

1 

I 

1Z2I-. ~_ 

Figure 4 .--Monthly precipitation 

weighted sulfate and hydrogen ion 

means for Samoa during 1985. 

SOUTH POLE 1985 

" " " " 

" 

" " " " " " 

· · • 

: ~ • 

fl : I:'i l'I b1 k, b b k, 

. • . . . . • . " ; 

Figure 5.--Monthly average hydrogen ion and sulfate concentrations for 

snow sampl es collected in Barrow and at the South Pole for 1985. 

97 
8.2 Arctic Gas and Aerosol Sampling Program 

ARCTIC HAZE ABOVE THE BARROW BASELINE STATION 

R.C. Schnell 

Cooperative Institute for Research in Environmental Sciences 

Un i versity of Colorado, Boulder , CO 80309 

INTRODUCTION 

Analyses of data from the AGASP flights of March-April 1983 show that 

measurements of Arctic haze gas and aerosol concentrations at the surface are 

strongly influenced by the vertical temperature structure of the atmosphere. 

Under strong temperature inversion conditions, the stable Arctic boundary 

layer reduces mixing from aloft to the surface. Under these conditions , gas 

and aerosol concentrations measured aloft are hi gher than and peak-to-peak 

variations greater than those measured at the surface . Under stable 

atmospheric conditions, ozone is depleted within the boundary layer. A 

combined sur face and airborne study for the Barrow station for 9-19 March 1983 

is presented below. 

BARROW SYNOPTIC CONDITIONS , 9-19 MARCH 1983 

The surface pressure distribution over this region of the Arctic on 12 

March 1983, 0000 GMT, was dominated by a large anticyclone (high-pressure 

area) located over the East Siberian Sea, a cycl one (low-pressure area) over 

the Canadian Archipelago , and a cyclone over the Gulf of Alaska. Organized 

air flow from Eurasia entered the Beaufort Sea area via the Canadian sector 

and crossed central Alaska on its way southward . Both the anticyclone and 

cyclone were developed as well at 500 mb . By 0000 GMT on 18 March 1983 , the 

anticyclone had moved north and east of Barrow shielding Barrow from haze 

transport . 

The occurrence of Arctic haze in the vicinity of Barrow during this 

period has been associated with well-organized transport of pollutants from 

Eurasia across the Pole into the Alaskan Arctic (Raatz , 1984). The pollutants 

from Eurasia were injected northward on 4-5 March (Raatz , 1984) reached 

Svalbard on 7-8 March (Ottar and Pacyna , 1984; Iversen , 1984) , and according 

to air mass trajectories, arrived over the Alaskan Arctic on 11-12 March 

(Harris , 1984) . By 17-18 March , haze was not observed either at the surface 

or above and upwind of Barrow. 

AIR MASS TYPE AND SURFACE MEASUREMENTS 

Cross sections of potential temperature and water vapor mixing ratio for 

9-19 March are presented in fig. 1. The cross sections are based upon the 

0000 GMT radiosonde data . The tropopause (as determined by the top of the 

isothermal temperature layer) and the top of the very stable surface boundary 

layer are indicated by dotted lines. 

98 
On the basis of temperature, pressure, moisture , and trajectory analyses , 

it has been determined that the air at Barrow was of marine Pacific cold (mPK) 

origins, 9-10 March; of continental Arctic cold (cAK) origins, 11-12 March; of 

continental Arctic warm (cAW) origins, 12-18 March;, and of marine Pacific 

warm (mPW) origins 18-20 March. These air mass designations are shown in fig. 

1. 

A time series of surface measurements of ozone, CO" aerosol scattering 

extinction coefficient 0sg' aerosol concentration in the 0 .24 -0 .84 ~ range, 

and CN concentration (cm ) is presented in fig. 2. From these data it may be 

observed that there are distinct changes over time in both the gas and aerosol 

characteristics observed at the Barrow station in concert with the air mass 

changes. 

On 13-14 March extensive aircraft measurements were conducted above and 

upwind of the Barrow station in order to determine the vertical and horizontal 

variability of the haze and to relate these measurements to the surface 

record . These measurements are presented in fig . 3 in latitude-altitude cross 

sections of aerosol backscatter, relative humidity (r.h.) , CN concentrations, 

and ozone partial pressure as measured by the aircraft. Individual latitudeconcentration series were obtained while the aircraft was flying at a constant 

pressure level . 

As shown in fig . 3, at 1010 mb and 60 km upwind of Barrow (Barrow 

experienced a surface pressure of 1026 mb), a high a of 60 x 10-· m-' was 

recorded. It decreased rapidly to 25 x 10-· m-' nor~g of this peak and then 

stabilized at 30 x ~O-· m-', which is slightly greater than the average as 

values of 27.8 x 10 • observed at Barrow during this day. At intermediateP 

pressure levels (780 mb), the range of asp values was (10 to 30) x 10-· m-', 

and asp exhibited an abrupt decrease near 73°N. Above 705 mb, asp values 

became lower with increasing altitude , as was observed in all the vertical 

profiles of asp (Schnell and Raatz, 1984). 

The cross section of r.h. suggests that within the surface boundary layer 

the variations in extinction were not related to variations in r .h. , which was 

constant in the 65-75% range . This was also the case at the surface (Bodhaine 

et al ., 1984) . At the 780-mb level , however, asp and r.h. appeared to 

correlate , with dry air having lower asp values than moist air . 

CN concentration varied between 70 and 1000 cm-', with peak 

concentrations of 1000 cm-' observed at all but the highest (670-mb) flight 

level. Within the surface boundary layer , the peak in CN concentration 

occurring at 71 .6°N correlated well with the increased o~p values. On the 

other hand, at the same level north of 73°N , a peak in CN concentration was 

associated with decreased Osg'_ The background average CN concentration in 

the 1010 mb flight leg (220 m ') was lower than the Barrow background average 

CN values of 315 cm-' on this day , but is in excellent agreement with the 

Barrow background average CN value of 225 cm-' the following day . At the 

intermediate level (780 mb) north of 73°N, dry and less turbid air was 

associated with lower CN counts. At upper levels, changes in CN 

concentrations over space changed by large factors but in no discernible 

relationship to as and r.h. Ozone partial pressures were in the normal 20-

35 nb background r~nge observed at Barrow in the spring and exhibited little 

variation horizontally. 

99 
:0-

S. 

w 

a: 

::J 

(/) 

(/) 

w 

a: 6ooi:2BO/ 

0.. 

9 10 11 

soo r 

r 

r 

:0- r 

E : - 600 20 I 

W ' 

a: ' 

~: .ij: r 

1000 20 

12 13 14 15 16 

9 10 11 12 13 14 15 16 

mPK : cAK : cAW 

17 18 19 

, X 10-2g/kg r 

r 

, 

, 

r 

cjO 20 

" 60 

80 

HlO 

('20 

2.'20 , 

" 17 18 19 r 

1 mPW 

Figure 1.--Time-height cross section 

of potential temperature (K) (top) 

and water vapor mixing ratio 

(x 10-' g kg-I) (bottom) at Barrow , 

9-19 March 1983 . The tropopause in 

the 300-350 mb level and the top of 

the stable surface boundary layer in 

the 725-900 mb level are indicated by 

dotted lines . The different air 

masses present over the time period 

are presented by marine Pacific cold 

(mPK) , continental Arctic cold (cAK) , cont inental Arctic warm (cAW) , and 

marine Pacific warm (mPW). 

100 

35 

30 :0 

S 

6 

;:: 

« 

~ z 

w 

u 

6 

u 

E 

.9: 

25 

20 

15 

10 

5 

Z 35 1 

o 

~ a: 

~ 349 

w 

u 

z 

o 

r r 

OZONE : 

u 347 

6~~~~~~~~~ 

'E 

~ 

'0 

~ 

4 

2 

IE 150 

M"-

' E 50 I-:--;-~-" u 

900 

10 11 12 13 14 15 16 17 18 19 

MARCH 1983 

Figure 2.--Time series of ozone 

partial pressure , CO, concentration , aerosol scattering extinc- tion coefficient , aerosol particle 

number, and CN concentration at 

Barrow, 9-19 March 1983 . 
w 

0 

:::J 

'= >:; 

<l: 

w 

0 

:::J 

f5 

<l: 

LIGHT SCATTERING 

(OSp x 10 - 6 m -') 

MARCH 13/14. 1983 

30- P;: 670mb 10~ ~ 

300 P =700-740mb 

10-~ 40· 

20 -

~80mb 

70-

50;~ P=1010mb 

30~ '-

CN CONCENTRATION (em-' ) 

MARCH 13/14 , 1983 

500 ' 

P = 670 mb 200 ~~ 

100 -

1000~0 500 ""\ P=700-740mb 

1000 500r ~mb 

2001 

SOOr P;: 1010 mb 10001 (\ 

200~ 1001 

71 73 

LATITUDE (N) 

75 

RELATIVE HUMIDITY (%) 

MARCH 13/14, 1983 

P;: 670mb 

50 · 

100 · ~ 

w 

0 50 -J P= 700-740mb 

:::J 

f5 100~ 50 -1. P = 780mb 

<l: 1 

l00~ 

50 1 P =1010mb , 

OZONE CONCENTRATION (nb) 

MARCH 13/14. 1983 

I P;: 670mb 50 · 

I 0 ' 

50 I-_P=700-740mb 

§i -~ 

50 · 

~ 

P = 780mb 

<l: 0 

50 - P= 1010mb 

L--~-

71 73 75 

LATITUDE (N) 

Figure 3.--Latitude-altitude cross sections of (a) aerosol scattering 

extinction coefficient (10- 6 m-'), (b) relative humidity (%) , (c) CN 

concentration (cm-'), and (d) ozone concentration (nb), 13-14 March 1983 . 

The examples presented in fig. 3 are typical of the results from two 

other flight days (11-12 March and 15-16 March) when the aircraft flew similar 

patterns upwind and above the Barrow station. 

As noted earlier, Barrow was under the i nfluence of four different air 

masses (mPK , cAK, cAW and mPW) over the 9-19 March period (fig. 1). These 

changes in meteorological air mass characteristics were reflected in the 

surface measurements of CN, aerosol size and number distributions, asp values, 

and C02 concentrations and ozone partial pressures logged by 6-24 hours. Each 

air mass contained distinct characteristics in the concentrations and ratios 

of all the constituent parameters. 

Comparison of the surface and aircraft aerosol and C02 data, shows that 

in the free atmosphere the data spans a broader range; i.e., the minima aloft 

are lower and the maxima are higher than the corresponding surface 

measurements. 

101 
Fo~ 13-14 Ma~ch , ai~bo~ne ozone measu~ements show that the atmosphe~e 

above the su~face contained an even and constant ozone dist~ibution, whe~eas 

the su~face ~eco~ds on this and othe~ days exhibited fluctuating ozone 

concent~atio . Du~ in g this time of yea~ the ozone chemist~y in the f~ee ai~ 

is appa~ently unimpo~tant (Levy et al ., 1985), but ozone will be ~emoved f~om 

the ai~ by dest~uction at the su~face of the g~ound (Galballyand Roy, 

1980) . Thus, the sho~t-te~m fluctuations in the su~face measu~ements p~obably 

~eflect changes in the ability of ozone-~ich ai~ f~om above to penet~ate to 

the su~face . 

CONCLUSIONS 

It is concluded that (1) t~oposphe~ic ai~ mass changes above the Ba~~ow 

GMCC site a~e detected at the su~face within a day; (2) the absolute concent~ations of gas and ae~osols in the midt~oposphe~e du~ing st~ong 

tempe~atu~e inve~sion situations a~e gene~ally g~eate~ than those measu~ed at 

the su~face ; and (3) the magnitude of the peak-to-peak va~iations in concent~at ons of gases and ae~osols measu~ed aloft tends to be g~eate~ than 

at the su~face , the~eby suggesting that the bounda~y laye~ may be p~oducing a 

damping effect on ae~osol pe~tu~bations measu~ed at the su~face. Thus, some 

caution is advised in ext~apolating that su~face A~tic haze measu~ements a~e 

being ~ep~esentative of the total t~oposphe~ic column. 

REFERENCES 

Bodhaine , B. A., E. G. Dutton, and J. J. DeLuisi, 1984. Su~face ae~osol 

measu~ements at Ba~~ow du~ing AGASP. Geophysical Resea~h Lette~s 

11: 377-380. 

Galbally , I. E., and C. R. Roy, 1980. Dest~uction of ozone at the ea~th s 

su~face. Qua~te~ly Jou~nal of the Royal Meteo~ological Society 106:599-620. 

Ha~~is, J. M., 1984. T~ajecto~ies du~ing AGASP. Geophysical Resea~ch Lette~s 

11 :457-460. 

Ive~sen, T., 1984. On the atmosphe~ic t~anspo~t of pollution to the A~ctic. 

Geophysical Resea~ch Lette~s 11 :457-460. 

Levy, H., J~. , J . D. Mahlmen, W. J. Moxim, and S. C. Liu , 1985. T~oposphe~ic 

ozone : The ~ole of t~anspo~t. Jou~ al of Geophysical Resea~ch 90(D2):3753-

3772. 

Otta~ , B. , and J. M. Pacyna , 1984. Sou~ces of Ni , Pb and Zn du~ing the A~tic 

episode in Ma~ch 1983. Geophysical Resea~ch Lette~s 11 : 441 -4 44 . 

Raatz, W. E., 1984. T~oposphe~ic ci~culation patte~ns du~ing the A~ctic Gas and Ae~osol Sampling P~og~am (AGASP) , Ma~ch/Ap~il 1983. Geophysical Resea~ch 

Lette~s 11 :449-452. 

Schnell, R. C., and W. E. Raatz, 1984. Ve~tical and ho~izontal cha~acte~ stics 

of A~ctic Haze du~ing AGASP: Alaskan ~ctic . Geophysical Resea~ch Lette~s 

11 : 369-372 . 

102 
INTRODUCTION 

8.3 Coope~ative P~ograms 

MONITORING FOR SULFUR DIOXIDE AND TOTAL 

SUSPENDED PARTICULATE AT MAUNA LOA OBSERVATORY 

Hen~y Yee , Wilf~ed Ching , and Richa~d Sasaki 

Hawaii State Depa~tment of Health 

Honolulu, HI 96813 

Sulfu~ dioxide (S02) and total suspended pa~ticulate (TSP) monito~ing 

we~e ~einstituted as a long-te~ study at MLO by the state of Hawaii at the ~equest of E.P.A . Region IX. The long-te~m t~ends in sulf~ dioxide and pa~ticulate (10 ~ diamete~ and smalle~) concent~ations will be studied to dete~mine the facto~s cont~ibuting to inc~eases obse~ved in the past. Also, 

the study will wo~k towa~ds dete~ining the atmosphe~ic lifetime of the pa~ticula~ gases and pa~ticulates, and the chemical composition of the othe~ 

pa~ticulates collected at the elevation of MLO . 

Table 1 and fig. 1 show the integ~ated concent~ations of 24-~ TSP and 

S02 fo~ samples collected at MLO in 1985 . 

C"l 

E 

--OJ 

::t 

1985 

802 • 

30 T8P 6 

20 

10 

o~~~~~~~~~~~~~~~ 

JJJ FFMMMAAMMMJJJ JJAAASSOQONNDDD 

11325618214~7~113256183012~517291022416U92131527 

Figu~e --Twenty-fou~-hou~ integ~ated concent~ations 

of TSP and S02 samples collected at MLO fo~ 1985. 

103 
Table 1.--Twenty-four-hour concentrations 

of TSP (hi-vol, gravimetric) and S02 

(pararosaniline method) at MLO (llg/m 3) 

TSP S02 

Jan 01 

13 0 0 

25 1 . ~ 

Feb 06 1 ~. 9 3.~ 

18 ~.3 0 

Mar 02 13.3 0 

1 ~ 1.0 0 

26 32. 8 0. 7 

Apr 07 3. 7 0. 8 

19 3.5 0 

May 01 2.3 0 

1 3 2.6 0.7 

25 2.5 0.8 

Jun 06 1.2 0. 8 

18 2.2 

30 1 . ~ 

Jul 12 6.9 0. 8 2~ ~.O 0.8 

Aug 05 ~.5 

17 3.2 1.4 

29 ~.6 3.1 

Sep 10 ~. 1 0 

22 0.8 0.8 

Oct O~ 0 0 

16 0 0 

28 2.3 2. 3 

Nov 09 3.1 1.5 

21 3.5 0 

Dec 03 3.1 ~.5 

1 5 2.0 3.0 

27 ~.7 

1 O~ 
THE GLO BAL PRECIPITATION CHENISTRY PROJECT 

W. C. Keene 

J. N. Galloway 

Department of Environmental Sciences 

University of Virginia , Charlottesville. VA 22903 

G. E. Likens 

Institute of Ecosystems Studies 

Cary Arboretum. Hillbrook. NY 12545 

INTRODUCTION 

J. H. Hiller 

Air Resources Laboratory 

NOAA. Silver Spring. HD 20910 

Anthropogenic emlssions of S02 and NO x have resulted in widespread 

acidification of precipitation and subsequent env~ronmental 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 does the long-distance transport of sulfur and nitrogen species 

influence the composition of precipitation in remote regions of the world? 

Th e Global Pr ec ipitation Chemi s try 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 et al •• 1982). an evaluation of the long distance 

transport of anthropogenic pollutants from North America to Bermuda (Jickells 

et al •• 1982; Church et al •• 1982). quantification of the importance of 

organic acidity in precipitation (Keene et al •• 1983; Keene and Galloway 

1984 a.b; 1985) an analysis of the influence of airmass source region on the 

composition of precipitation at remote locations (Galloway and Gaudry. 1984; 

Dayan et al. 1985) and a comparison between natural and anthropogenic 

components ln precipitation (Galloway et ai.. 1984). In this report we will 

summarize current research and review more recent contributions of the 

project. 

HATERIALS AND HETHODS 

Samples of precipitation are collected by event in scrupulously washed 

polyethylene containers. Immediately after collection. pH is measured. 

samples are treated CHC13 to prevent biological activity and aliquots are 

subsequently sent to the University of Virginia for analyses for major organic 

and inorganic chemical constituents. To-date we have analyzed approximately 

1700 samples of precipitation collected at 1 2 land-based sites and during 4 

oceanlC cruises. 

RESULTS AND DISCUSSION 

Seasalt Corrections in Marjne Precipjtation 

Differentiation of seasalt 

essential for m any studies of 

and non-seasalt (or 

m arlne aerosol and 

105 

excess) components is 

precipitation chemistry. 
Uncertainties in such calculations arise from (1) uncertainties in the composition of seawater. (2) analytical uncertainties. (3) the amount of dry deposited seasalt in samples. (4) the validity of assuming a purely marine source 

for the seasalt reference species. and (5) the validity of assuming no fractionation during or after production of seasalt aerosols. Keene et a1. (1986) 

assessed these uncertainties and. using the reduced major axis regression 

technique. evaluated these assumptions by analyzing the composition of 

precipitation at Amsterdam Island (38 0 5. 78 0 E) and at Bermuda (32 0 N. 65 0 W). 

Precipitation on Amsterdam Island contained significant excess concentrations 

of Na+ (2%) and Cl- (5%) relative to Hg2+ Indirect eVldence indicates that 

these departures from seawater ratios are probably not due to the influence of 

terrestrial material. Th e excess Cl- was sufficient to account for approximately 20% of free acidity. suggesting that scavenging of vapor phase H Cl may 

affect the acid-base chemistry of frecipitation at the site. Volume-weighted 

excess 50 4

2 - based on Na+ and Hg + differed by 11%. a nonnegligible source of 

bias in estimating the wet deposition of non-seasalt sulfur. Precipitation on 

Bermuda contained significant concentrations of locally derived alkali and 

alkaline earth metals. The influence of continental and non-seasalt marine 

sources on concentrations of excess S °

4

2 - was also evident. These observations suggest that assumptions involved in seasalt corrections are not always 

satisfied and that it is therefore necessary to evaluate individual data sets. 

using objective criteria. to select the appropriate reference species. 

Sources f.o..r. Qr~anjc A.c..i.d..s. in .the. Atmosphere 

H COO H (formic acid) and C H 3 COO H (acetic acid) are im portant chemical 

constituents of cloudwater and precipitation. but sources for these compounds 

in the atmosphere are at present unknown. The question of source of identification was addressed through the analysis of 465 samples of precipitation 

collected at 14 continental and marine locations around the world (Keene and 

Galloway. 1986). Continental precipitation during growing seasons contained. 

relative to marine precipitation and to continental precipitation during noogrowing seasons. higher absolute concentrations of organic acids and higher 

ratios of H COO T (H COO H aq + H C a a -) to C H 3 co aT (C H 3 COO H aq + C H 3 C 0 a -). The 

concentrations of HCOO T and CH 3 COO T in precipitation at most locations were 

also highly correlated. These results support the hypothesis that organic 

acidity in precipitation may originate with two m ajar sources, volatile vegetative constituents over continents and a second weaker source in both continental and marine regions. Henry's La w constants for H C 0 a H (5.6 x 103 H/atm) 

and CH 3COOH (8.8 x 103 H/atm) were derived from thermodynamic data and equilibrium vapor phase concentrations calculated from the aqueous phase measurements. Relative to the similar ratios of HCaO T to CH 3 COO, in the aqueous 

phase. differences in precipitation pH resulted in large reglonal differences 

in predicted equilibrium vapor phase concentrations. The mechanism by which 

proportionate concentrations of HCOO T and CH 3 COO T are maintained in the aqueous phase remains an open question. Comparisons between precipitation in 

impacted and remote regions indicate that. although possibly important near 

large popUlation and industrial centers. anthropogenic emissions are probably 

not major sources for organic acids in precipitation over broad geographic 

regions. 

ONGOING RESEARCH 

Research efforts which are currently underway within the GPCP include: 

o A reevaluation of processes controlling precipitation chemistry on 

Bermuda. 

106 
o Analysis of process controlling precipitation chemistry at Katherine. 

Australia and Amsterdam Island. Indian Ocean. 

o Comparison between the composition of precipitation in China, the 

United States. and remote regions. 

o An intercomparison of measurement systems for gaseous and particulate 

organic acids. 

Reference lill 

Church. T. H •• 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. Jonrnal m. ~eollhl'sjcal Research 87: 11013-11018. 

Dayan. U •• J. H. Hiller. W. 

meteorological analysis 

atmospheric Envjroom.ent. 19: 

C. Keene. and J. 

of precipitation 

651-657. 

N. Galloway. 

chemistry from 

1985. A 

Alaska. 

Galloway. J. N. and A. Gaudry. 1984. The chemistry of precipitation on 

Amsterdam Island. Indian Ocean. At.mosllheric Enyjronlll.e.nt 18: 2649-2656. 

Galloway. J. N .• G. E. Likens. W. C. Keene. and J. H. Hiller. 1982. The 

composition of precipitation 10 remote areas of the world. Journal.of 

~eOllhl'sical Research 87: 8771-8786. 

Galloway. J. N •• G. E. Likens. and H. E. Hawley. 1984. Acid prenp1tation: 

Natural versus anthropogenic com ponents. Science 226: 829-830. 

Jickells. T. C •• A. H. Knap. T. H. Church. J. N. Galloway. and J. H. Hiller. 

1982. Acid precipitation on Bermuda. Nat= 297: 55-56. 

Keene. W. C •• J. N. Galloway and D. H. Holden. Jr •• 1983. Neasurement of weak 

organic acidity in precipitation from remote areas of the world. Journal 

m. ~eollhl'sical Research 88: 5122-5130. 

Keene. W. C •• and J. N. Galloway. 1984a. A note on acid raw 1n an Amazon 

rainforest. J:cll.u.£ 36: 137-138. 

Keene. W. C. and J. N. Galloway. 1984b. Organic acidity in precipitation of 

North America. At.mosllheric Enyjronlll.e.nt 18: 2491-2497. 

Keene. W. C •• and J. N. Galloway. 1985. Gran's titrations: Inherent errors in 

in measuring the acidity of precipitation. MlIlosllheric .E;nyjronlll~ 19: 

199-202. 

Keene. W. C. and J. N. Galloway. 1986. Considerations regarding sources for 

formic and acetic acids in the troposphere. Jonrna1 m. ~eollhysjcal 

R esearch (und er review). 

Keene. W. C •• A. A. P. Pszenny. J. N. Galloway and N. E. Hawley. 1986. 

Sea-salt corrections and interpretation of constituent ratios in marine 

precipitation. Journal m. ~eollhl'sjcal Research 91: 6647-6658. 

107 
INTRODUCTION 

6C 13 IN ATMOSPHERIC CARBON DIOXIDE 

I~ving F~iedman, Jim Gleason , Augusta Wa~den 

U.S. Geological Su~vey 

Denve~ , CO 80225 

We have continued monitoring of the 6C 13 of atmospheric CO2. Samples 

were collected bi-weekly at South Pole, Mauna Loa , Samoa , and Point Barrow. 

EXPERIMENTAL 

The only change to the experimental procedure described in the previous 

Summary Repcrt (No. 13) has been the periodic analysis of the CO2 extracted 

from 10 L flasks filled from a high pressure tank containing Niwot Ridge 

air. The analysis of these samples assures that the CO2 extraction procedure, 

as well as the mass spectrometric analYSis , does not change with time. 

RESULTS 

The data for 1981 through August 1986 fo~ Mauna Loa, Samoa and Point 

Barrow are shown in figs . 1, 2, and 3. The data for the South Pole is given 

from 1981 through December 1985 in fig. 4. 

The line in figs. 1, 2, and 3 is the least square average of the data 

through 1984 . 

The data for Mauna Loa and Samoa in 1984 to the present shows less 

seasonal variation in 6C than for the previous 3 years, in contrast to Point 

Barrow where the seasonality appears unchanged for the entire 6 years. 

One explanation for the difference between the oceanic stations, Mauna 

Loa, Samoa, and Point Barrow, is the result of the 1983 El Nino, which would 

have influenced the ocean atmosphere 6C 13 exchange. 

108 
-8.5 

·8.4 

-8.3 MAUNA LOA 

-8 .2 

·8.1 

·8.0 

·7.9 

} ·7.8 

~ 

U 

~ 

·7.7 

·7.6 

·7.5 

·7.4 

·7.3 

7.2 

·71 

70 

1981 1982 1983 1984 1985 1986 1987 

YEARS 

Figure 1.--Record of 6C" in atmospheric CO2 at Mauna Loa . 

·8.5 

·8.4 

-8.3 SAMOA 

·82 

·8.1 

·8.0 

·7.9 

0 

* ·7.8 

~ 

u ·7.7 ~ 

·7.6 

-7.5 

-7.4 

·7.3 

·7.2 

·7.1 

·7.0 

1981 1982 1983 1984 1985 198' 198 7 

YEARS 

Figure 2.--Record of 6C l • in atmospheric CO2 at Samoa . 

109 
·8.S 

·8.4 

·8 .3 

·8.2 

·8.1 

·8.0 

·7 .9 

0 

;JI. ·7.8 

::' 

u ·7.7 ~ 

·7.6 

·7.5 

·7.4 

·7,3 POINT BARROW 

·7.2 

7.1 

·7.0 

1981 1984 1985 1986 1987 1982 

YEARS 

Figure 3.--Record of OC 'l in atmospheric CO2 at Point Barrow . 

".5 

-8.4 

·8.3 SOUTH POLE 

·8.2 

-8.1 

".0 

-7.9 

Be 13 'lb. 

-7.8 

-7.7 

·7.6 

-7.5 

-7.4 

-7.3 

-72 

-7.1 

-7.0 

1981 1984 1985 

YEARS 

Figure 4.--Record of OC 'l in atmospheric C02 at South Pole. 

11 0 
FOLLOWING THE TRAIL OF ANTARCTIC WINDS 

Eugene J. Mroz, Mohammed Alei, John H. Cappis, Paul R. Guthals, 

Allen S. Mason , and Donald J. Rokop 

Los Alamos National Laboratory 

Los Alamos, NM 87545 

The transport of tropospheric air masses from the north to the south (longitudinal 

transport) is responsible for bringing aerosols and trace gases to Antarctica from the 

lower latitudes. The atmospheric materials and pollutants from both natural and 

anthropogenic sources may then become part of the geological climatic record if they 

are trapped in the southern polar ice cap. If we are to use this record to evaluate the 

potential greenhouse and albedo effects of air pollutants on global climate, we need 

to understand the transport mechanisms involved. The Antarctic Tracer Experiment 

was designed to improve our scientific comprehension of these north-south transport 

processes by the use of unique atmospheric tracers. 

"Heavy" methanes were chosen to track the antarctic winds. These are the heavy 

isotopic analogues of methane-so named because they are composed of the heavy 

isotopes of carbon and hydrogen. We released specific amounts of 13CD4 and 12CD4 gas 

into the Antarctic atmosphere and subsequently conducted air and surface sampling in 

search of the tracer gas. Figure 1 shows the experimental concept and the location of 

the sampling stations. 

Sampling and mass spectrometric analysis techniques developed at Los Alamos 

can detect these tracers in quantities as small as a few parts in 1017 in air. Because 

of their extremely low natural abundance, their long atmospheric lifetime, and the 

high sensitivity for their detection, these isotopically unique methanes are ideal for 

experimentally tracking air masses in Antarctica over long periods of time and more 

than 4000 km from the release point. 

HEAVY METHANE 

TRACER GAS 

__~"'t"'!'::~,:'." NEW ~ _ i-

. ~ .. 

ZEALAND _ ~---:>_ 

----~~ . 

~'-.. ... <=> 

UROO " WE DOEll SEA 

ROSS SEA 

r:::...' '--~ ... - '-::;=-'-<::. 'r .- ~~7;(r.I(" '-- , '''~ IUSA I 

OU .... ONT IUSA I AJ,OI UNDSEN-SCOTT H~~~~Y o URVILLE SOUTH POLE IUS "'I ~-

FRANCE l '-r ~ -~" A TlANTIC OCEAN 

Jo"~1 .f 

CASEY 

AUSTR.t,U.l" • 

INOIA.N OCEAN 

Figure l.-Schematic showing the location of stations used for ground-based sampling of 

heavy methane tracers during the Antarctic Tracer Experiment. 

111 
Tracers were released between New Zealand and Antarctica in January, June, 

and October 1984. In January and June, 1 kg of 13CD4 was released by aircraft 

18 000 ft above sea level. In October, 20 kg of 12CD4 was discharged into the antarctic 

atmosphere 18 000 ft above sea level and was followed by 1 kg of 13CD4 at 5000 ft . 

Following each release, the network of ground-based sampling stations (shown in Fig. 1) 

was activated and air samples were collected for a period of 60 days. Although no 

above-ground air sampling was possible during the austral winter, we did collect samples 

by aircraft after the January and October releases. 

Detection of Heavy Methane Tracers in Antarctica 

By August 1985, all the samples collected in Antarctica were returned to Los 

Alamos for analysis. Before any samples were analyzed for the heavy methane tracers, 

we determined normal methane concentrations by gas chromatography with flame 

ionization detection. This step is necessary because the mass spectrometric analysis of 

the heavy methanes is normalized to methane in the sample to increase the precision of 

the procedure. For a number of the samples, we have observed higher t han anticipated 

levels of normal methane. We expected the concentration of methane in antarctic air to 

be ~1.65 ppm with little variability; however, a number of analyses have given. values 

exceeding 2 ppm. This poses no problem for the heavy methane tracer measurements, 

but it raises some interesting questions about our understanding of atmospheric methane 

sources and sinks in the southern hemisphere. We are evaluating these observations 

more carefully to determine whether the samples reflect local contamination, sampling, 

and/ or storage artifacts. 

In the aircraft-collected samples, the tracer was first observed over the Ross Ice 

Shelf ~26 h after the release. For the first week following the release, the tracer was 

observed in nearly every sample collected by aircraft over western Antarctica. However, 

the heavy methane tracer was not detected in the McMurdo surface samples, indicating 

that the tagged air parcel had not yet mixed down to the surface as the air passed over 

the edge of the continent. The tracer's very rapid transport to the continent from the 

point of release was unexpected. Meteorological trajectory analyses did not predict that 

this would occur. During the second and third weeks fo llowing the release, the frequency 

of positive samples declined, which suggests that the tracer was being transported out of 

the region. 

The first detection of tracer at the surface of the South Pole occurred 6 to 9 days 

after the release. During this 3-day period, the surface winds were blowing from the 

Weddell Sea sector. When this meteorological condition prevails, warm, moist, particleladen air from the open ocean in the Ross and/or Weddell Sea areas is blown over the 

polar plateau. These conditions frequently coincide with the breakdown of the inversion 

over the South Pole and the enhanced downward mixing from above the inversion layer 

to the surface. We believe that the tracer was carried down to the polar surface in this 

manner. After a travel time of about 10 days, tracer was detected at Halley Bay (UK) , 

which is located on the coast of the Weddell Sea. Analysis of several samples from 

the Palmer, Casey, Mawson, and Dumont D'Urville stations (collected after the last 

detection of tracer at Halley) have all been negative. 

112 
Atmospheric Dispersion of the Tracer 

One exc iting outcome of this experiment has been the confirmation of a 

theoretically predicted atmospheric dispersion process. For years, a number of 

atmospheric researchers throughout the world h ave been searching for evidence of a 

transition between the regime in which the dominant atmospheric dispersive process 

is three-dimensional turbulence and a regime dominated by quasi-two-dimensional 

circulation systems. These meteorological systems cause extensive distortion by 

stretching, contorting, and breaking t he tracer puff into a "lumpy" tracer plume. This 

distortion process effectively accelerates the rate at which atmospheric dispersion takes 

place because each "lump" then behaves as an independently dispersing puff of tracer. 

We expected that the transition between these two regimes of atmospheric 

dispersion would occur at travel times of ~ 100 to 200 h. Because the heavy methane 

tracers have a very high sensit ivity for detection, we were able to follow the tagged a ir 

masses in the Antarctic Tracer Experiment over this time scale and thus were able to 

compare experimental data with theory. Figure 2 is a plot of the tracer concentrations 

as a function of transport time. The data clearly indicate that there is an apparent 

increase in the tracer's r ate of dilution at times of 100 to 200 h (that is, increased slope). 

This, to the best of our knowledge, represents the first direct experimental confirmation 

of the transition between the three- and quasi-two-dimensional dispersion domains. 

0 10 15 i= « o~~ 0 

a: ~ 

'b---.. :J 

<.'J 

Z -3 \ 

x 

\~ Figure 2.-Heavy methane :;; 

w concentrations as a function of air 10 - 16 

z J.\ mass travel t imes are graphically « 

I l\ represented. The change in slope 

fw after 100- to 200-h travel time is the 

:;; L~ ~ first direct experimental indication of 

>- I I \ two dispersive regimes in the global > \ « troposphere. 10- 17 

W 

10 ' 10' 10' I 

TRAVEL TIME (h) 

11 3 
SOME RESULTS FROM UVB MEASUREMENTS AT MAUNA LOA AND ROCKVILLE,MD. 

INTRODUCTION 

Bernard Goldberg 

Smithsonian Institution 

12441 Parklawn Dr. 

Rockville, MD 20852 

The measurement of the UVB region of daylight (285nm-325nm) 

has been going on for some years at various sites around the worl d. 

One of the longest continuous records, other then the 

Berger-Robertson meters,has been that collected by the solar 

radition group at the Smithsonian Institution. This record contains 

data from Rockville, MD. ,Wallops Island, VA., Panama Canal, 

Tallahasee, FL., Barrow, AK., Mauna Loa in Hawaii. The longest 

record is that from Rockville, MD .. The data are in five nanometer 

bands centered around 290,295,300,305.310,315,320 and 325 

nanometers . These are nominal points that vary by + or - 1nrn. The 

band widths can also vary by the same amount. 

DATA COLLECTION 

The data are collected and recorded at one minute intervals 

from sunrise to sunset every day. Each of the one minute readings is 

the sum of seventy-two readings over the interval. The calibration 

of the instrument allows us to give the spectral band values in 

joules/square meter/nanometer. To make comparisons of the data over 

the year and from year to year a fixed solar secant value is used. 

This immediately detrends the variations due to geometry and time of 

day as well as the geographical location of the instrument. Because 

of the Rockville location we usually use a solar secant of 2 . 5 to 

accomadate all of the seasons. Ozone calculations are done at 

mid-day between 10 and 14 hrs. This allows us to use at least sixty 

values to determine a mean ozone value.A comparison with Dobson 

readings were made to check the data (fig.1). 

Satellite data are from the ERB experiment on Nimbus 7 and are 

taken from nine track tapes. Two of the channels are UV sensors. 

These are channels 8 and 9 with channel 8 covering from 300-4 10nm 

and 9 from 275-360nm. Every fourth day is missing because of the 

manner in which data are gathered. The daily value is derived from 

the average of about fourteen measurements . The data are received in 

engineering units (counts) and then converted into irradiance 

values. 

RESULTS 

The data from 1986 at Mauna Loa and Rockville, the only two 

sites now operational, had shown a major anomaly in February. There 

was a tremendous drop in the UVB irradiance. Because of the large 

amount of cloud cover at Rockville,the drop was noticed first in the 

Mauna Loa data (fig . 2). Using only the clear days at Rockville it 

was found that the drop there was the same as at Mauna Loa (fig . 3). 

Because the UVB is modulated by the ozone, a concomitant change in 

11 4 
ozone should have occurred. The expected change was found (fig.4). 

However,when looking for the reason for these sudden changes it was 

found that the ERB channels 8 and 9 showed the same drop in energy . 

The drop shown by the ERB channels was not the same order of 

magnitude. A spectral study showed that the change was greater at 

wavelengths more affected by ozone then those that are not absorbed 

by the ozone. 

f 

i 

• 

~ 

~ • " 

, 

~ 

~ 

! 

~ 

~ 

VARIABILITY IN ERB CHANNEL 8 

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

" 

,. 

71 

,. 

: VI '/-

: +----r------r-------.------'TV....----l 

o 20 00 

1986 TREND AT 305 NM AT W,UNA LOA 

n .. 

n12 

n, 

01111 

01111 ~ ~ 

n.o< 

lUll 

0 II -<l.O> 

-oDO 

-o.£J8 

\ Y -o.em 

-0.' 

-0. ' 2 

0 20 00 00 

11 5 

/ 

Fig.l. ERB data for the 

first 60 days in 1986. 

The drop in UV is very 

pronounced around day 40 

which is in February. 

Fig.2.The 305nm band was 

used to illustrate the 

drop in irradiance 

because it clearly shows 

the large percentage 

change due to the ozone 

change. The trend units 

are data at a solar 

secant 2.5 and are one 

minute readings. 
i 

• 

~ 

a 

I 

~ 

~ 

y 

~ 

~ 

u 

~ 

~ N 

0 

~ 

y 

~ 

~ 

i 

~ ~ 

305NM TREND AT ROCKVILLE ( 1986) ClUft Clll'S CJrU' 

0' 

0<» 

""" 

= 

D.OI 

"'" OD< 

om 

Q.aI 

aDO 

0 

-<>00 

-<Un 

-o.oJ 

-<ODO 

--<0.00 

r~' 

, 20 

OZONE VARIATIONS AT MAUNA LOA ...... ,- 0J1J 

0.00 

"'" OD< 

om 

no> 

aDO 

0 

-<l.o> 

-0.02 

~ -<>Jl3 

-OD< 

-<>£6 

-<l.OIO 

-001 

0 '" '" eo eo HI) ,., ,., "" "" 

OZONE VARIATIONS AT MAUNA LOA 

""" 001 

M . 

ad> 

OD< 

"'" Q.aI 

aDO 

0 

-<>.0> 

-0.02 

-o.oJ 

-QD< 

---<0.00 

-Ml 

-""" .. ~ .. ~ ." ... , .... .... ...... . fRIll DCl8!DN 'f'JU£S • 

11 6 

00 

Fig . 3. 305nm band trend 

at Rockville for clear 

days only . Values are 

the means of three one 

minute values around 

secant 2 . 5. 

Fig.4. This two part 

figure shows the ozone 

trends at Mauna Loa for 

1986 and since late 1984 

when the UVB istrument 

was put into place. The 

upper graph shows the 

increase during the 

month of February 1986 

while the bottom graph 

shows the comparison 

with the Dobson readings 

over a long period of 

time. 
LOGISTIC AND OTHER MODELS FOR THE TRENDS OF NITROUS OXIDE 

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

Institute of Atmospheric Sciences 

Oregon Graduate Center 

Beaverton, Oregon 97006 

Nitrous oxide (NzO) and other trace gases have been measured for more 

than a decade in both hemispheres. This record consists of average concentrations during every January at the South Pole. For comparison, similar measurements have been taken in the Pacific Northwest around 45° north latitude. The 

results for several trace gases, including CC1 3F, CClZFZ, CH", and NZO, were 

reported recently by Rasmussen and Khalil (1986). These trace gases are all 

increasing in the earthts atmosphere, probably because of increasing emissions 

from industrial and agricultural processes, and all have the potential for 

changing the earth's climate by adding to the greenhouse effect (Ramanathan 

et al., 1985). The effects of these trac e gases on the environment are directly related to the concentrations expected in the future. In this paper we 

discuss the consequences of various assumptions for extrapolating the trends 

into the future and apply the methods to nitrous oxide. 

The basic equations governing the behavior of a trace gas in the atmosphere are: 

dC/dt = S - nC 

dS/dt = f(S) 

S = Sa + Sn 

(1) 

(2) 

(3) 

where C is the average global concentration (here in ppbv) , S is the source 

(ppb/yr), and n is the inverse of the lifetime (1). Sa and Sn are the anthropogenic and natural components of the global emissions. For NzO, as for many 

other gases, the observed increase is probably related to increasing emissions 

from anthropogenic sources (Sa)' How these sources will increase in the future will determine the concentrations of N20 and hence its importance in 

changing the climate. We have compared four possibilities assuming that the 

natural sources Sn are constant. The first is simply to extrapolate the present rate of increase into the future, which does not require eqns. (1)-(3). 

The remaining possibilities are described in eqns. (4)-(6): 

f(Sa) = a 

f(Sa) = aSa 

f(Sa) = BSa(A - Sa) 

(4) 

(5) 

(6) 

where a, A, and B are constants and BA = a. The first two models are simple 

linear and exponential extrapolations of the present rates of increase of the 

sources. While these may be adequate for projecting changes over a few years, 

they have no limits to their increase. The model of eqn. (6) is perhaps the 

simplest limited growth model, and eqns. (3) and (6) form the logistic equation for the growth of sources (Khalil and Rasmussen, 1982a, 1982b, 1983). 

In the logistic model the ultimate anthropogenic source is limited to be A as 

t ... QQ. 

The solutions for the four cases mentioned above are: 

C = Co + b t 

C Sn" + Cle-nt + So"(l-e-nt) + a1 Z(nt-l)e-nt 

11 7 

Linear C (7) 

Linear S (8) 
S (9) 

Logistic S (10) 

where Cl is the present level of N20 contributed by human 

the present anthropogenic source, and T is the lifetime. 

parameters are given in Table 1. 

activities, So is 

The values of these 

Year 

1975 

1976 

1977 

1978 

1979 

1980 

Table l.--Concentrations of N20 between 1975 and 1985 and 

parameters for sources and sinks 

PNW (ppbv) SP (ppbv) Year PNW (ppbv) SP (ppbv) 

297 297 1981 304.3 305.0 

299 298 1982 306.8 305.4 

300.3 300.3 1983 306.7 306.5 

302.1 301.2 1984 306.2 306.5 

302.0 301.8 1985 307.3 307.5 

303.4 303.8 

Parameter s for sources and sinks 

S 

n 

2.78 

S (0) 

a (ppbv/yr) 

0.9 

A 

3 0.05 

T 

(yrs) 

100 

Cl 

(ppbv) 

15 

Notes: Contents of the table are based on Rasmussen & Khalil (1986) and 

Khalil & Rasmussen (1983). PNW denotes the Pacific Northwest representing 

the clean air of the mid-northern latitudes, and SP denotes the south pole. 

For some trace gases, such as N20, CH4, and C0 2 , the anthropogenic 

sources are related to production of food and energy, which are in turn related to the world population. Therefore, the rates of increase and the upper 

limits of the logistic equation may be set by the expected growths of population. We have used the estimates of world population from Erlich et al. 

(1977) to establish the limits of growth for the trace gases. These types of 

models and estimates have also been discussed earlier by Khalil and Rasmussen 

(1982a, 1982b, 1983) and applied to N20 and CH4. 

The results are shown in Figure 1. Fig. la shows the long-term behavior 

of the solutions. For shorter lived trace gases the features shown in this 

panel appear much sooner than for N20. The figure illustrates the speed with 

which different models allow for large buildups of trace gases. The limited 

growth in a logistic model is evident in the figure. For instance, the expec ted doubling time of concentrations for the models discussed is about 65 

years for the exponentially increasing sources, about 120 years for linearly 

increasing sources, and some 300 years for extrapolating the concentrations at 

present rates of growth. Since the logistic model has built-in limitations to 

growth, it does not predict a doubling of N20 ever. This is perhaps the most 

significant feature of logistic models in that they provide some assessment 

118 
> 

C 

Q 

Q 

C 

o 

~ 

• L 

~ 

C 

U • 

C 

o 

u 

> 

0 

Q 

Q 

c 

;: 

~ 

• L 

~ 

c 

• u 

C 

0 

u 

> 

0 

Q 

Q 

C 

0 

;; 

• L 

~ 

c 

• u 

c 

0 

u 

Nitrous Oxide Trends 

1000r------,,--------.~------~-------r-------, ! 

900 

.00 

700 

600 

500 

.00 

300 

200 

0 

600 

550 

500 

<50 

400 

350 

300 

250 

a: II 

: 

J//~-- /' i // 

: i/~ .. 

100 

b 

... 

200 

20~ , 70 1990 2010 

310 

309 C 

30B 

307 

306 

30. 

30. 

303 

302 

301 

300 

299 

297 

296 

29~ '" 1976 1978 

------------ .----

1980 

300 '00 

2030 2050 

Linear C 

---.- Linear 5 

.. __ ............. Exp 5 

----- Logistic S 

o NH 

• SH 

1982 1984 

500 

2070 

1986 

Time (ye ars) 

Figure 1.--Trends of N20 based on various models for extrapolating present 

concentrations and emissions. The methods considered are a linear 

extrapolation of present rates of growth of concentrations, linear and 

exponential increases of present anthropogenic emissions, and a logistic model 

for the growth of emissions. Figure 1a shows the overall behavior of the 

governing mass balance equations; Figure 1b is an expanded view over a 

century; Figure 1c is a view of N20 over the last decade. 

119 
of whether large atmospheric concentrations of trace gases are feasible. In 

other types of extrapolations any concentration can be achieved if sufficient 

time is allowed, even if these concentrations are unrealistic because they require anthropogenic emissions beyond our present expectations for the growth 

of population and industry. 

Fig. Ib shows extrapolations of the concentration of NzO over 100 years 

for the four cases mentioned above. Fig. lc is a blowup of the first decade 

showing more clearly the relationships between the data and the models. The 

results show that all the models can properly describe the available data 

from 1975 to 1985 . In the longer term the exponential solution (eqn. (5» 

quickly becomes unrealistically large. Of the other three methods, the simple 

extrapolation of the present rate of increase provides the lowest estimated 

concentrations in the future. This result is perhaps not expected for most 

other trace gases. It COmes about because the rate of growth of NZO is relatively slow, at about 0.3% per year, compared to other trace gases that are 

increasing at much faster rates. 

How the concentration of radiatively important trace gases is projected 

into the future has a substantial effect on the expected concentrations, which 

in turn determine whether the trace gas is likely to contribute significantly 

to global warming and climate change. Our results emphasize that physical 

models should be used to evaluate the expected increases of anthropogenic 

sources and the limits to their growth. 

REFERENCES 

Ehrlich, P. R., A. H. Ehrlich, and J. P. Holdren, 1977. Ecoscience. W. H. 

Freeman, San Francisco. 

Khalil, M. A. 

methane. 

K., and R. A. Rasmussen, 

Chemosphere 11:877-883. 

1982a. Secular trends of atmospheric 

Khalil, M. A. K., and R. A. Rasmussen, 1982b. Atmospheric methane (CH4): a 

review of current research. Proceedings, Second Symposium on the Composition of the Nonurban Troposphere, Boston, Massachusetts, May 25-28, 

1982, American Meteorological Society, 120-122. 

Khalil, M. A. K., and R. A. Rasmussen, 1983. 

nitrous oxide in the earth's atmosphere. 

Increase and seasonal cycles of 

Tellus 35B:161-169. 

Ramanathan, V., R. J. Cicerone, H. B. Singh, and J. T. Kiehl, 1985. Trace 

gas trends and their potential role in climate change. Journal of Geophysical Research 90:5547-5566. 

Rasmussen, R. A., and M. A. K. Khalil, 1986. Atmospheric trace gases: 

trends and distributions over the last decade. Science 232:1623-1624. 

120 
INTRODUCTION 

ATMOSPHERIC SUBMICRON PARTICLE COLLECTION 

AT THE SPO 

R. E. Witkowski and W. A. Cassidy 

University of Pittsburgh 

Pittsburgh, PA 15260 

G. W. Penney 

Carnegie -Mellon University 

Pittsburgh, PA 15213 

The electrostatic-type particle collector that was installed at the SPO 

CAF during the month of De cember , 1983, for the purpose of co llecting 

atmospheric submicron size particles, some of which may be of 

extraterrestrial origin, continues to operate successfully (Witkowski, et 

al., 1986). For the most part, only planned shutdowns of the device have 

occurred for routine specimen plate changes and, in one instance, for the 

replacement of the tungsten ionizer wire in the particle ionization chamber 

during October , 1985. In November, 1986, at the end of this current period 

of operation, more than 20,000 hours of collection time will have been 

logged with a total of 45 specimen plates being exposed. 

During this present season (January through November, 1986) an 

experimental set of nine specimen plates, fabricated from high density 

graphite, are being evaluated. This material, an alternate to stainless 

steel, was chosen in an effort to reduce fabrication time and costs, while 

at the same time reducing the total collector inventory of structural metals 

that offer sources of sample contamination. 

Single-particle characterization continues via scanning transmission 

electron microscopy (STEM) coupled with energy dispersive spectrometry (EDS) 

and selected area diffraction (SAD) measurements. At the present time, an 

automated STEM system is being evaluated for the purpose of providing a 

rapid method to survey scan the large number of specimen plates that have 

now been returned to the laboratory for study. 

RESULTS AND DISCUSSION 

Because this electrostatic pa~\icle collection technique employs a low 

air sampling velocity (300 ft min ) coupled with long sampling times (to 

4000 hours) and simple charged-particle attachment to a carbon-coated copper 

grid, the structure of very fine, delicate, submicron-size particles is 

preserved. It is felt that the delicate shapes of many of the collected 

particles may give clues as to their origin. Unlike impact-type collectors, 

no matting or fracturing of the collected material occurs, and no water 

~luble material is l ost as is the case with ice-core-type sampling-. -

In this search for particles of cosmic origin, the large contribution 

of sulfuric acid (or sulfate) droplets to the background, as shown in Figure 

1, continues to hinder STEM characterization of individual particles. These 

121 
droplets effloresce and immediately evaporate when the STEM electron beam 

impinges upon them. A number of rare particles that cannot be identified 

either as being of cosmic or terrestrial origin, which exhibit single 

element composition as measured by EDS, have been collected; some of these 

are illustrated in Figure 2. The source of these particles remains to be 

identified; they may be of artificial origin. Possible suggested sources 

may be from diesel heavy equipment or aircraft engine exhaust or even from 

earth-orbiting satellites (e.g. paint fragments) that have broken up or were 

destroyed in space (Marshall, 1985). Such a conclusion has obvious 

implications concerning contamination at the present site of the CAF. 

s cu 

Figure 1. - -STEM image and EDS spectrum generated from sulfur-rich droplets 

collected on specimen plate #8 after 168 hours of exposure. The Cu peaks 

noted in the EDS spectrum result from the copper grid material of the 

sampling system. 

FUTURE PROGRAM 

The major effort will be concentrated in the characterization of the 

particl es collected on the returned specimen plates; the automated STEM 

specimen plate scanning system may prove to be very valuable for the routine 

survey and identification of the many particles collected. Initially, the 

survey will concentrate on the search for particles containing the elements 

Mg, Si, Fe and Ni. In addition, the use of backscattered electron 

detection, as opposed to the collection of X-ray signals (EDS process) from 

individual particles, offers some hope in re lieving the sulfuric acid 

(sulfate) background problem while enhancing the ability to quickly identify 

particles or grains of interest. 

ACKNOWLEDGMENTS 

This continuing effort is part of the University of Pittsburgh 

Antarctic Search for Meteorites Project and is made possible through NSF 

Grant DPP 83 14496. We gratefully acknowledge the assistance of Mr. James 

Waddell, SPO CAF Station Chief, who maintained this experiment throughout 

the 1985 winter season. 

122 
;~ 

" 

~: TI :~ 

~~ lcu 

::; Ji\ 

................... w ................ ... ): 1.iL .............. ;;.; ..... ....... } t.}'::. .... .. 

I I 

n. l \lin Titanium 

• 

Cr 

Cu 

1 L.. 

I I 

0.2\l1ll Chromium 

Co 

Cu 

~s 

J ~\ ~ 

0.2 \llll Cobalt 

Figure 2.--STEM images and EDS spectra generated from rare particles 

collected on specimen plate #14 after 1032 hours of exposure. (Cu and S 

peaks from background.) 

REFERENCES 

Marshall, E., 1985. Space Junk Grows with Weapons Tests, Science, 

230:424-425. 

Witkowski, R. E., W. A. Cassidy and G. W. Penney, 1986. Atmospheric 

Submicron Particle Collection at the South Pole Observatory. GMCC 

Summary Report No. 13, February 1986, Everett C. Nickerson (Ed.) 

NOAA Environmental Research Laboratories, Boulder , CO, 102-103. 

123 
WASHOUT RATIOS OF NITRATE, NON-SEA-SALT SULFATE, AND SEASALT ON 

VIRGINIA KEY, FLORIDA, AND ON Al-IERICAN SAl-lOA 

Dennis L. Savoie, Joseph ~I. Prospero, and Ruby T. Nees 

Roscnstiel School of Marine and Atmospheric Science 

University of Miami, Miami, FL 33149-1098 

INTRODUCTION 

More precise estimates of the tluxes of ni trate and non-seasal t (NSS) 

sulfate to the ocean are required for a better understanding of the global 

atmospheric cycles of sulfur and nitrogen oxides. Estimates of deposition 

rates suggest that the washout of atmospheric aerosols by precipitation 

accounts for major portions of these fluxes . Because rainwater concentration 

data is sparse for marine areas, direct estimates of the wet flux are very 

uncertain. With precise estimates of the washout ratios, better estimates of 

the wet flux may be obtained from the relatively large data base which exists 

for the particulate concentrations of many constituents. 

Here, the washout ratios are defined as the ratio of the volume -weighted 

mean (V\'~!) concentration in rainwater (ug/kg rain) divided by the arithmetic 

mean concentration in the particulate phase (ug/kg air); to obtain 

dimensionle ss washout ratios based on conce ntrations per unit volume, multiply 

our values by 833. We use the V~I rather than any other parameter because it 

is the VW~I which, when multiplied by the total rainfall, yields a direct 

estimate of the total wet deposition. Estimates of the washout ratios of 

nitrate, non-seasalt (NSS) sulfate, and sodiulIl (seasalt) are presented for 

three marine locations: Virginia Key, Miami , Florida; American Samoa (14°5, 

171 oW); Bermuda (32 oN, bSoW). 

HATERIALS AND METHODS 

High vol ume bulk aerosol samples were collected by drawing atr through 

20x25 cm lVhatman-41 filters at volume flow rates of about 1. 2 m Imino To 

minimize contamination from local sources , the pumps (automatically controlled 

by wind sensors) were in operation only when the winds blew from the ocean at 

speeds of greater than 1 m/sec. Quarter sections of each filter were 

extracted with 20-ml of Milli-Q wat e r (Savoie and Prospera, 1982) . 

Rainwater samples were collected in using automatic wet-dry coll ectors 

similar to those used in the National Atmospheric Deposition Program (NADP). 

The rain was filtered, transferred to polyethylene bottles, and stored at SoC. 

Sulfate and nit r ate concentrations in the rainwater and f i lter extraction 

solutions were determined to +5% by ion chromatography. Sodium was determined 

to within ~2 % by atomic absorption spectroscopy (Savoie and Prospera , 19~2) . 

NSS sulfate concentrations were estimated by subtracting the seasa lt 

contribution (0.2517 x sodium) from the total sulfate concentrations. 

RESULTS 

To determine the washout ratios on Virginia Key, we have used the results 

from all of the 78 rainwater and 171 aerosol samples collected during calender 

year 1984. The results are summarized in Table 1. The i 984 rainwater data is 

124 
cons is tent with the means based on 

from Hay 1982 through April 1985. 

0 . 51 ug/ml for nitrate, 0 . 74 for NSS 

all of the available data (257 samples) 

The overall averages for that period are 

sulfate , and I.Y3 ror sodium. The annual 

mean washout ratios for nitrate and NSS sulfate are similar to one another . 

The washout ratio for sodium is nearly a factor of two higher. 

Table l.--Hean concentrations and washout ratios of sodium , nitrate, 

and NSS sulfate at Virginia Key, ~1iami ; American Samoa; and Bermuda 

SODlUN NITRATE NSS SULFATE 

VIRGINIA KEY Aerosol,ug/m 3 3. 7 1.9 2.1$ 

Rain,ug/ml 1.7 0 . 53 0 .69 

Washout ratio 550 320 L90 

ANERICAN SANDA Aerosol,ug/m 3 6.S 0.12 0.41 

Rain,ug/ml 2.83 u . ULZ-U.033 O. Db-U.1S3 

!.ashout ratio 520 220-330 4UO-450 

Geometric mean washout ratio 54U 300 350 

BERNUDA Aerosol ,ug/m 3 2.4 u.bl 0.91 

Rain , ug/ml 3. 9 0.25 0.64 

I.as hout ratio 1900 490 840 

For American Samoa, the average particulate concentrations were 

determined by us from 89 weekly samples collected from Harch 191$3 through 

April 1985 as part of the SEAREX South Pacific Aerosol Netwo rk (SEASPAN). The 

weekly rainwater concentrations for the period spanning the SEASPAN study were 

obtained from the NADP NTN database at Colorado State University. A range at 

values is given for the VWH's of both nitrate and NSS sulfate because most of 

the nitrate concentrations and a tew of the sulfate concentra tions were below 

the detection limit. 

For compa rati ve purposes, we have also estimated the washout ratios at 

Bermuda. However, these estimates must be used with caution. The aerosol and 

rainwater samples were collected during different periods and, thus, may not 

be directly comparable. Secondly, the particulate nitrate data at Bermuda was 

collected during a very small portion of a year. The annual V\~1 concentrations in rainwater at Bermuda have been reported by Keene ~ al. (1986). The 

results cover a period of almost two full years, n August 1982 to III Nay 

19l14, at the High Point site. This is the same si te used by Chen and Duce 

(1983) for the collection of aerosol samples from April to Uctober 1974; the 

mean NSS sulfate and sodium concentrations from that study are used tor the 

current washout estimates . The particulate nitrate concentrations are based 

on samples which we collected during August I Y82 and February 1983. 

125 
DISCUSSION 

For the two locations with long-term concurrent rainwater and aerosol 

data, Vi rginia Key and American Samoa, the mean washout ratios are very nearly 

equi valent to one another: about 300 to 400 for both nitrate and NSS s ulfate 

and about 500 for sodium. In comparison , those estimated fo r Bermuda are 

markedly higher: by about 50% for nitrate , about a factor of two for NSS 

sulfate, and nearly a factor of fou r for sodi um. It is still unclear how much 

of these differences are r eal and how much are actual l y related to the 

unce rtainties in the washout ratios at Be rmuda . A s ubstantially diffe rent 

mean meteorology during rain events at Be rmuda may well account for a major 

po rtion; however, what those diEference(s) might be is not at all clear. 

Until further investigations a r e co ndu cted to resolve the questj.on , we 

consider the washout ratios at American Samoa and Virginia Key to be most 

representative of ma r itime areas. 

On the basis of the variation in the above results and given sufticient 

ae r osol data, we s hould be able to estimate the wet deposition fl ux of nitrate 

and NSS sulfate to the ocean with an accuracy of well within a factor of two 

using the geometric mean of the washout ratios from Virginia Key and American 

Samoa . Considering t hese results, the flux of NSS sulfate to the ocean is 

probably conside rabl y less than that estimated by Varhe l yi and Gravenhorst 

(1983). To estimate the total sulfate concentrations in rainwater, they u sed 

a washout ratio of 180U.:!::600. This ratio appears to be about a factor of 3 too 

high even for sea-salt sulfate , ana it appears to be a factor ot 4 to 6 t oo 

high for NSS sulfate. A factor of four correction to the ir depOSition rates 

would hav e some major impli cations with regard to the inputs required to 

balance the sulfur budget of the marine atmosphere . 

Acknowledgments- We wish to thank Tom Snowdon , Nancy Douglas, R. Williams, D. 

Nelson, and the NOAA GNCC program. The work was supported by National Science 

Foundation g rants OCE-84-5609 and ATN-83-11335 . 

REFERENCES 

Chen, L., and R. A. Du ce , 1983. The sources of s ulf a t e , vanadium and mineral 

matt e r in ae ro sol parti c l es over Bermuda. Atmospheric Environment 

17: 2055 -2064 . 

Kee ne, W. C., A. A. P. Pszenny, J. N. Galloway, and N. E . Hawley, 1~ 8b . 

Sea-salt corrections and interpretation of constituent ratios in marine 

precipitation. J ournal E.!. Geophysical Kesearch 9 1:664 7-6658 . 

Savoie, D. L., and J. M. Prospe ro, 1982. Particle s i ze distribution of 

nitrate and s ulf ate in the marine atmosphere. Geophysical Research 

Le tte rs 9:1207-1210. 

Varhelyi, G., and G. Gravenhor st , 19 M] . Production rate of airbo rne sea-salt 

sulfur deduced from chemical analysis of marine aerosols and 

pr ecipitation. Journal E.!. Geophysical Research ~8:6737-6751 . 

126 
SEASONAL VARIATION OF 110Pb AND 'Be AT MAUNA LOA AND BARROW 

INTRODUCTION 

Richard Larsen and Herbert Feely 

USDOE Environmental Measurements Laboratory 

New York, New York 10014 

Air filter samples are routinely collected by GMCC personnel at BRW, 

MLO, SMO and SPO for the USDOE Surface Air Sampling Program . The primary 

objective of this program is to study the temporal and spatial distribution 

of specific natural and man-made radionuclides in the surface air. The 

concentrations of Z10Pb at MLO show a seasonal cycle and wide variations on 

a weekly time scale. At BRW the concentrations of both 110Pb and 'Be 

display seasonal cycles, and week to week variability. 

MATERIALS AND ~!ETHODS 

Hi-volume air filter samples are collected on a weekly basis using 

Microsorban filter material. The air samplers at MLO and BRW move about 1.0 

and 2.0 thousand cubic meters of air per day, respectively. through a 20 cm 

diameter filter. A section of each filter is compressed into a 1 to 2 cm' 

cylinder. and is analyzed by gamma-ray spectrometry using a high purity 

germanium (HPGe) detector with a 1.5 cm diameter well. A second section of 

each filter is composited on a monthly basis. The monthly composite is 

compressed into a 45 em] plastic planchet, and is analyzed for gamma- ray 

emitting nuclides using high resolution germanium detectors of either an 

n- type low energy coaxial or a Ge(Li) or HPGe p-type coaxial . Concentrations of the gamma-ray emitting nuclides are determined by computer 

resolution of the spectral data. 

RESULTS 

Figures 1 and 2 show the long term seasonal cycle and 

surface air concentrations, respectively, of 110Pb at MLO. 

analagous data for 110Pb are shown in Figures 3 and 4, and 

Figures 5 and 6. 

the weekly 

For BRW, 

for 'Be in 

The cumulative mean monthly surface air concentrations with one sigma 

errors are plotted in Figures 1, 3 and 5. The 210Pb monthly means represent 

about six years of measurements, while the 'Be monthly means represent about 

10 years . The weekly surface air concentrations of 210Pb and 'Be are 

reported for 1985 samples. There are gaps in the curves in Figures 2. 4 and 

6 because of missing data. 

DISCUSSION 

The surface air concentrations of 210Pb at ~~O show a seaso~al cycle, 

with the highest concentrations observed in April and May. The weekly 

concentrations of 210Pb show a pronounced episodic behavior throughout the 

year . Parrington et a!. (1983) reported that there is a spring peak in 

127 
J I F I MI AI MIJ 1 J I AI 510 I Nl o 

25 

30 MLO 

MLO .;;- 20 "'l-"'" 25 ~ 

~ 

.~ 

'> ~ 

BB~ ~ 

~ 20 0 15 

0 

~BBD~ ~ ~ g b 15 " 0 10 0 ~ 

~ • ~ 0 

10 13 ~ B " ~ ~ 5 

~ 5 " 

0 0 fEB APR JU N AUG OCT DEC 

Figure l.--Monthly u.Pb at MLO. Figure 2.--Weekly l10Pb at IILO 

during 1985. 

J1 F 1 MIA 1 M 1 J I J I A I 5 I 0 I N 10 

40 

40 BRW 

BRW .;;-

.;;- 35 ~ 

"- 30 ~ 

~~~B G "- 30 , ~ ~ 

0 ~ 25 

B~ ~ 0 ;; -2 20 

20 " J b 0 " ~ 

0 c ~ 15 0 ~ 

< 13 

B 13 10 ~ 10 

~ b 

~ 5 aaB 

;;; 

a 

0 0 

FEB APR JUN AUG OCT DEC 

Figure 3.--Monthly u·Pb at BRW. Figure 4.--Weekly 210Pb at BRW 

during 1985. 

200 J 

BRW ~ 120 

~ .;;-.:;- 100 

~ 150 

~ 

~BB8 ~ I ~ 80 ~ ~ 

~ ~ I 0 ~ 

88 8B8~ 100 ~ 60 g 0 0 " ~ 

0 ~ 

~ 40 0 

~ 

~ 50 13 ~ 

~ 20 i!" ~'" 

0 

8 ~ 0 DEC 

Figure 5.--Monthly 7Be at BRW. Figure 6.--Weekly 7Be at BRW 

during 1985. 

128 
aluminum concentrations in the aerosol at 

influx of dust from the Asian continent. 

be derived from the same source. 

~~O. and attributed it to the 

The "·Ph spring peak appears to 

The concentrations of 'Be and 210Pb at BRW reach a maximum during the 

late winter and early spring. At that time of year the troposheric 

circulation transports pollutants from mid-latitude continental regions into 

the polar regions. producing the Arctic haze layer (Lowenthal and Rahn. 

1985; Barrie. 1986). Figures 4 and 6 show the episodic nature of the 

surface air concentrations of 'Be and 210Pb within the seasonal cycle. 

Iverson and Joranger (1985), among others, observed similar episodic 

behavior of anthropogenic materials in the Norwegian Arctic. Summertime 

episodes of elevated concentrations of 'Be and 210Pb can be observed in 

Figures 4 and 6. Summertime episodes of 210 Pb in the Arctic were also 

described by Samuelsson et a1 . (1986). while Pacyna and Ottar (1985) 

described episodes of transport of crustal and anthropogenic mate rials into 

the Norwegian Arctic during the summer. 

The rate of emission of 122Rn , from which 21°Pb is derived, should be 

greater from the dry soils of the int erior Asian continent than from the 

moist soils of Europe. Thus 210Pb may be useful, in conjunction with other 

elements and compounds, as a tracer for air masses that enter the Arctic 

from off the central regions of the Asian continent . 

REFERENCES 

Barrie. L •• 1986. Arctic air pollution: An overview of current knowledge. 

Atmospheric Environment 20: 643-663. 

Iversen. T. and E. Joranger. 1985. Arctic air pollution and large scale 

atmospheric flows. Atmospheric Environment 19: 2099-2108. 

Lowenthal. D. and K. Rahn. 1985. Regional sources of pollution aerosol at 

Barrow. Alaska during winter 1979-80 as deduced from elemental tracers. 

Atmospheric Environment 19: 2011-2024. 

Pacyna. J. and B. Ottar. 1985. Transport 

summer aerosol in the Norwegian Arctic. 

2109-2120. 

and chemical composition of 

Atmospheric Environment 19: 

the 

Parrington . J .• W. Zollar and N. Aras. 1983. Asian dust: Seasonal transport 

to the Hawaiian Islands. Science 220: 195-197. 

Samuelsson. C .• L. Hallstadius . B. Persson. R. Hedvall and E. Holm. 1986. 

22lRn and 210Pb in the Arctic summer air. Journal of Environmental 

Radioactivity 3: 35-54. 

129 
RADIOACTIVITY AT BARROW AND MAUNA LOA FOLLOWING TBE CHERNOBYL ACCIDENT 

INTRODUCTION 

Richard Larsen and Z. Russell Juzdan 

USDOE Environmental Measurements Laboratory 

New York, New York 10014 

With the support of NOAA/GMCC daily air filter and bulk deposition 

samples were collected at BRW and MLO following the Chernobyl accident. 

Bulk deposition samples were also collected at the GMCC office located in 

Hila, Hawaii. These samples were analyzed by gamma-ray spectrometry to 

measure their content of fission products, such as 131 1 and 131CS, that are 

present in the Chernobyl debris . The debris sampled at these sites 

exhibited large differences in composition, and at BRW there were 

significant day to day variations. 

MATERIALS AND METBODS 

Hi-volume air filter samples were collected during May on a daily 

basis, whenever possible, at BRW and MLO using Microsorban filter material. 

Daily bulk deposition samples were collected at BRW and ~~O using plastic 

bag inserts in a 3 1/2 gallon plastic container having a 28.5 em diameter. 

At Hilo , plastic buckets were used to collect bulk samples. After every 

preCipitation event the bucket was sealed and sent to E~~, and a new 

bucket was exposed. Some of these deposition samples were composited for 

analysis. The air filters were placed into 45 em' plastic planchets and 

were analyzed for gamma-ray emitting radioisotopes using high resolution 

germanium detectors. The wet bulk samples were placed in 90 em] aluminum 

cans for gamma-ray counting. Samples that had large volumes and had 

specific activities that were too low to count were evaporated to 

90 em'. When the bulk sample contained no water, the plastic inserts were 

placed in Marinelli beakers and counted. None of the deposition samples 

contained 131 1 concentrations that were measurable without evaporation, and 

131 1 can be lost during evaporation. Thus no 131I deposition data are 

reported. 

RESULTS 

The surface air concentrations of 7Be, 131I, 134CS, 137C5 and 103Ru at 

BRW and MLO are presented in Tables 1 and 2, respectively. The deposition 

of 134CS, 137CS and 10lRu at MLO and Hilo are given in Tables 3 and 4, 

respectively. For all samples the radionuclides are corrected for decay to 

the mid-point of the collection period. 

DISCUSSION 

The data for the air filter samples in Tables 1 and 2 reveal that the 

Chernobyl debris intercepted at Barrow had a higher "'I/"'Cs ratio, and a 

lower '·'Ru/"'Cs ratio than the debris intercepted at Mauna Loa. 

130 
Collection 

Period 

5105 

5 /06 

5 /07 

5/08 

5/09 

5 111 

5 /1!. 

5 / 13 

5 / 1;. 

5 15 

Silo 

5/17 

5 / 18 

5/19 

5120 

5/21 

5/12 

5/23 

5/l.fo 

5/25 

5/26 

5 /06 

5 /0; 

5 /08 

5/09 

5 / II 

5/12 

5113 

5 i 14 

5/15 

5/1(> 

5 /17 

5/18 

5 /19 

5/20 

51! 1 

5 / 12 

5 /23 

5/1':' 

5/2 5 

5/26 

s/ll 

Table l .--Surface air concentrations at BRW 

Be 

3-+. 6 ;); 10 '1 

57.9 ::!: 80 

55.2 ± 9.1 

10... ± 11 

9':'.1 ± 0 . 1 

52 .... ± 9 5 

38 . 1 ± it. 

61.7::; 7 . 5 

29.8 

37.5 '" 

29.8 ± 

50 .3 ± 

':' 0 4 ::; 

50 2 ± 

57. 6 ± 

55 2 ± 

:'b . ± 

17.8 ± 

3) . 8 ± 

41. 9 ± 

-'+7.) ± 

. y 

.9 

12.0 

j. 

s. 

6 . 

s." 5.0 

]. . 7 

3.3 

3 .5 

1. 

(Femt()curiesiCubic ~~~t<,r) 

. ~ - 1 

< 19.0 

2).1 ± 10 .5 

17 5 ± 6. 

6) 8 ± 13.8 

46 ± 

32.6 ± . 2 

42 . 9 ± .~ 

23 . 6 :!: 1. 

.• 2 . ± 3. 

34.5 ± 

36. ± 

178 6 ± 

89.3 ± 

66 .1 ± 

57 .5 ± 

218. ± 

5~. ± 

57 .3 ± 

39.8 ± 

33. ± 

25 . 6 ± 

I. 

1.6 

. , 

5. 

4 . 0 

4 0 

6.6 

3. 0 

2.7 

2 . 0 

1.4 

1.0 

< 1.5 

< 0.8 

-.o"C5 

2 ± 0 .0 

. '1 U.8 

18 . 0 ± .-1 

18 6 ± 1. J 

9 . 5 ± 0 .7 

11.0 ;:: 09 

B 

o ± 0 .3 

. 6 ± 0 . 6 

4 .2±1.1 

. 0 0 .8 

6 . ± 0 . 7 

8. ± 0 .8 

7 .8± O.8 

0 . 0 :%; 0 . 8 

3 . 8 :l: 0 . 4 

4 .3 ± 0 . 4 

5.4 ± 0 . 4 

8 ± 0 .':' 

< 1. ') 

< I. 

1.6;:;0.7 

5.0 1. .. 

27.6 ± j 

25.4 ± l. 

19 '+ :%; 1 . 

1~ 2 ± 0 ') 

< 1 . 3 

8 2 ± 0 5 

6 . 6 ± 0 .8 

6 .3 ± 1.3 

7.0 ± 0 . 8 

1]. ± O. Y 

15 .5 ± . 0 

15 . 5 ± 1.0 

13.2 ± 0 . 8 

. 3 ± 0 . 6 

8 .8 ± 0 .5 

11.0 ± 0 5 

Ib . 8 ± 0 .5 

Air filter sample co11ect<!d using i] Brooks Roots system (S ASP pum.p) 

l<'ss than l' c'port<'d \'i]lue 

Error~ !·cp..:'rLcu r..;pr~s<'IlL two stand.lrd d<,\· j.:ltions of the t'ount il\ ~ ,..rror 

l;l.l:1K ~p'H':<'"' r..;prcsenl U<.It-l ...:.iltlli.nio'ls in pro,;x.css 

Table 2.--Surface air concentrati ons at ~~O 

(Femt ocu rie /Cub ic ~ieter) 

< 2 . 6 

l . 

- c':; Ru 

. 0 ± 1.8 

2.8 ± 0.0 

). '::I ± 0 b 

. b ::; O. 

8 . 1 0 8 

S . O. 

. 0 U. 

. 9 ± 0 

9 . 3 ± 0.5 

15 . 3 ± 0 .5 

Collection 

Period 

Be ':; "Cs cO 

- - Cs c, Ru 

5/01 

5 /02 

5 108 

5/09 

5 /12 

5 / 13 

5 / 14 

5 / 15 

5/ 16 

5 /21 

5 /22 

5 /2 3 

5 /27 

5 /2 8 

5 /2') 

5/30 

5 /02 

5 /05 

5 /09 

5 /12 

5 /13 

5 / 14 

5/15 

5116 

5 /19 

5 /2 2 

5 /2 3 

5 /27 

5 /2 8 

5 /29 

5j30 

6/02 

246.0 ± 16.1 

lt9.6 ::t: 8 . 3 

146 9 24 . 

165. 6 _ 6.2 

183.1 ± 18. 

308 8 25.4 

]0~ 2 ± 16 . 

113 2::t: 2 . 

35. ± . 0 

26 . 6 :t: . 2 

lJ5. :%; 9 . 7 

187 4 ± 3 5 

186 . ± 1:' . 0 

] 00 .8 ± 16.3 

125. ~:%; 5:. 

17').4 6 

< 5.3 

I. 

< 5.4 

1 . 1 ± 0 4 

< 4.0 

< 14 . 9 

< 12 . 1 

< 12 . 6 

12 .3±4.8 

10 .5 

. 6 ± .9 

. 4 ± 0 4 

19 . ± 3.3 

28 . 5 ... 3.3 

4.8 ± 1.3 

7 . ± 0 .4 

< 

< 

< 

< 

1.5 

o 6 

.j 

0 .5 

4. 9 ± 1. 

2 

I.l 

1.0 

. 6 

. 9 

< 0.7 

1. ± 0.2 

5 8 ± 1.0 

11.2 ± 1.6 

6 :t: 0 4 

. 9 _ 0 

< 

< 

< 

< 

l 

O. 

.1 

o 6 

. j 

3 .5:%; .3 

. 3 ± O. 

.8 ± ~ 

1.3 

2 . 3 

0 . 9 ± 0 5 

. 2 ± 0 2 

'l . Y ± 1.3 

2.2 . ') 1 .5 

5 . 2 ± 0 .5 

6 . O. 

1. O. <) 

.... 3 ::; O. 

24 . 9 ± 1. 8 

40.9 ± 2 . 0 

10.8±06 

15. 2 ± 0 .3 

Air filter sa~lple collected using a Brooks/ Roots Sy stem (SASP pump ) 

less than reported \'alue 

Errors reported represent twO standard deviations of lhe counting error 

Blank spaces represent da ta calculations in prOsress 

1 31 
Table 3.--Total deposition at MLO 

Coll~ction Precipitation "Cs C, ,c' Ru 

Period c:n ~Ci/;,,::t .;:C j , k.~::' mCi./K..!n~ 

; 0, - 5iL! 3.0 < 0.05 < 0.07 O.l~ 

5: L 5/10 u.O u . Ol 0.01 

5 f lO 5/27 0 . 0 < 0.01 

S! lJ Sj}.') 0.2 0.05 0.09 ± U.O'+ 0.10 

5/30 6/02 -0. 4 < 0 . 02 0.0) ± 0.u1 0.00 

Table 4.--Total deposition at Hilo 

Collection Pro,)cipitation -~.;. Cs c, .C Ru 

Period ct:! nCiLkm' rr:CiU_:n:: mCilb~ 

5/02 5 /09 U 0.02 U.O) , 0 . 0<) 

SIll 5 /16 2:.:' O. 17 ± 0. 01 O.]!j ± 0.0) 0.27 ± U. U8 

5/18 3/27 1.3 0.u5 ± 0.01 0.09 ± 0.02 O.l:' ± 0 . 07 

5/28 5i30 5. l 0 . 05 : 0 . 02 0.09 ± 0.03 < 0.18 

A similar pattern was observed by Uematsu (University of Rhode Island; 

personal communication, 1986) in surface air at Gambell, St. Lawrence 

Island and at Midway Island. At Barrow the '3'1 concentrations and the 

'3'I/'3'Cs ratios were especially high during May 17-18 and May 21-22. 

Uematsu observed periods of high 13'1 at Gambell during May 5-14 and May 20-

22. We have not observed this pattern at any of our other North American 

sites (Larsen et al .. 1986). Evidently the portions of the cloud of debris 

from Chernobyl that reached these Arctic sites were quite heterogeneous. 

At ~~O the concentrations of '3'1 were below or near our limits of 

detection during the first half of May. On the other hand, beginning by May 

10# Uematsu detected significant concentrations of 131I and 137CS at Oahu. 

Our deposition data for ~~O are consistent with our air filter measurements 

at that site, while our deposition data for Hilo are consistent with 

Uematsu's observations on Oahu . Evidently substantial portions of the 

Chernobyl cloud reached the Hawaiian Islands below the marine boundary layer 

by May 10, but only traces reached MLO, above the marine boundary layer 

before, May 16 . 

REFERENCE 

Larsen, R. J .. C. G. Sanderson, W. Rivera and M. Zamichieli, 1986. The 

characterization of radionuclides in North American and Hawaiian surface air 

and deposition following the Chernobyl accident. (Unpublished manuscript), 

100 pp. 

132 
EXPERIMENTAL SAMPLING Or ATMOSPHERIC METHANE 

Lester Machta , Kirby Hanson, Monte POindexter 

Air Resources Laboratory, NOAA 

Silver Spring, MD 20910 

An experimental program of continuous air sampling for atmospheric 

methane was begun at Virginia Key , rL in August 1985 , and at McMurdo Sound, 

Antarctica in November 1985. The air samplers are located at the AOML/ERLI 

NOAA Building on Virginia Key (4301 Rickenbacker Causeway, Miami) and in the 

Cosray Building at McMurdo Sound. During 1985 the equipment recovered 

discrete air samples over 24-hr periods. The feasibility of using cryogenic 

methods for extracing methane are being studied. Laboratory analysis of the 

samples for methane are planned . 

133 
9. INTERNATIONAL ACTIVITIES 

Du~ing Octobe~ 1985, the NOAA SRF absolute cavity ~adiomete~s we~e taken 

to Davos, Switze~land, fo~ pa~ticipation in the WMO-sponso~ed Sixth Inte~national Pyrheliomete~ Compa~ison (IPC VI). These compa~isons a~e held 

eve~y 5 yea~s and enable pa~ticipants to compa~e di~ectly with the wo~ld 

standa~d g~oup of ~adiomete~s. The WSG senso~s a~e used to maintain the WRR 

scale , and pa~ticipation by NOAA establishes a check of the pe~fo~mance of the 

SRF stand~ds and maintains t~aceability to the WRR. 

GMCC pe~sonnel continued to pa~ticipate in the HMO Global Ozone Resea~ch 

and Monito~ing P~oject to upgrade the quality of Dobson ozone spect~ophotomete~s th~oughout the wo~ld. Inst~ments calib~ated in 1985 we~e 

nos. 87 (Pe~u) and 41 (United Kingdom). 

A new ~ound of spect~ophotomete~ calib~ations in the global Dobson inst~ument station netwo~k was unde~taken in Ma~ch 1985 by means of t~aveling 

s tanda~d lamps. 

Plans we~e fo~mulated to conduct an inte~national compa~ison of Dobson 

ozone spect~ophotomete~s at ~osa, Switze~land in 1986. At least 12 count~ies 

a~e expected to pa~ticipate. 

Coope~ative Umkeh~ obse~vation p~og~ams with automated Dobson ozone spect~ophotomete~s continued in 1985 at Obse~vato~y Haute P~ovence, F~ance, 

and Pe~th, Aust~alia. 

R. G~ass and R. Evans visited Huancayo, Pe~, du~ing Septembe~ and 

Octobe~ 1985 to install automated Dobson ozone spect~ophotomete~ no. 87 fo~ 

ope~ation at the Huancayo Obse~vato~y. The Huancayo station is the sixth 

automated Dobson station to be installed by the NOAA GMCC g~oup and is one of 

seven global sites whe~e Umkeh~ obse~vations will be made on a long-te~ basis 

to monito~ possible futu~e st~atosphe~ic ozone depletion. 

E. Nicke~son se~ved on a thesis examining committee at the Unive~site de 

Cle~mont II , Cle~mont-Fe~~and, F~ance. Also while in F~ance, he assisted in 

completing ~evisions to a joint nume~ical modeling pape~ that was subsequently 

published in the Monthly Weathe~ Review. Du~ing the co~se of this visit (19-

26 Ma~ch) discussions we~e held on the p~oposed use of the NOAA/LAMP mesoscale 

air-quality model in a field expe~iment in Ge~many. 

R. Schnell was an invited speake~ at the week-long A~ctic Haze Policy and Resea~ch Planning Meeting, Camb~idge, UK, 2-6 Septembe~ 1985. At the meeting, 

plans fo~ the Second A~ctic Gas and Aerosol Sampling P~og~am (AGASP II) we~e 

discussed with pa~ticipants and E~opean collabo~ators. Following the 

meeting, Schnell spent 2 days in F~ance discussing a possible satellite- t~acked balloon A~ctic haze t~ace~ p~og~am with F~ench scientists f~om a 

va~iety of gove~nment and unive~sity g~oups. 

Du~ing 26-28 August, J. DeLuisi visited G. Fiocco at the Unive~sity of 

Rome to discuss the ~ole of the F~ascati lida~ in a wo~ld netwo~k. Data f~om 

the wo~ld lida~ netwo~k will be used to correct Umkehr observations of 

stratospheric ozone. Possible cooperative resea~ch p~ojects were discussed in 

134 
the context of the U.S.-Italy bilateral agreement, which was scheduled for 

renewal in the fall of 1985. The possibility of Italy placing a lidar in 

Antarctica was brought up because Italy plans to establish a research site on 

that continent. F. Congeduti , lidar expert from Frascati , visited GMCC to 

become familiar with our lidar program and work with the improvement of the 

analysis of raw lidar data. His visit was supported mainly by the Italian 

ministry of research. 

During 10-12 December, J. DeLuisi participated in a special WMO-sponsored 

workshop to organize a global lidar network intended to encourage research 

with modern lidar technology . Research areas in which modern lidar technology 

can make notable contributions in a networked system were suggested . Among 

these are aerosol vertical structure, ozone ground truth and relationships 

between ozone and atmospheric dynamics , atmospheric temperature structure up 

to the stratopause, aerosol corrections to satellite remote sensors , and cloud 

structure and dynamics. WMO will issue a special report on the workshop. 

In September , C. Mateer from the Canadian AES at Toronto was a scientific 

visitor at GMCC in Boulder. He worked on new ozone absorption coefficients 

for the Dobson instrument , and also worked on the aerosol correction to the 

Umkehr measurement. 

J. Pete rson and T. Conway participated in the conference Atmospheric 

Carbon Dioxide: Its Sources, Sinks, and Global Transport at Kandersteg, 

Switzerland , 2-6 September 1985. The papers "C02 Variability Between High 

Northern Latitude Sites," and "Recent Results from the NOAA/GMCC CO2 Flask 

Sampling Network" were presented by Peterson and Conway, respectively . 

In October 1985 , 24 glass flasks and a portable air-sampling unit were 

sent to T. Nakazawa of the Upper Atmosphere Research Laboratory , Tohoku 

University , Sendai, Japan . Air samples will be collected at Syowa Station 

(69.0 0S, 39.6°E), the Japanese Antarctic Research Program site . The GMCC 

flask sample CO2 measurements will be compared to in situ and flask CO2 

measurements made by the Japanese at Syowa during 1986. The flasks should 

arri ve in Boulder in early 1987. 

J. Peterson, P. Tans, and T. Conway attended the 2nd \oJMO Expert Meeting 

on Atmospheric Carbon Dioxide Measurement Techniques held at Lake Arrowhead, 

CA , 4-8 November 1985 . The meeting was attended by representatives from 

Australia , Canada , Federal Republic of Germany , France , Italy , New Zealand , People's Republic of China, Peru, Republic of Korea, Spain, the United States, 

and WMO. Discussion topics were CO2 standards and calibration techniques , field measurements and analytical techniques, reporting and publication of 

data , and recommendations. A summary of the discussions will be published as 

a WMO report. 

Collection of flask samples for CO2 and CH4 analyses was begun in June 

1985 at Alert, N.W.T . , Canada (82.5°N, b2.3°W) , in cooperation with N. 

Trivett, AES, Canada . Alert is now the northernmost sampling site in the GMCC 

flask sampling network. When AES begins in situ C02 and CH4 measurements at 

Alert , the GMCC flask data will provide an intercomparison of the GMCC and AES 

measurement and calibration systems. 

135 
J. Peterson attended the conference International Assessment of the Role 

of Carbon Dioxide and of other Greenhouse Gases in Climate Variations and 

Associated Impacts, held at Villach, Austria , 1-15 October 1985. The 

conference was sponsored by UNEP , WMO, and ICSU. The conference findings 

called on international governments to take into account the likely climate 

changes expected from increasing amounts of greenhouse gases when they develop 

policies on social and economic development, environmental programs, and 

control of emissions of radiatively active gases. 

An International Workshop on Sand Transport and Desertification in Arid 

Lands was held in Khartoum, Sudan , during the period 17-26 November 1985 . It 

was attended by GMCC scientist D. Gillette along with 81 scientists from Sudan 

and 61 scientists from 29 other countries. The workshop was sponsored by the 

International Centre for Theoretical Physics and several other international 

agencies. The purpose of the workshop was to examine , through detailed case 

studies, the flow of sand in arid regions of the earth . The program of the 

first 5 days consisted of 12 scientific sessions during which several case 

studies, review papers , and contributed papers were presented. Gillette 

presented the paper "A Physically Based Wind Erosion Estimation Method." 

Following the scientific sessions, Gillette participated in two working groups 

concerned with developing wind erosion and desertification studies. A field 

excursion was organized during the period 23-25 November to central Sudan to 

observe regional problems caused by wind erosion and wind-driven sand . 

At the invitation of the Soviet Union , B.G. Mendonca presented a paper on 

"Measurements in the Geophysical Monitoring for Climatic Change Division of 

NOAA, U.S.A. : A First Step 1n an Integrated Global Monitor-ing Effor-t " at the 

Third International Symposium on Integrated Global Monitoring of the State of 

the Biosphere. The conference was held in Tashkent , USSR, 13-20 October 1985 

and was sponsored by the USSR State Committee for Hydrometeorology and Control 

of the Natural Environment , the USSR Academy of Sciences, the Uzbek SSR 

Council of Ministers with the support of the United Nations Educational , Scientific , and Cultural Organization . This well-attended conference was the 

third in a series held every 4 years to discuss world problems in the area of 

pollution and the Earth's biosphere . 

136 
10. PUBLICATIONS AND PRESENTATIONS BY GMCC STAFF, 1985 

Boatman , J . F., and D. L. Wellman. The efficiency of an airborne cloud water 

separator. Proceedings , International Symposium on Moisture and Humidity, 

April 15-19 , 1985 , Washington , DC . 

Bodhaine, B. A. , and J . J . DeLuisi, 1985. An aerosol climatology of Samoa . ~ Atmos. Chern . 3:107-122 . 

Brainard, R. E. Geophysical Monitoring for Climatic Change, Amundsen-Scott 

South Pole Station , 1983-1984 . Ant. ~~~ XIX(5):202-203. 

Castillo, R., E. Patterson , and J. DeLuisi. Organic and elemental carbon 

loading in interstitial aerosol and hydrometeors, and its relationship to 

acidity of hydrometeors at a rural northeast site, Whiteface Mt ., NY. 

Paper presented at the IAMAP/IAPSO Joint Assembly , Honolulu, HI, 5-16 

August 1985 , 

Conway , T. J., W. E. Raatz, and R. H. Gammon . Airborne CO2 measurements in 

the Arctic duri ng spring 1983. Atmos. Environ. 19(12) :2195-2201. 

Conway, T. J . , L. S. Waterman, R. H. Gammon, and R. F. Weiss. Measurements of 

AtmospheriC CO2 from the AKADEMIK KOROLEV cruise, October-December 1983. 

Paper presented at the AGU Fall Meeting, San Francisco, CA, 8-13 December 

1985 . 

Conway , T. J ., L. S. Waterman , K. W. Thoning, and K. A. Masarie. Recent 

results from the NOAA/GMCC CO2 flask sampling network. Paper presented at 

the conference Atmospheric Carbon Dioxide : Its Sources , Sinks, and Global 

Transport, Kandersteg , Switzerland , 2-6 September 1985. 

Dayan , U., J. M. Miller , A. M. Yoshinaga, and D. W. Nelson . An assessment of 

precipitation chemistry measurements from the Global Trends Network and 

its predecessors (1972-1982) . NOAA Tech. Memo. ERL ARL-136, Boulder , CO, 

61 pp. 

DeLuisi, J., T. DeFoor, K. Coulson, and F. Fernald. Lidar observations of 

stratospheric aerosol over Mauna Loa Observatory: 1982-83. NOAA Data 

Report ERL ARL-5, Boulder, CO, 78 pp. 

DeLuisi , J. J. , E. G. Dutton, E. Flowers, and J. Peterson. Recent 

developments in atmospheric turbidity measurements in NOAA Geophysical 

Monitoring for Climatic Change. Lectures presented at the WMO Technical 

Conference on Observation of Atmospheri c Contaminants, TECOMAC, Vienna, 

Austria, 17- 21 October 1983 . WMO No . 64 , Spec . Environ. Rept. No. 16, 

World Meteorological Organization, Geneva, Switzerland. 381-386. 

DeLuisi , J . J . , E. G. Dutton, and B. G. Mendonca. Physical features of the EI 

Chichon stratospheric aerosol cloud over Mauna Loa. Paper presented at 

the IAMAP/IAPSO Joint Assembly , Honolulu , HI, 5-16 August 1985. 

137 
DeLuisi, J. J., C. L. Mateer , and P. K. Bhartia. On the correspondence 

between standard Umkehr, short Umkehr, and solar backscattered ultraviolet 

vertical ozone profiles. ~ Geophys . Res . 90(D2) :3845-3849. 

DeLuisi, J. J., C. L. Mateer, and W. D. Komhyr. Effects of the EI Chichon 

stratospheric aerosol cloud on Umkehr measurements at Mauna Loa , Hawaii. 

In Atmospheric Ozone. C. S. Zerefos and A. Ghazi (Eds. ), D. Reidel Publ . Co ., Boston, MA, 316-320. 

Dutton, E. G., J . J. DeLuisi, and A. P. Austring. Interpretation of Mauna Loa 

Atmospheric transmission relative to aerosols, using photometric 

precipitable water amounts. ~ Atmos . Chem. 3:53-68 . 

Dutton , E. G., J. J. DeLuisi, and D. J. Endres. Solar radiation at the 

Barrow, AK, GMCC baseline observatory 1976-1983 . NOAA DR ERL ARL-6, 

Boulder, CO , 112 pp. 

Fraser, P. J. , N. Derek , R. O' Brien , R. Shepherd, R. A. Rasmussen, A. J. 

Crawford , and L. P. Steele. Intercomparison of halocarbon and nitrous 

oxide measurements, 1976-1984. In Baseline Atmospheric Program 

(Australia) 1983- 1984 . R. J. Francey and B. W. Forgan (Eds. ) , Dept . of 

Science/Bureau of Meteorology , Aspendale, Australia , 17-26. 

Galloway , J., R. Pueschel , and R. Artz. Determination of the impact of North 

American emisSions on the atmosphere of the Western Atlantic Ocean. Paper 

presented at the AGU Fall Meeting, San Franciso , CA, 8-13 December 1985. 

Gendron, J. F., R. A. Feely, R. H. Gammon, B. A. Taft, P. E. Pullen, L. S. 

Waterman, and T. J. Conway. Distributions of chemical tracers in the 

eastern equatorial Pacific during and after the EI Nino-Southern 

Oscillation event . Paper presented at the AGU Fall Meeting , San 

Francisco, CA, 8-13 December 1985 . 

Grass, R. D. , and W. D. Komhyr. Traveling standard lamp calibration checks on 

Dobson ozone spectrophotomers during 1981-83. In Atmospheric .Ozone . C. S. Zerefos and A. Ghazi (Eds.) , D. Reidel Publ . Co. , Boston, MA, 376-380. 

Halter, B. C., J. M. Harris, and K. A. Rahn . carbon dioxide and Arctic haze aersols at 

19(12):2033-2037. 

A study of winter variability in 

Barrow, AK . Atmos. Environ., 

Hoecker, W. H., E. C. Flowers, and G. F. Cotton . Variation of direct beam 

solar radiation in the United States due to the EI Chichon debris cloud. 

Bull . Am. Meteorol. Soc. 66(1 ):14-19. --- ----

Komhyr, W. D. , R. H. Gammon, T. B. Harris, L. S. Waterman, T. J. Conway, W. R. 

Taylor , and K. W. Thoning . Global atmospheric CO2 distribution and 

variations from 1968-1982 NOAA/GMCC CO2 flask sample data. ~ Geophys. 

Res . 90(D3) :5567-5596. 

Komhyr, W. D. , R. D. Grass, R. D. Evans, R. K. Leonard, and G. M. Semeniuk. 

Umkehr observations with automated Dobson spectrophotometers. In 

Atmospheric Ozone. C. S. Zerefos, and A. Ghazi (Eds.), D. Reidel Publ. 

Co ., Boston, MA, 371-375 . 

138 
Oltmans , S. J. T~oposphe~ic ozone at fou~ ~emote obse~vato~ies . In Atmosphe~ic Ozone . C. S. Ze~efos and A. Ghazi (Eds.), D. Reidel Publ. 

Co., Boston , MA , 796-802 . 

Patte~son, E. M., R. A. Castillo, and J. J. DeLuisi. Cloud washout ~atios fo ~ 

g~aphitic ca bon at Whiteface Mt., NY. Pape~ p~esented at the IAMAP/IAPSO 

Joint Assembly, Honolulu , HI, 5-16 August 1985. 

Pete~son, J. T. Summa~y comments on the scientific highlights of the 

confe~ence. Lectu~es p~esented at the WMO Technical Confe~ence on Obse~vation of Atmosphe~ic Contaminants , TECOMAC, Vienna, Aust~ia, 17-21 Octobe~ 1983. WMO No . 64 , Spec. Envi~on . Rept. No. 16, Wo~ld 

Meteo~ological O~ganization , Geneva , Switze~land, xx-xxv. 

Pete~son, J . T. , and W. D. Komhy~ . Atmosphe~ic CO2 measu~ements at Ba~~ow, 

Alaska . Lectu~es p~esented at the WMO Technical Confe~ence on Obse~vation 

of Atmosphe~ic Contaminants , TECOMAC , Vienna , Aust~ia, 17-21 Octobe~ 

1983. WMO No. 64 , Spec. Envi~on . Rept. No. 16 , Wo~ld Meteo~ological 

O~ganization , Geneva , Switze~land, 76-80 . 

Pete~son, J. T., T. J . Co nway, and D. A. Gillette. CO2 va~iability between 

high no~the~n latitude sites. Pape~ p~esented at the confe~ence 

Atmosphe~ic Ca~bon Dioxide: Its Sources, Sinks, and Global T~anspo~t, 

Kande~steg, Switze~land , 2-6 Septembe~ 1985. 

Pollack , J. B., M. P. McCo~mick, E. G. Dutton, and J. J. DeLuisi. A 

climatology of the El Chichon volcanic cloud fo~ use in climate models. Pape~ p~esented at the IAMAP/IAPSO Joint Assembly , Honolulu , HI, 5-16 

August 1985 . 

Pueschel , R. F., D. L. Wellman, and J. F. Boatman. T~oposphe~ic ae~osols ove~ 

the este~n Atlantic: Scale height and ooncent~ations. Pape~ p~esented at 

the AGU Fall Meeting , San F~anciso , CA, 8-13 Decembe~ 1985. 

Raatz , W. E. Meteo~ological conditions ove~ Eu~asia and the A~ctic 

cont~ibuting to the March 1983 Arctic haze episode . Atmos . Envi~on . 

19(12) :2121-2126 . 

Raatz, W. E., R. C. Schnell, and B. A. Bodhaine. Atmosphe~ic c~oss sections 

fo~ the A~tic Gas and Ae~osol Sampling P~og~am , Ma~ch-Ap~il 1983. NOAA 

Tech. Memo. ERL ARL-134, Boulde~, CO, 50 pp. 

Raatz , W. E., R. C. Schnell , and B. A. Bodhaine . The dist~ibution and t~anspo~t of pollution ae~osols ove~ the No~wegian Arctic on 31 March and 

4 Ap~il 1983. Atmos. Envi~on . 19(12) :2135-2142. 

Raatz , W. E., R. C. Schnell, B. A. Bodhaine, and S. J . Oltmans. Obse~vations 

of A~ctic Haze du~i g pola~ fights f~om Alaska to No~way. Atmos. Envi~on. 

19(12) :2143-2151. 

Raatz, W. E., R. Gammon . Ai~ 

Ma~ch 1983 . 

C. Schnell , B. A. Bodhaine, S. J. Oltmans, and R. H. 

mass cha~acte~istics in the vicinity of Ba~~ow , Alaska, 

Atmos. Envi~on . 19(12):2127:2134. 

1 ~ 

9-19 
Komhy~ , W. D., T. B. Ha~~is, and L. S. Wate~man. Calib~ation of nondispersive 

inf~a~ed CO2 analyze~s with C02-in-ai~ refe~ence gases. ~ Atmos. Ocean. 

Technol . 2(1 ):82-88 . 

Komhy~, W. D., S. J. Oltmans, A. N. Chop~a , and P. R. Franchois. Pe~fo~mance 

cha~acte~istics of high-altitude ECC ozonesondes. In Atmosphe~ic Ozone . 

C. S. Ze~efos and A. Ghazi (Eds.), D. Reidel Publ. Co., Boston, MA, 499-

503. 

Komhy~, W. D., S. J . Oltmans, A. N. Chop~a, R. K. Leona~d, T. E. Ga~ia, and 

C. M. McFee. Results of Umkehr, ozonesonde , total ozone, and sulfur 

dioxide observations in Hawaii following the e~uption of EI Chichon 

volcano in 1982. In Atmosphe~ic Ozone. C. S. Ze~efos and A. Ghazi 

(Eds . ), D. Reidel Publ . Co ., Boston, MA, 305-310. 

Lu~ia , M., and G. Sha~f . The influence of light intensity , S02 ' NOx and C3H6 

on sulfate ae~osol fo~mation. J. Atmos. Chern. 2:321-329. 

Lu~ia, M., U. A~mit, and M. Peleg. Compa~ison 

f~om rooftop , sidewalk and subu~ban a~eas. 

5 :249-254. 

of ai~ quality data obtained 

Envi~on. Monito~. Assess. 

Luria, M., T. David, and M. Peleg. Five yea~ ai~ quality t~ends in Jerusalem, 

Is~ael. Atmos. Envi~on. 19:715-726. 

Luria, M., C. 

Pueschel. 

presented 

C. Van Valin, J. F. Boatman, D. L. Wellman, D. Hastie, and R. F. 

S02 flux measu~ements ove~ the Western Atlantic Ocean. Pape~ 

at the AGU Fall Meeting, San F~anciso, CA, 8-13 Decembe~ 1985. 

Matee~, C. L. and J. J. DeLuisi. A compa~ison of ozone profiles de~ived from standa~d Umkeh~ and short Umkehr measu~ements from fifteen stations . In 

Atmosphe~ic Ozone. C. S. Ze~efos and A. Ghazi (Eds.), D. Reidel Publ. 

Co., Boston, MA , 290-294. 

Mendonca, B. G. Measu~ements in the Geophysical Monito~ing fo~ Climatic 

Change Division of NOAA, U.S.A : A fi~st step in an integ~ated global 

monito~ing effo~t. Pape~ p~esented at the Thi~d Inte~national Symposium 

of Integ~ated Global Monito~ing of the state of the biosphe~e, Tashkent, 

U.S.S.R., 13-20 October 1985. 

Mendonca, B. G., J. J. DeLuisi, and E. G. Dutton. Twenty-six yea~s of long- ~ange t~anspo~t of atmosphe~ic ae~osols ove~ Mauna Loa. Paper p~esented 

at the IAMAP/IAPSO Joint Assembly, Honolulu, HI, 5-16 August 1985. 

Miller, J. M., and J. M. Ha~~is. The flow climatology to Be~muda and its 

implications fo~ long-range t~ansport. Atmos. Environ. 19(3):409-414. 

Oltmans, S. J. Measu~ements of wate~ vapo~ in the st~atosphere with a frostpoint hyg~ometer. Proceedings, Inte~national Symposium on Moistu~e and 

Humidity, Ap~il 15-19, 1985, Washington, D.C. Instrument Society of 

America, Resea~ch T~iangle Pa~k , NC, 251-258. 

140 
Oltmans , S. J . T~oposphe~ic ozone at four ~emote obse~vato~ies. In 

Atmosphe~ic Ozone. C. S. Ze~efos and A. Ghazi (Eds .), D. Reidel Publ. 

Co., Boston, MA, 796-802. 

Patte~son , E. M., R. A. Castillo , and J. J. DeLuisi . Cloud washout ~atios for 

graphitic carbon at Whiteface Mt., NY. Paper presented at the IAMAP/IAPSO 

Joint Assembly, Honolulu, HI, 5-16 August 1985. 

Peterson, J. T. Summary comments on the scientific highlights of the 

confe~ence. Lectures p~esented at the WMO Technical Conference on Obse~vation of Atmospheric Contaminants, TECOMAC , Vienna , Aust~ia, 17-21 

October 1983. HMO No. 64 , Spec. Environ . Rept. No . 16, Wo~ld 

Meteorological Organization , Geneva , Switzerland, xx-xxv. 

Pete~son, J. T., and W. D. Komhyr . Atmospheric CO2 measurements at Barrow , Alaska. Lectures presented at the WMO Technical Conference on Observation 

of Atmospheric Contaminants , TECOMAC, Vienna, Austria, 17-21 October 

1983. WMO No. 64 , Spec. Environ. Rept . No. 16, World Meteorological 

O~ganization, Geneva, Switze~land, 76-80. 

Peterson , J. T., T. J. Conway, and D. A. Gillette. CO2 variability between 

high northern latitude sites. Paper p~esented at the conference 

Atmospheric Carbon Dioxide: Its Sources, Sinks, and Global Transpcrt, 

Kandersteg , Switzerland, 2-6 September 1985. 

Pollack, J. B., M. P. McCormick, E. G. Dutton , and J. J. DeLuisi. A 

climatology of the El Chichon volcanic cloud for use in climate models. 

Paper presented at the IAMAP/IAPSO Joint Assembly, Honolulu, HI, 5-16 

August 1985. 

Pueschel, R. F. , D. L. Wellman, and J. F. Boatman . Tropcspheric ae~osols over 

the Western Atlantic: Scale height and concentrations. Paper presented at 

the AGU Fall Meeting, San Franciso, CA , 8-13 December 1985. 

Raatz, W. E. Meteorological conditions over Eurasia and the Arctic 

contributing to the March 1983 A~ctic haze episode. Atmos. Environ. 

19(12):2121-2126. 

Raatz, W. E., R. C. Schnell, and B. A. Bodhaine. Atmospheric c~oss sections 

fo~ the A~tic Gas and Aerosol Sampling P~ogram, March-Ap~il 1983. NOAA 

Tech. Memo. ERL ARL-134, Boulder, CO, 50 pp. 

Raatz , W. E., R. C. Schnell, and B. A. Bodhaine. The dist~ibution and 

t~anspc~t of pcllution ae~osols ove~ the Norwegian Arctic on 31 March and 

4 April 1983. Atmos. Environ. 19(12):2135-2142. 

Raatz, W. E., R. C. Schnell , B. A. Bodhaine, and S. J. Oltmans. Observations 

of Arctic Haze during polar fights from Alaska to Norway. Atmos. Environ. 

19(12) :2143-2151. 

Raatz , W. E. , R. C. Schnell, B. A. Bodhaine, S. J. Oltmans, and R. H. 

Gammon. Air mass characte~istics in the vicinity of Barrow, Alaska , 9-19 

Ma~ch 1983 . Atmos. Environ . 19(12):2127:2134. 

1 41 
Raatz, W. E., R. C. Schnell, M. A. Shapi~o, S. J . Oltmans , and B. A. Bodhaine. Inst~usions of st~atosphe~ic ai~ into Alaska 's t~oposphe~e, 

Ma~ch 1983 . Atmos . Envi~on . 19(12) :2153-2158. 

Robinson, E. Book ~eview , "The Majo~ Biogeochemical Cycles and Thei~ 

Inte~actions " B. Bolin and R. B. Cook (Eds . ). In Wate~, Ai~ , Soil 

Pollut ., 24(2):228-229 . 

Robinson , E. Book ~eview, "Ai~ Pollution Modeling and Its Application III ," 

C. DeWispelae~e (Ed.). Wate~ , Ai~, Soil Pollut. , 25(2):233-234 . 

Schnell , R. C. A~ctic Gas and Ae~osol Sampling P~og~am . Pape~ p~esented at 

the Inte~-Agency Wo~kshop on Sensing f~om Ai~c~aft, NCAR , Boulde~ , CO, 19-

22 August 1985. 

Schnell , R. C. The inte~national A~tic Gas and Ae~osol Sampling P~og~am. In A~ctic Atmosphe~ic Pollution, Abst~acts of pape~s , Inte~national 

Confe~ence , Scott Pola~ Resea~ch Institute , Unive~sity of Camb~idge , 

England , 2-5 Septembe~ 1985 . Sponso~ed by the State of Alaska , 6-7 . 

Schnell , R. C. , and W. E. Raatz . Rapid long ~ange t~anspo~t of ai~ pollutants ac~oss the A~ctic: The Ma~ch 1983 A~ctic haze episode . Pape~ p~esented at 

the IAMAP/IAPSO Joint Assembly, Honolulu, HI, 5-16 August 1985 . 

Schnell , R. C. , W. E. Raatz, and J. T. Pete~son. A~ctic Gas and Ae~osol 

Sampling P~og~am . Lectu~es p~esented at the WMO Technical Confe~ence on Obse~vation of Atmosphe~ic Contaminants, TECOMAC, Vienna , Au~L~ia, 17-21 Octobe~ 1983. WMO No . 64 , Spec . Envi~on . Rept . No . 16, o~ld 

Meteo~ological O~ganization, Geneva , Switze~land , 324-333. 

Sieve~ing , H. G~adient measu~ements of sulfu~ and soil mass d~y deposi tion ~ates unde~ clean ai~ and high-wind-speed conditions. Atmos. Envi~on. 

20(2) :341-345 . 

Stea~ns , L. P. , and R. F. Pueschel. Pa~ticle dis ~ibutio n of cl ouds on 

Whiteface Mountain . Pape~ p~esented at the AGU Fall Meeting , San F~anciso , CA, 8-13 Decembe~ 1985. 

Steele, L. P., T. J. Conway , L. S. Wate~man , R. H. Gammon , P. J. F~aser , R. F. Weiss, and R. A. Rasmussen . Measu~ements of atmOSphe~ic methane m the 

AKADEMIK KOROLEV c~uise, Octobe~-Decembe~ 1983. Pape~ p~esented at the 

AGU Fall meeting, San F~ancisco , CA , 8- 13 Decembe~ 1985 . 

Steele , L. P. , P. J. F~ase~ , R. A. Rasmussen, M. A. K. Khalil , A. J . Crawfo~d , 

T. J. Conway, R. H. Gammon , K. A. Masa~ie , and K. W. Thoning . The global dist~ibution of methane in the t~oposphe~e . Pape~ p~esented at the AGU 

Fall Meeting , San F~ancisco , CA , 8-13 Dece be~ 1985 . 

Thompson, T. M. , W. D. Komhy~, and E. G. Dutton . Chlo~ofluo~oca~bon-11 , -12 , and nit~ous oxide measu~ements at the NOAA/GMCC baseline stations (16 Septembe~ 1973 to 31 Decembe~ 1979) . NOAA Tech. Rep . ERL-428 - ARL-8 , Boulde~, CO , 124 pp . 

142 
Van Valin , C. C., and M. Lu~ia. 03' CO, hyd~oca~bons and dimethyl sulfide ove~ the Western Atlantic Ocean . Pape~ p~esented at AGU Fall Meeting , San F~anciso , CA , 8-13 Decembe~ 1985 . 

Wate~man, L. W., T. J . Conway , R. H. Gammon, and R. F. Weiss. pC02 measu~ements in the equato~ial Pacific Ocean . Pape~ p~esented at the AGU 

Fall Meeting , San F~ancisco , CA , 8-13 Decembe~ 1985 . 

Wincheste~, J . W., R. C. Schnell, S. 

Naegele, A. D. A. Hansen , and H. 

in Arctic ae~osols, sp~ing 1983. 

F. Fan , 

Rosen. 

Atmos. 

S. Li , B. A. Bodhaine , P. S. Pa~ticulate su lfu~ and chlo~ine 

Envi~on . 19:2167-2173. 
A~ 

AGASP 

ALE 

A~ 

ARM 

ASASP 

AS~ 

ASR 

BAO 

BAPMoN 

BRW 

BW 

CAF 

CAMS 

CIR~ 

CFR 

CN 

CNC 

002 

~IRO 

CPU 

DAS 

DEW 

OOE 

DSET 

D.U. 

OOY 

EC-GC 

ECC 

Effi 

EML 

ENSO 

EPA 

EP~ 

ERL 

ITS 

FPD 

FSSP 

FWNIP 

FYO 

GC 

G.E. 

GMCC 

GPCP 

GMT 

mA 

HASL 

~O 

& 

IAMAP 

11. ACRONYMS AND ABBREVIATIONS 

Atmospheric Environment Service, Canada 

Arctic Gas and Aerosol Sampling Program 

Atmospheric Lifetime Experiment 

Air Resources Laboratory, Silver Spring, MD (E~) 

Aerosols and Radiation Monitoring 

Active-scattering aerosol spectrometer probe 

Alaska Soil Conservation Service 

Aerosols and Solar Radiation, referring to CAMS 

Boulder Atmospheric Observatory 

Background Air Pollution Monitoring Network 

Barrow Observatory, Barrow, Alaska (GMCC) 

Biologically-active ultraviolet 

Clean Air Facility 

Control and Monitoring System 

Cooperative Institute for Research in Environmental SCiences, 

University of Colorado , Boulder, CO 

Centre des Faibles Radioactivites, Gif-sur-Yvette, France 

Condensation nuclei 

Condensation nucleus counter 

Carbon dioxide, referring to CAMS 

Commonwealth Scientific and Industrial Research Organization, 

Australia 

Central processing unit 

Data acquisition system 

Distant Early Warning 

Department of Energy 

Desert Solar Environment Testing 

Dobson unit 

Day of year, Julian 

Electron capture gas chromatograph 

Electrochemical concentration cell 

Energy dispersive spectrometry 

Environmental Measurements Laboratory (DOE) 

El Nino-Southern Oscillation 

Environmental Protection Agency 

Equatorial Pacific Ocean Climate Studies 

Environmental Research Laboratories, Boulder, CO (NOAA) 

Federal Telecommunication System 

Flame photometric detector 

Forward-scattering spectrometer probe 

Four-wavelength manual incidence phyrheliometer 

Four-year oscillation 

Gas chromatograph 

General Electric 

Geophysical Monitoring for Climatic Change, Boulder, CO (A~) 

Global Precipitation Chemistry Project 

Greenwich mean time 

General Services Administration 

Health and Safety Laboratory (EPA) 

High Altitude Observatory 

Hewlett-Packard 

International Association of Meteorology and Atmospheric Physics 

144 
IAPSO 

IBM 

ICDAS 

ICSU 

IPC 

IR 

IS\-IS 

ITT 

LAMP 

LBL 

LST 

MLO 

MMD 

M03 

MPBL 

MSL 

NADP 

NAPAP 

NARL 

NASA 

NBS 

NCAR 

NESDIS 

NDIR 

NH 

NIP 

NOAA 

NRI 

NRIP 

NI-IR 

N\-IS 

NI-IT 

~~ 

PBL 

PC 

PIXE 

PMEL 

PMOD 

PRE-STORM 

QBO 

RITS 

RFP 

SAD 

SAGE 

SBUV 

SEASPAN 

SEAREX 

SH 

SIO 

S~lO 

SN 

STEM 

SUNYA 

International Association for the Physical Sciences of the Ocean 

International Business Machines 

Instrumentation Control and Data Acquisition System 

International Council of Scientific Unions 

International Pyrheliometer Comparison 

Infrared 

Illinois State \-later Survey 

International Telephone and Telegraph 

Laboratoire Associe de Meteorologie, France 

Lawrence Berkeley Laboratory (DOE) 

Local standard time 

Mauna Loa Observatory, Hawaii (GMCC) 

Mass mean diameter 

Meteorology and ozone, referring to CAMS 

Marine planetary boundary layer 

Mean sea level 

National Atmospheric Deposition Program 

National Acid Precipitation Assessment Program 

Naval Arctic Research Laboratory, Barrow, AK 

National Aeronautics and Space Administration 

National Bureau of Standards 

National Center for Atmospheric Research, Boulder, CO 

National Environmental Satellite, Data, and Information Service 

Nondispersive infrared 

Northern Hemisphere 

Normal incidence pyrheliometer 

National Oceanic and Atmospheric Administration 

National Resource Inventory 

New River Intercomparison of Pyrheliometers 

Niwot Ridge, CO 

National \-leather Service 

Northwest Territories, Canada 

Oregon Graduate Center, Beaverton, OR 

Portable pressurizer pack air sampler 

Planetary boundary layer 

Personal computer 

Proton-induced X-ray emission 

Pacific Marine Environmental Laboratory, Seattle, \-IA 

Physikalisch-Meteorologisches Observatorium Davos 

Preliminary Regional Experiment for Storm Central 

Quasi-biennial oscillation 

Radiatively Important Trace Species 

Request for proposal 

Selected Area Diffraction 

Stratospheric Aerosol and Gas Experiment 

Solar backscattered ultraviolet 

SEAREX South Pacific Aerosol Network 

Sea-Air Exchange Program 

Southern Hemisphere 

Scripps Institution of Oceanography, La Jolla, CA 

Samoa Observatory, American Samoa (GMCC) 

Serial number 

Scanning Transmission Electron Microscopy 

State University of New York at Albany 

145 
SPO 

SRF 

SRL 

SRBL 

SST 

TMI 

TTO 

ULF 

UNEP 

UPS 

URAS 

URI 

USGS 

UV 

WATOX 

WERIS 

WMO 

WRR 

WSG 

ZRAM 

South Pole Obse~vato~y, Anta~ctica (GMCC) 

Sola~ Radiation Facility 

Smithsonian Radiation Labo~ato~y 

Smithsonian Radiation and Biological Labo~ato~y 

Sea s~face tempe~at~e 

Technical Meas~ements, Inc. 

T~ansient T~ace~s in the Ocean Ult~alow f~equency 

United Nations Envi~onmental Prog~am 

Uninte~ruptible power supply 

Ult~a Rot Absorptions Schreiber (Ha~tmann-Braun infra~ed 

analyzer) 

University of Rhode Island, Kingston, RI 

United States Geological Survey 

Ultraviolet 

Western Atlantic Ocean Experiment 

Wind Energy Resou~ce Information System 

World Meteo~ological O~ganization, Geneva , Switzerland 

World Radiometric Reference Wo~ld Standard Group 

"Z" ~andom access memory 

146 

.u.s. GOVERNMENT PRINT I NG OFF I CE; 1989-0-673-0 02/ 92042