A.	CRUISE NARRATIVE:
A.1.	HIGHLIGHTS

                              WHP Cruise Summary Information

SHIP:  METEOR
WOCE Line   | ExpoCode | Chief Scientist                    | Dates
            |          |                                    |
AR12, AR24  | 06MT39_2 | Thomas J. Müller, Walter Zenk/IfMK | 1997.05.15 - 1997.06.06
A02         | 06MT39_3 | Peter Koltermann/BSH               | 1997.06.11 - 1997.07.03
AR07W, AR05 | 06MT39_4 | Fritz Schott/IfMK,                 | 1997.07.07 - 1997.08.07
AR07E. AR25 | 06MT39_5 | Alexander Sy/BSH                   | 1997.08.14 - 1997.09.14


06MT39_2 (74 stns)  | 06MT39_3 (80 stns)     | 06MT39_4 (102 stns) | 06MT39_5 (43 stns)
--------------------|------------------------|---------------------|--------------------
Brest, France to    | Cork, Ireland to St.   | St. John's, Nfndlnd | Reykjavik, Iceland
Cork, Ireland       | John's Newfndlnd, Can  | to St. Anthony to   | to Hamburg, Germany
                    |                        | Reykjavik, Iceland  | 
--------------------|------------------------|---------------------|--------------------
GEOGRAPHIC BOUNDARIES:                       |                     |
--------------------|------------------------|---------------------|--------------------
       61°10'N      |     49°13.9'N          |      60°18.5'N      |        65°31'N
35°9.84'W  9°3.78'W | 50°.4'W   10°38.8'W    | 56°32'W    34 °50'W | 42°51'W    14°29.9'W
      50°25.32'N    |      42°.9'N           |     48°51.4'N       |         51°42'
--------------------|------------------------|---------------------|--------------------
FLOATS:             |                        |                     |
--------------------|------------------------|---------------------|--------------------
9 RAFOS floats      | 3  C-PALACE floats     | 7  Palace floats    | 0  Floats
--------------------|------------------------|---------------------|--------------------
MOORINGS:           |                        |                     |                     
--------------------|------------------------|---------------------|--------------------
2 deployed          | 1 recovered/1 deployed |  0                  | 6 deployed, 4 recovered 


                       CONTRIBUTING AUTHORS (as they appear in text)
                       ---------------------------------------------
R. Zahn, W. Zenk, K.P.Koltermann, F. Schott, A. Sy, S. Becker, B. Lenz, T.J. Müller, 
O. Plähn, A. Körtzinger , L. Stramma, C. Mertens, J. Fischer, U. Send, D. Kindler, 
M. Rhein, U .Karger, H. Gäng, L. Mintrop, H.-J. Weichert, G. Stelter, A. Frohse, 
F. Morsdorf, Ch. Stransky, R. Kramer, H. Tacke, F. Schmiel, A. Gottschalk, K. Bulsiewicz, 
U. Fleischmann, G. Fraas, R. Gleiss, V. Sommer , H. Giese, C. Neill, E. Lewis, K. Bakker, 
D. Machoczek, H. Mauritz, K. Schulze, M. Stolley, N. Verch, M. Reich, L. Czechel, 
H. Hildebrandt, C. Mohn, J. Read, G. Hargreaves, J. Ashley, H. Thomas, B. Schneider, 
N. Gronau, E. Trost, R. Keir, G. Rehder, M. Arnold, R. Bayer, M. Huels, S. Jung, A. Müller, 
C. Willamowski, G. Bozzano, C. Didie, L. Lembke, N. Loncaric,  P. Schäfer , J. Schönfeld, 
A. Kohly, B. Bader, I. Cacho, K. Heilemann, F.-J. Hollender, T. Karp, K. Flechsenhar, 
B. Brandt, G. Kahl

                                         METEOR - BERICHTE
                                               99-1
                                       North Atlantic 1997
                                          Cruise No. 39
                                   18 April - 14 September 1997

                                           Edited by:
             Friedrich Schott, Klaus-Peter Koltermann, Lothar Stramma, Alexander Sy, 
                                    Rainer Zahn and Walter Zenk

                                       Editorial Assistance:
                                         Franck Schmieder
                        Fachbereich Geowissenschaften, Universität Bremen
                                         Leitstelle METEOR
                         Institut für Meereskunde der Universität Hamburg
                                               1999

WHP CRUISE AND DATA INFORMATION

TABLE OF CONTENTS

Abstract
Zusammenfassung

1	Research Objectives
	1.1	Introduction
	1.2	Projects

2	Participants

3	Research Programs
	3.1	WOCE program
		3.1.1	Physical Oceanography during WOCE cruises
			3.1.1.1 Hydrographic measurements at 48ƒN in the North Atlantic 
				along the WHP section A
			3.1.1.2 WOCE-NORD
		3.1.2	Nutrients and tracer measurements during WOCE cruises
	3.2	Sonderforschungsbereich (SFB) 
		3.2.1	Physical Oceanography during SFB cruises
		3.2.2	Air-sea fluxes
		3.2.3	Carbon dioxide system, oxygen, nutrients during SFB-cruises
	3.3	Other programs 
		3.3.1	VEINS programs
		3.3.2	Tracer sampling
		3.3.3	Methane
		3.3.4	Foraminifera (_13C and _18O data in foraminifera)
	3.4	Paleoceanography
		3.4.1	Water Column Profiling: Ground-Truth Data Base for Calibration of 
			Paleoceano-graphic Proxies
		3.4.2	Plankton in Surface Waters off Portugal
		3.4.3	Benthic Foraminifera: Faunal Composition and Stable Isotopes
		3.4.4	Trace Fossils and Bioturbation as Indicators of Paleo- 
			Environmental Conditions
		3.4.5	Temperate Water Carbonates
		3.4.6	Trace Metals in Calcareous Microorganisms as Paleoceanographic 
			Tracers
		3.4.7	Sediment Geochemistry and Mineralogy

4	Narrative of the cruise
	4.1	Leg M39/1 (R. Zahn)
	4.2	Leg M39/2 (W. Zenk)
	4.3	Leg M39/3 (K. P. Koltermann)
	4.4	Leg M39/4 (F. Schott)
	4.5	Leg M39/5 (A. Sy)

5	Preliminary Results
	5.1	SFB
		5.1.1	Physical Oceanography of the eastern Basin (M39/2)
			5.1.1.1 Hydrography (S. Becker, B. Lenz, T.J. M¸ller, W. Zenk)
			5.1.1.2 Freon Analysis (CFC) (O. Pl”hn)
			5.1.1.3 Carbon Dioxide System, Nutrients and Oxygen (A. K–rtzinger)
		5.1.2	Physical Oceanography of the Labrador and Irminger Sea (M39/4)
			5.1.2.1 Technical aspects
			5.1.2.2 Analyses and Evaluations
			5.1.2.3 Air-sea fluxes (U.Karger, H.G”ng)
			5.1.2.4 Carbon Dioxide System, Nutrients and Oxygen (L. Mintrop)
	5.2	WOCE and VEINS
		5.2.1	Leg M39/3
			5.2.1.1 Hydrographic Measurements
			5.2.1.2 Nutrients and Oxygen Measurements
			5.2.1.4 Mooring work and float deployment (H. Giese, K. P. 
				Koltermann)
			5.2.1.5 "TCO2 and Total Alkalinity Measurements along 48ƒN on the 
				WHP section A2 1997" (C. Neill, E. Lewis)
		5.2.2	Leg M39/5
			5.2.2.1 Hydrographic Measurements (A. Sy, K. Bakker, R. Kramer, D. 
				Machoczek, H. Mauritz, F. Schmiel, K. Schulze, G. Stelter, 
				M. Stolley, N. Verch)
			5.2.2.2 Tracer Measurements
			5.2.2.3 Current Measurements
			5.2.2.4 Carbonate chemistry in the Northern Atlantic Ocean (H. 
				Thomas, B. Schneider, N. Gronau and E. Trost)
	5.3	Other programs
		5.3.1	Methane (R.Keir, G.Rehder)
		5.3.2	Tritium/helium sampling program results from M39, legs 4 and 5 (H. 
			Hildebrandt, M. Arnold, R.Bayer)
	5.4 	Paleoceanography
		5.4.1	Water Column T-S Profiling (M. Huels, S. Jung, R. Zahn)
		5.4.2	Seawater Sampling for Trace Element and Nutrient Analysis (A. 
			M¸ller, C. Willamowski)
		5.4.3	Shipboard Sediment Sampling and Core Flow (G. Bozzano, C. Didie, M. 
			Huels, S. Jung, L. Lembke, N. Loncaric, P. Sch”fer, J. Sch–nfeld)
		5.4.4	Plankton Hauls (A. Kohly)
		5.4.5	Porewater Oxygen Profiling: Reference for Benthic Foraminiferal 
			Assemblage Studies (J. Sch–nfeld)
		5.4.6	Trace Fossil Recording and Grab Sampling (P. Sch”fer, B. Bader)
		5.4.7	Geochemistry and Mineralogy (G. Bozzano, I. Cacho)
		5.4.8	High-Resolution Acoustic Mapping and Core Logging: 
			Paleoceanographic Application (K. Heilemann, F.-J. Hollender, T. Karp)

6	Ship's Meteorological Station
	6.1	Meteorological conditions during leg M39/1 (K. Flechsenhar)
	6.2	Meteorological conditions during leg M39/2 (B. Brandt)
	6.3	Meteorological conditions during leg M39/3 (B. Brandt )
	6.4	Meteorological conditions during leg M39/4 (G.Kahl)
	6.5	Meteorological conditions during leg M39/5 (G.Kahl)

7	Lists
	7.1	Leg M39/1
		7.1.1	Locations for sediment and plankton/water samples
		7.1.2	Water sampling sites for plankton assemblage studies
		7.1.3	Phyto- and zooplankton species found in M39/1 sampling sites
	7.2	Leg M39/2
		7.2.1	CTD Inventory
		7.2.2	Mooring Activities
		7.2.3	List of RAFOS Float Launches
	7.3	Leg M39/3
		7.3.1	Station list of cruise M39/3
	7.4	Leg M39/4
		7.4.1	CTD-profile station list and water samples taken from the bottles
	7.5	Leg M39/5
		7.5.1	Station listing

8	Concluding remarks and acknowledgements

9	CFC Reports
	9.1	Leg M39/2 
	9.2	Leg M39/3 
	9.3	Leg M39/4 
	9.4	Leg M39/5 

10	References



ABSTRACT

METEOR cruise M39 took place in the North Atlantic Ocean and consisted of five 
legs. Work on M39 was carried out mainly in the context of two climate relevant 
programs: for Sonderforschungsbereich (SFB) 460 ("Dynamics of thermohaline 
circulation variability"), during legs M39/2 and M39/4, and for the World Ocean 
Circulation Experiment (WOCE), during M39/ 3 and M39/5 while paleo-oceanographic 
studies were carried out on one leg, M39/1.

During the first cruise leg M39/1, departing 18 April 1997 out of Las Palmas, 
Canary Islands, paleo-oceanographic work was carried out in the eastern Atlantic. 
The objective was to document the history of the North Atlantic's thermohaline 
circulation during the last glacial period. Sediment cores and sediment surfaces 
along deep transects in the Gulf of Cadiz and off Portugal were sampled. With 
detailed paleo-oceanographic time series, the hydrographic history of North 
Atlantic water masses and of Mediterranean water were recorded. Ocean chemistry 
work documented today's distribution of paleo-oceanographic trace-elements. Cruise 
leg M39/1 ended on 10 May in Brest.

METEOR left Brest again on 14 May for leg M39/2. During this leg measurements were 
conducted in the eastern North Atlantic within the context of the SFB 460 of Kiel 
University. The aim was to investigate the variability of water masses of the 
subpolar gyre during their passage through the Iceland Basin as well as its 
transport rates and pathways. Detailed CTD surveys on seven sections and the 
deployment of current meter moorings and RAFOS floats were carried out for long-
term observations of Overflow- and Labrador Sea Waters. Leg M39/2 was completed on 
8 June 1997 in Cork, Ireland.

Cruise leg M39/3 focused once again on a survey of the 48ƒN WOCE section A2 under 
one-time survey requirements. Since earlier observations had shown a large 
interannual variability of all hydrographic properties, this survey was again 
combined with chemical oceanographic measurements to arrive at a CO2 budget. 
Results from this cruise confirm these rapid full-depth changes. The data will be 
used to calculate indices of the meridional circulation such as transports of heat, 
freshwater and mass and the meridional overturning. Previous estimates had shown 
large changes in the heat transports. The observations of cruise M39 are required 
to advance the understanding of the underlying mechanisms.

Leg M39/4 began in St. John's on 6 July and investigations were carried out for 
several projects of the SFB 460. Since leg M39/4 had as an essential objective the 
retrieval and redeployment of a variety of moorings, it had to be subdivided into 
two segments with an interim stop on 16 July in St. Anthony (New Foundland). During 
the first part of leg M39/4 several moorings were successfully recovered, a 
boundary current meter array was deployed, CTD-profiles were taken and profiling 
ALACE floats deployed in the western part of the Labrador Sea. After the interim 
stop in St. Anthony the mooring work was continued in the Labrador Sea. Here, as 
well as in the Irminger Basin, a large amount of CTD stations were carried out to 
investigate the water mass distribution, spreading paths and transports in the 
western North Atlantic. Leg M39/4 had accomplished its objectives and ended on 11 
August in Reykjavik, Iceland.

Cruise M39/5 by R.V. METEOR was another contribution to the "World Ocean 
Circulation Experiment" (WOCE). In addition, work was carried out for the EC 
program "Variability of Exchanges in the Northern Seas" (VEINS). This leg started 
in Reykjavik (Iceland) on 14 August and finished in Hamburg (Germany) on 14 
September, 1997. The purpose of the first part of the cruise (VEINS) was to carry 
out CTD sections and to recover and redeploy current meter moorings in the overflow 
waters off East Greenland, between the Denmark Straits and Cape Farvel. Work was 
part of a cooperation effort between British, Finnish, Icelandic and German 
institutions. The objective of the second part of this cruise leg was a repeat of 
the WOCE Hydrographic Programme section A1E/AR7E, running from Cape Farvel to the 
southern tip of the Porcupine Bank off the west coast of Ireland.

Overall METEOR cruise 39 was successful, and the intended work could be carried out 
according to plan. 

ZUSAMMENFASSUNG

Die METEOR-Reise M39 fand im Nordatlantischen Ozean statt. Im Verlauf von f¸nf 
Fahrtabschnitten wurden Arbeiten haupts”chlich im Zusammenhang mit zwei 
klimarelevanten Programmen durchgef¸hrt, dem Sonderforschungsbereich (SFB) 460 
"Dynamik thermohaliner Zirkulationsschwankungen" (Abschnitte M39/2 und M39/4) und 
dem "World Ocean Circulation Experimentis (WOCE) (Abschnitte M39/3 und M39/5). Ein 
Fahrtabschnitt (M39/1) diente Paleo-Ozeanographischen Untersuchungen.

FS METEOR lief am 18. April 1997 von Las Palmas auf den Kanarischen Inseln f¸r den 
ersten Abschnitt M39/1 aus. Paleo-Ozeanographische Arbeiten wurden im –stlichen 
Nordatlantik durchgef¸hrt. Das Ziel der Arbeiten war die Erforschung der Geschichte 
der Nordatlantischen Thermohalinen Zirkulation w”hrend der letzten Glazialperiode. 
Daf¸r wurden Sedimentkerne und Sedimentverteilungen entlang tiefer Schnitte im Golf 
von Cadiz und vor Portugal gesammelt. Meereschemische Arbeiten dokumentierten dabei 
die heutigen Verteilungen der Paleo-Ozeanographischen Spurenelemente. Das 
wissenschaftliche Programm von M39/1 wurde mit der Ankunft in Brest am 10. Mai 
beendet.

METEOR verlieþ Brest am 14. Mai f¸r den Abschnitt M39/2. Auf diesem Abschnitt 
wurden Messungen im –stlichen Nordatlantik f¸r den SFB 460 der Universit”t Kiel 
durchgef¸hrt. Ziel war die Untersuchung der Variabilit”t von Wassermassen des 
subpolaren Wirbels w”hrend ihres Durchquerens des Islandbeckens sowie ihre 
Ausbreitungswege und Transporte. Detaillierte CTD-Untersuchungen auf sieben 
Schnitten und Verankerung von Strommessern und RAFOS Floats wurden zur Beobachtung 
des Langzeitverhaltens des Overflow und des Labradorsee-Wassers durchgef¸hrt. Der 
Abschnitt M39/2 wurde am 8. Juni 1997 mit der Ankunft in Cork, Irland beendet.

Der Abschnitt M39/3 diente der erneuten hydrographischen Aufnahme des WOCE-Schnitts 
A2. Damit verbunden war die Wiederholung der Aufnahme der CO2-Verteilung auf diesem 
Schnitt im Rahmen von JGOFS. Die vorangegangene Aufnahme mit FS METEOR im Herbst 
1994 hatte bereits die deutlichen und schnellen Ver”nderungen der hydrographischen 
Kenngr–þen in diesem Ðbergangsgebiet zwischen dem Subpolar- und dem Subtropenwirbel 
im Vergleich mit den Vorg”ngeruntersuchungen aufgezeigt. Diese signifikante 
Variabilit”t wurde auf der jetzigen Reise best”tigt. Die Daten dieser Reise werden 
ebenfalls f¸r die Berechnung der meridionalen Zirkulationsgr–þen wie W”rme-, 
S¸þwassertransport und Meridionalzirkulation verwendet. Fr¸here Aufnahmen in den 
90er Jahren hatten Schwankungen besonders im W”rmetransport gezeigt, die zu 
verstehen Ziel der jetzigen Untersuchungen ist.

Der Abschnitt M39/4 begann in St. John's am 6. Juli, und die durchgef¸hrten 
Untersuchungen standen im Zusammenhang mit mehreren Teilprojekten des SFB 460. Da 
M39/4 als eines der Hauptarbeitsziele die Aufnahme und erneute Auslegung einer 
Vielzahl von Verankerungen hat- te, muþte M39/4 aus logistischen Gr¸nden in zwei 
Teile mit einem kurzen Zwischenstop in St. Anthony am 16. Juli aufgespalten werden. 
W”hrend des ersten Teils von M39/4 wurden mehre- re Verankerungen erfolgreich 
geborgen, ein Strommesser- und Randstromarray ausgelegt, CTD- Profile gewonnen und 
profilierende ALACE Floats im westlichen Teil der Labrador See ausgesetzt. Nach dem 
Zwischenstop in St. Anthony wurden zun”chst die Verankerungsarbeiten in der 
Labrador See fortgesetzt. Hier als auch im folgenden im Irminger Becken wurde eine 
Vielzahl von CTD-Profilen gewonnen, um die Wassermassenverteilung, und 
Ausbreitungspfade und Transporte im westlichen Nordatlantik zu untersuchen. Der 
Abschnitt endete am 11. August in Reykjavik, Island.

Reise M39/5 war ein weiterer Beitrag zum deutschen WOCE-Programm. Weiterhin wurden 
Arbeiten f¸r das EG-Programm "Variability of Exchanges in the Northern Seas" 
(VEINS) durchgef¸hrt. Der Fahrtabschnitt begann am 14. August in Reykjavik (Island) 
und endete am 14. September 1997 in Hamburg. Der Beitrag zu VEINS w”hrend des 
ersten Teils von M39/5 waren CTD-Messungen sowie Aufnahme und Wiederauslegung von 
Strommesserverankerungen zwischen dem ostgr–nl”ndischen Kontinentalabhang, der 
D”nemarkstraþe und Kap Farvel. Diese Arbeiten wurde in Kooperation zwischen 
britischen, finnischen, isl”ndischen und deutschen Instituten durchgef¸hrt. Das 
Hauptziel des zweiten Teils des Abschnitts war eine Wiederholung des WOCE Schnittes 
A1E/AR7E, einem hydrographischen Schnitt zwischen Kap Farvel und dem S¸dende der 
Porcupine Bank vor der Westk¸ste Irlands. Insgesamt war METEOR-Reise M39 
erfolgreich und die vorgegebenen Aufgaben konnten in vollem Umfang abgewickelt 
werden.

1	RESEARCH OBJECTIVES
1.1	Introduction

METEOR-cruise 39 took place in the North Atlantic Ocean with measurements mainly 
north of 40ƒN (Figure 1) except for some work off Portugal and near the entrance to 
the Mediterranean Sea during the first leg. The cruise began on 18 April 1997 in 
Las Palmas and ended on 14 September 1997 in Hamburg. METEOR-cruise 39 combined 
during five legs (Table 1) activities of paleo-oceanographic, physical 
oceanography, marine chemistry, meteorological, geological and tracer physics 
working groups.

After cruise M39 started in Las Palmas, METEOR headed towards the entrance of the 
Mediterranean. The work during the first leg off the southwest European shelf 
combined different working groups and measurement techniques to investigate paleo-
oceanographic problems with regard to the thermohaline circulation during the last 
glacial period.

The aims during the second and forth leg were regional investigations of the 
thermohaline circulation in the western and eastern basins within the context of 
the new "Sonderforschungs-bereich" at the University of Kiel SFB-460 "Dynamics of 
thermohaline circulation variability". The main objectives during the SFB-460 
related cruise legs were hydrographic measurements as well as intense mooring work.

Besides the hydrographic and mooring work during the two SFB-460 related cruise 
legs distributions of total dissolved inorganic carbon and total alkalinity were 
measured at the hydrocast locations. Nutrients and dissolved oxygen were determined 
in parallel. This combined analysis will allow the calculation of the penetration 
of anthropogenic CO2 into the water column. Additionally, a system to continuously 
monitor the CO2 partial pressure in surface waters and air operated during the two 
legs. This will allow calculating the CO2 flux between atmosphere and ocean.

During the third and fifth leg measurements of the thermohaline overturning 
circulation of the North Atlantic along two trans-Atlantic sections were carried 
out as final contributions of the Hamburg groups to the World Ocean Circulation 
Experiment (WOCE). Both sections were repeated several times since 1991 to 
investigate the transport rates of the meridional overturning circulation and its 
variability. Besides hydrography, marine chemistry and tracer measurements were 
carried out. During the fifth leg, measurements were made also for the "Variability 
of Exchanges in the Northern Seas (VEINS)" Project as part of the EC-MAST II 
program.

As part of the joint operation between WOCE and JGOFS (Joint Global Ocean Flux 
Study), on the leg M39/3, the components of the CO2 -system, such as dissolved and 
particular carbon CO2, were measured along the WHP-section A2 throughout the water 
column to describe the ocean's role as a buffer of atmospheric CO2. Its input into 
these highly to moderately convective regions covered by section A2 is strongly 
variable and therefore calls for more frequent sampling than elsewhere in the 
ocean.

Several other groups not imbedded in the large projects summarized about 
participated in some of the cruise legs and their work is detailed under sections 3 
and 5.

Fig. 1:	Cruise track of the 5 legs of METEOR cruise no. 39. To separate the 
	different cruise legs M39/2 is shown as dashed line. Transit sections are 
	shown as thin dashed lines.

Tab.1: Legs and chief scientist of METEOR cruise No. 39

Leg M39/1
18.04.-12.05.1997, Las Palmas, Canary Islands, Spain - Brest, France
Chief scientist :	Dr. R. Zahn

Leg M39/2
15.05.-08.06.1997, Brest, France - Cork, Ireland
Chief scientist :	Dr. W. Zenk

Leg M39/3
11.06.-03.07.1997, Cork, Ireland - St. John's, Canada
Chief scientist :	Dr. K. P. Koltermann

Leg M39/4
06.07.-11.08.1997, St. John's, Canada - Reykjavik, Iceland
Chief scientist :	Prof. Dr. F. Schott

Leg M39/5
14.08.-14.09.1997, Reykjavik, Iceland - Hamburg, Germany
Chief scientist :	Dr. A. Sy

Coordination: Prof. Dr. F. Schott

Masters:	Captain D. Kalthoff
		Captain M. Kull

1.2	Projects

A large fraction of the work carried out on cruise M39 is imbedded in the 
international WOCE program and the SFB-460, which both are shortly introduced here:

The goal of the World Ocean Circulation Experiment (WOCE) is to develop models for 
improved descriptions of the ocean circulation and prediction of climate changes 
and to collect the appropriate data in the World Ocean. The North Atlantic Ocean is 
characterized through an intensive meridional circulation cell, carrying near 
surface waters of tropical and subtropical origin northwards and deep waters of 
arctic and subarctic origin southwards. The transformation and sinking of water 
masses at high latitudes are the important processes for the "overturning" of the 
ocean. The overturning rates and the intensity of the meridional transports of 
mass, heat, and salt are control parameters for the modeling of the ocean's role in 
climate.

The two legs M39/3 and M39/5 provided two complete full-depth transoceanic 
hydrographic sections in the North Atlantic as a prominent contribution to the WOCE 
Hydrographic Programme (WHP), completing the German WOCE field work that started 
with METEOR cruise M18 in 1991. Both legs, M39/3 and M39/5 were also part of the 
seven-year observational programme WOCE-NORD (World Ocean Circulation Experiment - 
North Atlantic Overturning Rate Determination), a German contribution to WOCE and 
funded by the Ministry of Education and Research. Using repeated hydrographic 
sections between the southern tip of Greenland and Ireland in combination with 
current measurements the overturning rates of the North Atlantic will be estimated. 
Quantifying both input and output in the meridional overturning cell (MOC) will 
help to improve modeling the role of the ocean in the climate system.

The Sonderforschungsbereich SFB 460 "Dynamics of thermohaline circulation 
variability" began in 1996 at Kiel University. Main objective of the SFB 460 is to 
investigate the variability of the water mass formation and transport processes in 
the subpolar North Atlantic and to gain an understanding of its role in the 
dynamics of the thermohaline circulation and the ocean uptake of anthropogenic CO2. 
The variability of circulation and water mass distribution appears to be related 
through the North Atlantic Oscillation (NAO) with climate changes in northern 
Europe. These connections shall be investigated.

Legs M39/2 and M39/4 were carried out within the context of the SFB 460 with a wide 
range of hydrographic, tracer and current measurement techniques to investigate the 
variability of the circulation in the North Atlantic. The cruises were part of the 
opening phase of the SFB although the leg to the Labrador Sea was already the 
second cruise to this area of annually planned cruises within the SFB. During these 
two legs the focus was on the pathways of the deep circulation and the associated 
signals in the water mass distributions. Besides the shipboard measurements, a 
large part of the work was mooring work and the deployment of floats.

2	PARTICIPANTS

Tab.2: Participants of METEOR cruise no. 39

Leg M39/1

NAME			SPECIALITY		INSTITUTE
Zahn, Rainer, Dr.	Chief Scientist		GEO
Bader, Beate		Sedimentology		GIK
Bassek, Dieter		Meteorol.radio operator	DWD
Bozzano, Graziella	Sedimentology		ICM
Didie, Claudia		Sedimentology		GEO
Flechsenhar, Kurt	Meteorologist		DWD
Harder, Angela		Inorganic chemistry	GEO
Heidemann, Kristina	Geophysics		GEO
Hollender, Franz-Josef	Geophysics		GEO
H¸ls, Matthias		Paleocenaography	GEO
Jung, Simon		Paleocenaography	GEO
Karp, Tobias		Geophysics		GEO
Kohly, Alexander	Sedimentology		GIK
Lembke, Lester		Paleocenaography	GEO
Loncaric, Neven		Sedimentology		IGM
M¸ller, Anja		Sedimentology		GEO
Neufeld, Sergeij	Technician		GTG
Sch”fer, Prisca,Prof.Dr.Sedimentology,Paleontol.GIK
Sch–nfeld, Joachim	Micropaleontology	GEO
St¸ber, Arndt		Inorganic chemistry	GEO
Willamowski, Claudia	Inorganic chemistry	GEO

Leg M39/2

NAME			SPECIALITY		INSTITUTE
Zenk, Walter, Dr.	Chief scientist		IfMK
Amman, Lars		Marine Chemistry	IfMK
Bahrenfuþ, Kristin	Tracer Oceanography	IfMK
Becker, Sylvia		Marine Physics		IfMK
Brandt, Benno		Meteorology		DWD
Carlsen, Dieter		Marine Physics		IfMK
Csernok, Tiberiu	Marine Physics		IfMK
Friedrich, Olaf		Marine Physics		IfMK
Johannsen, Hergen	Marine Chemistry	IfMK
Keir, Robin, Dr.	Geochemistry		GEO
K–rtzinger, Arne, Dr.	Marine Chemistry	IfMK
Lenz, Bernd		Marine Physics		IfMK
Link, Rudolf		Marine Physics		IfMK
Meyer, Peter		Marine Physics		IfMK
M¸ller, Thomas J., Dr.	Marine Physics		IfMK
Nielsen, Martina	Marine Physics		IfMK
Heygen, Ronald		Logistic		RF
Ochsenhirt, Wolf-Thilo	Meteorology		DWD
Pinck, Andreas		Marine Physics		IfMK
Pl”hn, Olaf		Tracer Oceanography	IfMK
Rehder, Gregor, Dr.	Geochemistry		GEO
Schweinsberg, Susanne	Marine Chemistry	IfMK
Trieschmann, Babette	Tracer Oceanography	IfMK
Wehrend, Dirk		Marine Physics		IfMK

Leg M39/3

NAME			     SPECIALITY		      INSTITUTE
Koltermann, Klaus Peter, Dr. Chief Scientist	      BSH
W–ckel, Peter		     CTD engineer	      BSH
Stelter, Gerd 		     data scout & manager     BSH
Weichert, Hans-J¸rgen	     CTD data processing      BSH
Frohse, Alexander	     Salinometer	      BSH
Lohrbacher, Katja	     Hydrowatch captain	      BSH
Esselborn, Saskia	     Hydrowatch		      IfMH
Gouretski, Victor, Dr.	     Hydrowatch captain	      BSH/MPI
Stransky, Christoph	     Hydrowatch captain, XBT  BSH
Morsdorf, Felix		     Hydrowatch, L-ADCP	      IfMK
Gottschalk, Ilse	     Hydrowatch		      BSH
Fick, Michael		     Hydrowatch		      IfMH
Giese, Holger		     Moorings		      BSH
Tacke, Helga		     Nutrient Analyst	      BSH
Gottschalk, Anke	     Oxygen Analyst	      BSH
Schmiel, Franziska	     Oxygen Analyst	      BSH
Kramer, Rita		     Nutrient Analyst	      BSH
Bulsiewicz, Klaus	     Tracer/CFC		      UB
Plep, Wilfried		     Tracer/CFC		      UB
Fleischmann, Ulrich	     Tracer/CFC		      UB
Sommer, Volker		     Tracer/CFC		      UB
Gleiss, Ralf		     Tracer/CFC		      UB
Neill, Craig		     CO2 Analysis, DIC	      BNL
Lewis, Ernie		     CO2 Analysis, Alkalinity BNL
Brandt, Benno		     Meteorology	      DWD
Ochsenhirt, Wolf-Thilo	     Meteorology	      DWD

Leg M39/4

a) 06.07. - 16.07.1997 St. John's, Canada - St. Anthony, Canada
b) 16.07. - 11.08.1997 St. Anthony, Canada - Reykjavik, Iceland

NAME				SPECIALITY		INSTITUTE
Schott, Friedrich, Prof., Dr.	Chief Scientist (a,b)	IFMK
Adam, Dorothee			Tracer (b)		IFMK
Arnold Matthias			Helium/Tritium (a)	IUP
Bahrenfuþ, Kristin		Tracer (a, b)		IfMK
Begler, Christian		Oceanography (a, b)	IfMK
Dombrowsky, Uwe			Oceanography (a, b)	IfMK
Eisele, Alfred			Oceanography ( a, b)	IfMK
Fischer, J¸rgen, Dr.		Oceanography, (a, b)	IfMK
Friis, Karsten			CO2 (b)			IfMK
F¸rhaupter, Karin 		Foraminifera		GEO
G”ng, Holger, Dr.		Meteorology (a, b)	IfMK
Kahl, Gerhard			Meteorology, (a, b)	DWD
Karger, Uwe			Meteorology (a, b)	IfMK
Keir, Robin, Dr.		Methan (b)		GEO
Kindler, Detlef			Oceanography (a, b)	IfMK
K–nig, Holger			Oceanography (a, b)	IfMK
Malien, Frank			Oxygen, Nutrients (a, b)IfMK
Mauuary, Didier, Dr. 		Tomography (a)		CEP
Meinke, Claus			Oceanography (a, b)	IfMK
Mertens, Christian		Oceanography (a, b)	IfMK
Mintrop, Ludger, Dr.		CO2 (a, b)		GeoB
Ochsenhirt, Wolf-Thilo		Meteorology (a, b)	DWD
Papenburg, Uwe			Oceanography (a, b)	IfMK
Pl”hn, Olaf			Tracer (a)		IfMK
Rehder, Gregor, Dr.		Methan (b)		GEO
Rhein, Monika, Dr.		Tracer (b)		IfMK
Schweinsberg, Susanne		CO2 (a, b)		IfMK
Send, Uwe, Dr. 			Tomography (b)		IfMK
Stramma, Lothar, Dr.		Oceanography (a, b)	IfMK
Walter, Maren			Oceanography (a, b)	IfMK
Winckler, Gisela		Helium/Tritium (b)	IUP

Leg M39/5

NAME			SPECIALITY		    INSTITUTE
Sy, Alexander, Dr.	Chief Scientist		    BSH
Stolley, Martin		Hydro Watch, XBT	    BSH
Mohn, Christian		Hydro Watch, VM-ADCP	    IfMH
Berger, Ralf		Hydro Watch, CTD, L-ADCP    IfMK
Gottschalk, Ilse	Hydro Watch		    BSH
Weigle, Rainer		Hydro Watch		    IfMH
Struck, Petra		Hydro Watch		    BSH
Verch, Norbert		Salinity		    IfMH
Stelter, Gerd 		Bottle Data management	    BSH
Mauritz, Heiko		CTD DATA Processing	    BSH
Schulze, Klaus		TSG, Ship's Data management IfMH
Bakker, Karel		Nutrients		    NIOZ
Kramer, Rita		Nutrients, Oxygen	    BSH
Schmiel, Franziska	Oxygen			    BSH
Machoczek, Detlev	Oxygen			    BSH
Read, John		Moorings		    CEFAS
Hargreaves, Geoff	IES, Moorings		    POL
Ashley, John IES,	Moorings		    POL
Hildebrandt, Hauke	Tritium/He, 0-18, SF-6	    IUP
Rhein, Monika, Dr.	CFC, L-ADCP		    IfMK
Elbr”chter, Martina	CFC			    IfMK
Czeschel, Lars		CFC			    IfMK
Reich, Michael		CFC			    IfMK
Thomas, Helmuth, Dr.	CO2			    IOW
Trost, Erika		CO2			    IOW
Gronau, Nicole		CO2			    IOW
Kahl, Gerhard		Meteorology		    DWD
Bassek, Dieter		Meteorology		    DWD
Henning, Arndt		Film Team		    AmPuls
Sch”fer, Werner		Film Team		    AmPuls

Tab.3: Participating Institutions

AmPuls	AmPuls Film
	Film und TV Produktion
	Curschmannstr. 13
	20251 Hamburg - Germany
BNL	Oceanographic and Atmospheric Sciences Division
	Department of Applied Sciences
	Brookhaven National Laboratory
	Upton, NY 11973 - USA
BSH	Bundesamt f¸r Seeschiffahrt und Hydrographie
	Bernhard-Nocht-Str. 78
	20597 Hamburg - Germany
CEFAS	Centre for Environment
	Fisheries & Aquaculture Science
	Lowestoft Laboratory
	Lowestoft, Suffolk NR33 0HT - England
CEP	Centre d'Etude des PhÈnomËnes AlÈatoires et GÈophysiques
	EINSIEG-CAMPUS Universitaire
	BP 46,
	38402 Saint Martin d'hËres Cedex-France
DWD	Deutscher Wetterdienst
	Gesch”ftsfeld Seeschiffahrt
	Bernhard-Nocht-Str. 76
	20359 Hamburg - Germany
GEO	Geomar Forschungszentrum f¸r Marine Geowissenschaften
	Universit”t Kiel
	Wischhofstr. 1-3
	24148 Kiel - Germany
GeoB	Universit”t Bremen
	Fachbereich 5, Geowissenschaften
	Klagenfurter Str.
	28359 Bremen - Germany
GIK	Geologisch-Pal”ontologisches Institut
	Universit”t Kiel
	Olshausenstr. 40
	24118 Kiel - Germany
GTG	Geomar Technologie GmbH
	Wischofstr. 1-3
	24148 Kiel - Germany
ICM	Institut de Ciencies del Mar
	Consejo Superior de Investigaciones CientÌficas
	Passeig Joan de BorbÛ, s/n
	08039 Barcelona-Spain
IfMH	Institut f¸r Meereskunde der Universit”t Hamburg
	Troplowitzstr. 7
	22529 Hamburg - Germany
IfMK	Institut f¸r Meereskunde an der Universit”t Kiel
	D¸sternbrooker Weg 20
	24105 Kiel - Germany
IGM	Instituto GeolÛgico e Mineiro
	Rua Academia das CiÍncias, 19-2ƒ
	1200 Lisboa-Portugal
IOW	Institut f¸r Ostseeforschung Warnem¸nde
	Seestraþe 15
	18119 Rostock-Warnem¸nde - Germany
IUP	Institut f¸r Umweltphysik der Universit”t Heidelberg
	Im Neuenheimer Feld 366
	69120 Heidelberg - Germany
MPI	Max-Planck-Institut f¸r Meteorologie
	Bundesstr. 55
	20146 Hamburg - Germany
NIOZ	Nederlands Instituut voor Onderzoek der Zee
	Postbus 59
	1790 AB Den Burg, Texel -Netherlands
POL	Proudman Oceanographic Laboratory
	Bidston Observatory
	Birkenhead, Merseyside L43 7RA - England
RF	R/F Reedereigemeinschaft Forschungsschifffahrt GmbH
	Haferwende 3
	28357 Bremen - Germany
UB	Universit”t Bremen
	Institut f¸r Umweltphysik, Abt. Tracer-Oceanographie
	Bibliotheksstraþe
	28359 Bremen - Germany

3	RESEARCH PROGRAMS
3.1	WOCE program

Two hydrographic sections were carried out within the WOCE program. The northern 
section from Greenland to Ireland (WHP A1-East) cuts across the convective regime 
of the Subpolar Gyre, whereas the southern of the two sections, running from the 
English Channel to the Grand Banks off Newfoundland (WHP A2), spans the non or 
weakly-convective regime of the transition zone between the subpolar and 
subtropical gyres. The data are used to estimate the transports of heat and matter 
of the meridional circulation and contribute towards estimating the so-called 
"overturning" of the oceanic meridional circulation regarded as the main driving 
mechanism for the global thermohaline circulation and its temporal changes. Special 
emphasis is put on the intensive propagation of newly formed Labrador Sea Water 
(LSW) into the North Atlantic, first seen in the 1993 coverage of A2. These 
coverages of sections A1 and A2 repeat some earlier measurements that have shown a 
high temporal and spatial variability of both the water mass characteristics and 
the meridional transports of heat, salt and freshwater.

3.1.1	Physical Oceanography during WOCE cruises
3.1.1.1 Hydrographic measurements at 48ƒN in the North Atlantic along the WHP 
	section A2

The meridional transports of heat, freshwater and salt in the Atlantic Ocean and 
their seasonal and inter-annual changes have been determined for the 90s across the 
latitude of the global maximum freshwater transport at ca. 50ƒN in the Atlantic 
Ocean. Results are compared with previous measurements in the 50s and 80s. They 
show surprisingly variable transports, suggesting time scales of 10 years for 
changes originating in the subpolar and some 30 years for those originating in the 
subtropical gyre.

Working the section A2/AR19 at about 48ƒN in the summer of 1993 with FS Gauss 
(G226) has shown the Labrador Sea Water temperatures some 0.4ƒC below its 
historical characteristic temperature, and deeper in the water column by some 700 
m. This fits with the observations for the early 90s along 60ƒN and 24ƒ30'N and 
indicates a rapid reaction of the intermediate circulation of the northern North 
Atlantic to changes in the buoyancy forcing in the Labrador Sea. This situation 
seems to have ended in 1995/96 when the NAO-Index, characterizing the prevailing 
atmospheric forcing over the region, changed from an all-time high to moderate 
values. First reactions of the ocean to these changes can be seen in the coverage 
of the sections A2 with FS Gauss (G276/1) and A1 with FS Meteor in the fall of 
1994. The cruise M39/3 served also to document this tendency.

Following the WOCE Hydrographic Programme requirements, the section WHP-A2 along 
nominally 48ƒN was worked again as under "One - Time Survey" conditions. In 
addition to the classical hydrographic parameters, nutrients and small volume 
tracer concentrations were deter- mined. Continuous ADCP (Acoustic Doppler Current 
Profiler) data provided the absolute vertical current shear of the top 500 m to 
calculate, from geostrophic transports, the absolute transport through this 
section. Additionally, velocity profiles have been acquired using a LADCP to 
support calculations of the absolute velocities. With a horizontal station spacing 
between 5 and 35 nm, a 24x10 l - rosette system was deployed to collect at up to 36 
discreet depth levels water samples together with the quasi-continuous profiles of 
T, P, S and O2 with a CTDO2 -probe. The track and station spacing essentially 
follows the Gauss section from 1993, covering 66 stations with 86 casts. Some 
additional casts for performance tests of the CTD/rosette system, calibrations and 
for the instruments for the chemical analyses have been worked.

Since the summer 1996 a mooring array again covers over the full water depth the 
deep eastern boundary current on the west side of the Mid-Atlantic Ridge on A2. The 
velocity, temperature and salinity data will describe the long-term changes of this 
current system that seems to play an important role in the exchange of newly formed 
water masses such as the LSW within the ocean basin or across the ridge. The 
moorings were turned around for another deployment of one year to be recovered in 
the summer of 1998. There were no problems in locating, retrieving or setting the 
moorings.

3.1.1.2 WOCE-NORD

The second part of leg M39/5 was part of the WOCE-NORD project funded by BMBF and 
was the sixth repeat of the WHP section A1E/AR7E. Meridional transports of heat and 
matter in the North Atlantic will be quantified through a section connecting 
Ireland and South Greenland. This section runs south of the region where the 
atmospheric forcing transforms the water advected to high latitudes such that it 
will sink to greater depths and spreads further south, forming the source water 
masses of the North Atlantic Deep Water. For several years we have been observing a 
cooling trend in the LSW caused by the spreading of newly formed LSW in the 
Labrador Sea. Estimates of circulation times derived by linking single LSW 
vintages, using hydrographic and tracer data independently, lead to trans-Atlantic 
propagation times of 4 to 5.5 years from the source region to the West European 
Basin. During the second part of leg M39/5 the A1E/AR7E section was sampled 
successfully.

3.1.2	Nutrients and tracer measurements during WOCE cruises
a) Nutrients along the WHP section A2

Along the WHP section A2 the nutrients PO4, NO3, NO2, NH4, Si(OH)4 and the content 
of dissolved oxygen O2 from all water samples were determined to differentiate 
water masses and their origin.

From 1591 water samples nutrients and dissolved oxygen were determined on board 
according to the WHP Standards. For quality assurance purposes additional samples 
were taken as duplicates or replicates. All data will be processed on board, 
subjected to detailed consistency and quality checks and compared to existing data 
sets from this region. An annotated data file was produced at the end of the 
cruise, containing all relevant information and documentation on methodology and 
the quality of the data.

b) CFC's and helium/tritium on WHP section A2 and A1E

In addition to the classical hydrographic data the measurements of anthropogenic 
tracers provide additional parameters for water mass analysis. They are 
particularly important for the determination of water mass transports and mixing 
processes making use of their well-known time-dependent input history at the ocean 
surface.

As on the A2-survey in 1994 (M30/2) measurements were carried out for the 
determination of the CFCs F-11, F-12, F-113, and CCl4 and samples for the 
laboratory measurements of helium isotopes and tritium have been taken.

Since most of these tracers provide transient signals, the main objective will be 
to measure their time dependence. The hydrographic parameters for the mainly 
stationary flowing water masses like NADW or the deep waters of the eastern basin 
will not show much changes. But the tracer concentrations (except possibly for 
tritium) of these waters are expected to increase. The differences in tracer 
concentrations from these two cruises and the knowledge of the different input 
histories will allow us to determine the age structure of these water masses. The 
age structure is caused by mixing of waters of different age within a water mass, a 
process hardly detectable by hydrographic parameters. The "width" of the age 
structure gives an indication of the turbulent exchange coefficient, a parameter of 
general interest.

We expect further information on the intrusion of younger water from the north 
close to the bottom in the eastern basin which has been seen on the previous 
cruises M30/2 and further north during M18. This water is in contrast to older 
waters coming from the south as an eastern boundary current.

The highest tracer concentrations for NADW are expected in the western boundary 
current. The extension in zonal direction to and across the Mid Atlantic Ridge 
(recirculation) is easily detectable by the tracers. The LSW has changed its 
characteristic properties during the last years. To determine the development of 
these changes will be an objective of the cruise. The tracer concentrations will 
help to identify and to date the changes in the LSW.

The CFCs on section A2 were measured on the majority of the water samples. Helium 
and tritium sampling was restricted to about every second station, but with a high 
vertical resolution. The CFC data were available in preliminary form within about 
24 h after sampling, so that they served to assist selecting sampling depths 
further on.

The CFC distributions in 1991 and 1994 along WHP section A1 led to estimates of the 
spreading times of LSW into the Irminger Sea and into the Northeast Atlantic, which 
were significantly shorter than previously thought. They correspond, however, with 
estimates derived independently from the cooling signal of LSW.

The CFC analysis at M39/5 did continue the CFC time series of the deep water 
masses. In combination with the analysis at M39/2 and M39/4 the spreading and 
mixing of the deep water masses in the subpolar North Atlantic will be studied.

c) TCO2 and total alkalinity measurements on WHP section A2

Measurements were made of total dissolved inorganic carbon (TCO2) and total 
alkalinity from full water column profiles collected along 48ƒN. At least one full 
profile (36 samples) was analyzed each day. TCO2 was analyzed using a SOMMA-
coulometer system that belongs to IfM Kiel; total alkalinity was measured by 
potentiometric titration (open cell titration) again using equipment which belongs 
to IfM Kiel. Certified Reference Materials for these parameters was analyzed daily.

With accurate preliminary hydrographic data provided to the analysts at the 
completion of the cruise, a final TCO2 and alkalinity data set was made available 
for incorporation into the cruise data file.

The CO2 measurements will be used for the following purposes:

(1) The zonal section of TCO2 measurements will be combined with estimates of 
baroclinic, barotropic and Ekman water transport across the section to estimate the 
meridional transport of inorganic carbon at this latitude. These estimates should 
assist with the delineation of large scale patterns of divergence or convergence of 
the inorganic carbon transport in the North Atlantic ocean. These patterns in turn 
can be used as important constraints for large scale ocean carbon cycle models. 
Previous work during METEOR cruise M30/2 in 1994 has shown strong contrasts between 
waters from the source regions further to the North and particularly the deep 
Eastern Basin which was CO2 free. We expect, because of the observed large changes 
in the intermediate waters in the 1990s, considerable changes of the CO2 budget 
during this 1997 cruise.

(2) The observed TCO2 can be separated into anthropogenic and preindustrial 
components. Such a separation has been attempted for an earlier CO2 data set 
collected along this section and showed a large anthropogenic component penetrating 
to the ocean floor in the western basin and to approx. 4000 m in the eastern basin. 
However the influence of upper ocean seasonal changes can potentially obscure this 
anthropogenic signal: comparison of anthropogenic CO2 components estimated from 
data collected during November 1994 and summer, 1997 should allow the magnitude of 
this possible seasonal contamination of the anthropogenic CO2 signal to be 
addressed.

(3) TCO2 is remineralized at depth in the ocean together with nutrients and in 
association with the removal of dissolved oxygen: as a result there are very robust 
inter-relationships between dissolved oxygen, TCO2 and dissolved nutrient 
concentrations in the deep ocean. Whereas

Certified Reference Materials are available for quality control of measurements of 
the TCO2 content of seawater, there are unfortunately no such standards for 
nutrients or oxygen. The observed empirical relationships between TCO2 and the 
other parameters should, however, remain constant in the deep ocean for periods of 
at least several years to decades. Hence comparison of the quality controlled TCO2 
data with measured nutrients and oxygen concentrations provides one means by which 
the internal consistency of nutrient and oxygen measurements made on different 
cruises can be assessed. Simply put, any inaccuracies in the measurement of 
nutrients (for example) would show up as offsets or slope changes in the TCO2 -
nutrient plots derived from various cruises. Hence measurement of TCO2, because it 
is a parameter that can be traced to a Certified Standard, provides a means by 
which the quality of other closely related chemical parameter measurements can be 
assessed.

3.2	Sonderforschungsbereich (SFB) 460

The research program of the SFB is based on a combination of physical-
oceanographic, marine chemistry and meteorological observation programs, which are 
carried out in close interaction with a series of numerical models with moderate 
(50 km), high (15 km) and very high resolution (5 km), which will allow a 
simulation of current structures and variability over a wide range of space and 
time scales. The main interests during the first SFB phase are, first of all, the 
water mass formation processes and the circulation of deep waters in the subpolar 
North Atlantic, their interaction and integral effects, especially with regard to 
the uptake of anthropogenic CO2. Second, the variability of the ocean - atmosphere 
interaction is investigated, and modeling investigations of large-scale aspects and 
causes of this variability are supplemented by the analysis of fluxes from 
different meteorological standard models in comparison with observations, with 
emphasis on the fresh water exchange.

3.2.1	Physical Oceanography during SFB cruises

The western subpolar North Atlantic is a critical region for the climate of the 
North Atlantic region. Here, strong water mass transformations take place, with 
far-reaching consequences. This region is formation as well as transformation 
region of cold water masses, which are exported and as a consequence require 
northward compensating flow of warm water masses. The deep western boundary 
current, fed by the Denmark-Strait-Overflow at the lowest level and by the Deep 
Water from the Gibbs-Fracture-Zone above, flows along the topography in the 
Labrador Sea and continues past the Grand Banks. Indications exist for a deep 
cyclonic recirculation cell located between the Grand Banks and the Mid-Atlantic 
Ridge, its physical explanation is still unclear.

The work on leg M39/2 was related to subproject A3 of the SFB 460. The project 
focus deals with the variability of water masses of the subpolar gyre during their 
passage through the Iceland Basin. Some critical data gaps in observations east of 
the Reykjanes Ridge and at the depth level of the eastward spreading Labrador Sea 
Water could be closed. Data collection was concentrated on seven hydrographic 
sections cutting through the Iceland Basin and the western European Basin. With one 
exception all were oriented near-zonally between 60ƒ and 52ƒN, i.e. between WOCE 
sections A1 and A2. The latter was occupied again during legs 3 and 5 of METEOR 
cruise 39. Detailed CTD surveys and the deployment of current meters and RAFOS 
floats were conducted for long-term observations of Overflow and Labrador Sea 
Water. The distribution of temperature, salinity, nutrients and CFC tracers were 
mapped by four sections across the subpolar gyre in the central eastern basin. 
Properties of Labrador Sea Deep and Overflow Water from the Iceland Faroer Ridge 
were of importance for the survey. In addition to the section work, two low-energy 
signal generators and the first RAFOS floats were deployed.

Further work was concentrated at the Middle Atlantic Ridge, where detailed 
investigation of the spreading paths and transports of overflow water approaching 
the Gibbs Fracture Zone was conducted. In addition to a number of short 
hydrographic sections, a group of three current meter moorings, which also include 
a third signal generator, were deployed. Traditional RAFOS floats and, for the 
first time, a float park was deployed. The latter array contains a number of 
independent floats temporarily moored at the sea floor. They will leave their fixed 
position in a delayed mode after the METEOR has left the site. After release from 
their moorings these floats ascend to their mission level (appr. 1500 m) of the 
Labrador Sea Water. The purpose of the float park is to provide a Lagrangian time 
series of the inflow of Labrador Sea Water into the Iceland Basin. Float missions 
amount between one and two years.

The SFB program in the northwestern Atlantic began with a "Valdivia"-cruise in 
summer 1996 and was continued with cruise M39/4. A main water mass of the 
investigation during M39/4 was the Labrador Sea Water. After its formation in late 
winter in the central Labrador Sea it seems to circulate along complicated paths in 
the western basin and crosses the Mid-Atlantic Ridge far into the eastern basin. 
Only much later the LSW export to the south within the deep western boundary 
current takes place. The LSW seems to participate also in the recirculation east of 
the Grand Banks.

Large differences might exist between different years. Further, the flow paths of 
the LSW are not continuous, but its spreading paths are actually made up by a 
complicated interaction of eddy transport and mean advection. Until recently it was 
believed that the exchange of LSW with the water masses of the Irminger Sea takes 
place on time scales of several years, but recent measurements within WOCE 
indicated that the LSW can progress within less than a year far into the Irminger 
Sea.

Recent investigations indicate that convection takes place not only in the central 
Labrador Sea, but also at its southern margin. The water mass formed there seems to 
make up the upper part of the deep water export south of New Foundland, and as 
tracer data show, it moves there faster and more directly than the LSW. In 
addition, the possibility of convection in the Irminger Sea cannot be excluded. In 
late winter surface-mixed layers of more than 600 m appear regularly in the 
Irminger Sea, which forms the Subpolar Mode Water of the North Atlantic. So far, 
deep convection in this region could not be proved.

The main objective of leg M39/4 was the investigation of the different paths of the 
deep water circulation in the western subpolar basin of the North Atlantic and its 
water mass distribution.

Especially the focus was on the outflow of Labrador Sea Water into the western 
basin and its recirculation. To investigate the water mass transports, profiling 
current measurements from the ship by the ADCP lowered with the CTD (LADCP) were 
made. To characterize the water masses, CTD-hydrography and tracer measurements 
(Freon) and tritium/helium and 18O as well as nutrients and CO2 measurements were 
carried out.

To investigate small scale convection processes ("plumes"), ADCP moorings were 
deployed in the convection regions of the central and southern Labrador Sea. To 
measure the integral effects of convection, acoustic tomography was used.

The deployment of the Deep Labrador Current (DLC) array was one of the major 
objectives of project A4 of the SFB 460. The array is designed to determine the 
transports of the DLC south of Hamilton Bank. The array is oriented perpendicular 
to the continental slope near 52ƒ51'N, 51ƒ36'W and then northeastward. There the 
topography is very steep and the measurements from summer 1996 (Valdivia 161) 
showed a well defined DLC. In addition to the current meters and ADCPs the array 
also contains several conductivity/temperature probes (SEACATs) to monitor the 
water mass characteristics in key layers.

3.2.2	Air-sea fluxes

The meteorological aim in the SFB 460 is the investigation of air-sea interaction 
parameters in the Labrador Sea. Especially the focus is on the variability of 
surface fluxes and their feedback with ocean deep convection events in this region. 
The comparison of model results, field experiments and satellite remote sensing 
data should lead to a better understanding of variability of air-sea fluxes on 
different time scales.

The METEOR cruise M39/4 was the second field experiment in the context of the SFB 
460 in the Labrador Sea region. Data under meteorological winter conditions were 
sampled on a cruise on the RV Knorr during February and March 1997. The 
meteorological program on cruise M39 was divided up in two parts. The first part 
was the collection of data for the eddy correlation calculation of air-sea fluxes. 
For this purpose high resolution time series of three dimensional wind components, 
air temperature and humidity are necessary. The second part of the program was to 
get atmospheric data for the improvement and development of air-sea flux algorithms 
for satellite remote sensing applications.

3.2.3	Carbon dioxide system, oxygen, nutrients during SFB-cruises

The determination of the carbon dioxide system parameters total dissolved inorganic 
carbon and alkalinity and their depth distribution is a prerequisite to understand 
the carbon cycle. While the nutrient concentrations determined in parallel are 
mainly used as indicators for water mass properties, the carbon parameters and 
dissolved oxygen values allow also for the calculation of uptake of anthropogenic 
carbon into the water column. A significant anthropogenic signal even at greater 
depth is expected for the study area where the transport of anthropogenic carbon 
into the Deep Water is achieved mainly through the thermohaline circulation. 
Another aspect of air- sea carbon exchange is the CO2 partial pressure difference 
between surface seawater and the atmosphere. This difference indicates the degree 
of saturation of the surface waters and allows for the calculation of momentary 
air-sea exchange fluxes.

On the second and fourth leg of the METEOR cruise 39, the depth distribution of the 
parameters total dissolved inorganic carbon, alkalinity, nutrient- and dissolved 
oxygen concentrations were measured at the hydrocast locations. One aspect also was 
the determination of a baseline to detect variations in later studies within the 
SFB. In parallel, an automated system to measure CO2 partial pressure in atmosphere 
and surface seawater was run during the whole length of both legs.

3.3	Other programs
3.3.1	VEINS programs

VEINS (Variability of Exchanges in the Northern Seas) is an EU-MAST III programme 
to measure and model the variability of fluxes of water, heat and dissolved matters 
between the Arctic Ocean and the North Atlantic over a period of three years. It is 
aimed at developing an efficient observation design to measure time series 
resolving up to decadal time scales which are considered crucial for advancing our 
predictive capabilities for shorter term climate changes. For this purpose VEINS 
covers four key regions with recording current meters and repeat hydrography. One 
of these regions is the Denmark Strait (including the Greenland continental slope 
to the southwest) which was the working area for cruise METEOR 39/5. Here Atlantic 
input (Irminger Current) and output of polar surface waters (East-Greenland 
Current) as well as Arctic deep water (overflow) are the components of the exchange 
between the North Atlantic and the Seas of high latitudes. The measurements east of 
Greenland during the first part of leg M39/5 were carried out in the context of 
VEINS. Forty-three hydrographic stations were taken, six current meter moorings and 
two Inverted Echo Sounders (IES) were deployed and four moorings and one IES were 
recovered.

3.3.2	Tracer sampling

a) Helium/Tritium An extended sample set for on-shore analysis of helium isotopes, 
tritium concentrations and oxygen isotopes was collected along the cruise tracks of 
M39/4 and M39/5. In addition to the classical hydrographic parameters these tracer 
data will provide additional information for water mass analysis: making use of 
their well known time-dependent input history at the ocean surface the 
helium/tritium distribution will be used to estimate apparent 3H/3He ages of the 
prominent water masses and to determine spreading times and mixing rates. In 
particular, the interpretation of different tracer distributions characterized by 
different input histories (such as 3H/3He and CFCs) allows to describe mixing 
processes and to determine the age structure of the water masses. Interpretation of 
the tritium/helium data obtained will be done in context to the tracer information 
accomplished during former occupations of the area and will especially refer to the 
investigations performed during the WOCE cruises M18 (1991) and M30/3 (1994).

Use of 18O/16O ratios as oceanographic tracer is based on the fact that isotopic 
fractionation processes during evaporation and condensation lead to a typical _18O 
signature of different oceanic reservoirs. The _18O analysis allows to separate 
fresh water components e.g. arctic run-off transported by polar water or 
contributions of melted ice derived from the Greenland ice-shield. A total of 400 
samples for helium isotope and tritium analyses was taken along the cruise track 
M39/4. The vertical and horizontal resolution of the sampling grid was determined 
by the topography and the dynamic structures of the water column. Special focus was 
on the distribution of the Labrador Sea Water as well as on the deep boundary 
currents resulting in a dense station coverage at the shelf sections of the track 
(off Labrador, off SW Greenland, off Cape Farewell and off Flemish Cap). Another 
focus was on the Gibbs Fracture Zone outflow. The helium isotope and tritium 
analyses will be performed using a sectorfield mass spectrometer at the IUP in 
Heidelberg. In addition, a total of 145 samples for 18O/16O analyses was collected 
along the cruise track of M39/4. Samples were taken in the upper 600 m of the water 
column focusing on sections marked by surface boundary currents. The analytical 
work will be done on shore at the IUP (Heidelberg) after the cruise.

b) delta 18O

As supplement to the tritium, helium and 18O/16O samples taken by the Institut f¸r 
Umweltphysik Heidelberg oxygen-18 (18O) samples were taken during leg M39/4 for two 
other groups. 18O samples were taken for Robert Houghton at the Lamont Earth 
Observatory U.S.A. at the legs M39/4 and also M39/5 and for Tim Winters at the 
University of East Anglia, U.K. during M39/ 4. 18O samples for Robert Houghton were 
taken during M39/4 at 6 short near coastal stations of the upper 200 m at the 
Labrador and Greenland coasts and of the Flemish Cap. In collaboration with Rick 
Fairbanks, Houghton studies the freshwater balance along the northeast continental 
margin from Labrador to Georges Bank using oxygen isotope analysis to trace 
freshwater sources. In the Labrador Sea they are attempting to resolve conflicting 
estimates of the relative importance of freshwater input via the Baffin Basin and 
the West Greenland Current.

The 18O samples for Tim Winters were taken at the AR7 section from Labrador to West 
Greenland and for a short section at the southeastern shelf of Greenland over the 
full depth range. The samples are for measuring the 18O content of the water in the 
Labrador Sea. Winters will use an unmixing model to quantify the amounts of the 
various components of NADW as it flows south in the Deep Western Boundary Current 
through 50ƒN. It is intended to utilize 18O content of the water as an extra 
conservative parameter to identify the relative amounts of source waters in the 
NADW.

3.3.3	Methane

The overall goal of the methane program is to understand the nature of various 
processes that influence the distribution of this dissolved gas in the ocean. 
Methane appears to be slowly consumed in deep waters by oxidation and its 
concentration in old deep waters is very low. Sources include exchange with the 
atmosphere, production in the upper few hundred meters of the ocean by a biological 
process that is not fully understood, and bottom sources where hydrothermal and 
cold vents occur. In connection with the first of these, the concentration of 
methane in the atmosphere has varied over time. Proxy measurements made in ice 
cores indicate that over the last 200 years, the atmospheric methane has risen from 
about 700 to 1800 ppb volume, and, on a percentage basis, the rise has accelerated 
during the last decades at a rate faster than the rise of atmospheric CO2. As has 
already been observed in other transient tracers such as tritium and 
chlorofluorocarbons, the changing atmospheric concentration should result in a time 
dependent net input of methane to the ocean, the signature of which should be 
observable in recently formed deep waters.

Since the majority of the ocean's deep water is produced in the northern Atlantic, 
it is an area where the changing atmospheric exchange should influence the 
distribution of methane most strongly. Research objectives include determination of 
the concentrations of the dissolved CH4 in the various water masses of the 
northwestern Atlantic, particularly in the various sources of North Atlantic Deep 
Water, and determination of the 13C/12C isotope ratio of the dissolved methane. The 
isotope measurements should provide an indication of the extent of the methane 
decrease in the water column that is due to oxidation, because this process 
consumes the lighter isotope preferentially. In contrast, the carbon isotope ratio 
of methane in the atmosphere has remained nearly constant over time, and changes in 
the distribution due to varying atmospheric concentration should not strongly 
affect the isotope ratio in the ocean.

Discrete CH4 Measurements

Measurements of the dissolved methane concentration in the water column were made 
from the hydrocast collections during M39/2 and M39/4. In order to conduct these 
measurements, a new procedure for separating the gas phase from the water was 
employed. Water from the Niskin bottles is drawn into a 200 ml glass syringe 
without contact to the air. The syringe is then connected to an evacuated 500 ml 
bottle. As the water is drawn into this bottle from the syringe, most of the 
dissolved gas separates from the liquid phase. Altogether, 400 ml of water from 2 
syringes is added to each bottle. The gas is now led into an evacuated burette by 
injecting a degassed brine into the bottom of the sample through a sidearm at 
atmospheric pressure. At this point, 1 ml of gas is extracted and injected into a 
gas chromatograph equipped with a flame ionization detector.

The gas remaining in the burette is collected in an evacuated vial for carbon 
isotopic analysis by mass spectrometry ashore. In addition to the gas samples, on a 
few stations separate water samples were collected in air free bottles, and these 
will be returned to the shore-based laboratory for carbon isotope analysis. The 
dissolved gas in these samples will be stripped using helium, and the trapped 
methane injected directly into the mass spectrometer. These isotope measurements 
will be compared to those on the already separated gas samples.

Surface Water pCH4

Since deep waters are formed from surface waters, one needs to observe whether the 
atmosphere does indeed tightly control the methane concentration in the open ocean 
where this formation occurs. The partial pressure of methane in the surface layer 
of the ocean as well as in the atmosphere was surveyed continuously underway with a 
gas equilibrator connected to a pump 5 meters below the water line. A sample of the 
air recirculated in the equilibrator is periodically shunted into a gas 
chromatograph equipped with a flame-ionization detector. Both the methane and the 
CO2 partial pressure were measured, the latter by catalytic conversion to methane. 
These measurements were also carried out continuously on air pumped from overtop 
the bridge into the wet lab. The apparatus provides a semi-continuous measurement 
of the partial pressures in the water every twenty minutes and atmospheric 
measurements every 40 minutes.

3.3.4	Foraminifera (delta-13C and delta-18O data in foraminifera)

The isotopic signal of carbonate shells of planktonic foraminifera is used to 
deduce water mass temperatures or climatic changes in the past. However, without 
knowledge of the influence of biological factors on the isotopic composition of 
these shells, there is considerable latitude for false interpretation of the data.

Therefore plankton samples at different sites of leg M39/4 should give more 
information about horizontal and vertical distribution patterns, calcification 
depth and population dynamics of the foraminifera, Neogloboquadrina pachyderma 
(sin.) (Ehrenberg), an important species in palaeo- oceanography. The values of 
delta-13C and delta-18O of the foraminifera shells can then be compared with values 
of the water.

Some specimens of N. pachyderma (sin.) will be used for culture experiments under 
controlled temperature and food conditions in order to gain a paleo-temperature-
equation for low temperature ranges.

On 18 different stations in polar and subpolar water masses plankton samples were 
taken with a multinet at specific depth intervals (500-300 m, 300-200 m, 200-100 m, 
100-50 m, 50-0m). These samples were preserved in ethanol for later inspection.

4 samples were taken for culture experiments. The foraminifera of the species N. 
pachyderma (sin.) were sorted out and held in cell wells containing filtered sea 
water at a temperature of 4ƒC (similar to natural environment) Culture medium was 
changed every week and food (fresh algae cells about 20-64 µm in diameter) was 
added once a week. The culture experiments themselves will start immediately 
following this expedition.

3.4	Paleoceanography

The scientific program of R/V METEOR cruise M39/1 concentrated on the history of 
the North Atlantic's thermohaline circulation during the last glacial period. A 
primary cruise objective was to monitor the evolution of Mediterranean Outflow 
Water that today constitutes an important hydrographic component for North Atlantic 
mid-depth waters. Of special interest were short- term climatic anomalies that 
occurred sporadically during the last ice age and their effects on the regional 
circulation. Temperatures in the North Atlantic region rose between 2ƒ and 7ƒC 
during these abrupt climatic shifts, and remained high for several 100 to 1000 
years. Then they dropped back abruptly - within few 10-100 years - to ínormal' ice 
age values. These anomalies caused distinctive changes in the North Atlantic's 
thermohaline circulation: melt water surges flooded the North Atlantic and resulted 
in an almost complete shut-down of surface water convection and deep water 
formation. The oceanographic signals that were caused by these anomalies reached 
the Portuguese margin. Further interest concentrated on benthic growth habitats and 
carbonate production at the Iberian shelf and Gulf of Cadiz which may serve as an 
example of extra- tropical carbonate production.

R/V METEOR cruise M39/1 consisted of acoustic surveys of sediment drifts in the 
Gulf of Cadiz, and a sampling program including sediment sampling along depth 
transects immediately west of the Gibraltar Strait and at the western Iberian 
margin as well as plankton hauls and hydrocasts. Shorebased sedimentological and 
geochemical analyses that will be carried out post- cruise will provide data that 
are needed to decipher the history of climate change and ocean variability in the 
northeastern Atlantic in association with changes of climate and ocean circulation 
in the northern North Atlantic and the Mediterranean Sea.

The intended paleoceanographic and paleoclimatic research depends critically on the 
quality of the sediment samples. Acoustic surveys that map the sea floor topography 
and the internal structure of the upper sediment layers are essential to locate 
coring positions that are suitable for this research and provide continuous and 
undisturbed sediment records. The combination of R/V METEOR's Hydrosweep and 
Parasound systems allows integrative mapping of topography and sediment structure 
which is an important prerequisite to reconstruct current-induced sediment 
redeposition and erosion, and to detect current patterns - e.g., of Mediterranean 
Outflow Water in the Gulf of Cadiz. Paleoceanographic proxy-records to be 
established by using M39/1 sediment samples will include a wide range of 
biological-micropaleontological and organic and inorganic geochemical parameters. 
The most viable paleoceanographic proxies are benthic and planktonic foraminiferal 
community structures, stable oxygen and carbon isotope composition of benthic and 
planktonic foraminiferal shells and foraminiferal trace element composition that 
all trace various physical and chemical oceanographic parameters.

Interpretation of paleo-oceanographic time series requires knowledge about how 
tightly individual proxies are linked to environmental parameters such as water 
temperature and salinity, and nutrient concentration. To gain better control on the 
sediment data, continuous water column temperature and salinity profiles as well as 
profiles of trace element and nutrient concentration provide ground-truth data 
bases that are essential for calibrating the paleoceanographic proxy- records. 
Hydrographic surveys using CTD-probes in conjunction with water sampling bottles25 
and separate sets of clean GoFlo bottles for trace-metal water sampling were thus a 
central research program of R/V METEOR cruise M39/1.

3.4.1	Water Column Profiling: Ground-Truth Data Base for Calibration of 
	Paleoceanographic Proxies

The hydrography of deeper water masses at the Portuguese margin is defined by the 
advection of North Atlantic Central Water (NACW), Mediterranean Outflow Water 
(MOW), upper and lower North Atlantic Deep Water (NADW), and Antarctic Bottom Water 
(AABW) (HARVEY and THEODOROU, 1986; McCARTNEY, 1992; SCHMITZ and McCARTNEY, 1993). 
MOW is the most outstanding hydrographic component in that it comprises a prominent 
salinity maximum. MOW today enters the North Atlantic with temperature-salinity (T-
S) values of 13ƒC/38.4 (HOWE, 1982;, 1975; AMBAR et al., 1976). Potential density 
of this water is around 37.4 (s 2 =density on 2000 dbar surface), i.e. considerably 
higher than that of 36.7 for North Atlantic Deep Water (NADW). Rapid mixing with 
less saline North Atlantic Central Water (T-S=13ƒ/35.6; ZENK (1975)) and Labrador 
Sea Water (LSW, a component of upper NADW; T-S=3ƒ/34.85; TALLEY and McCARTNEY 
(1982)) that both flow at the depth level of MOW reduces the density of MOW so that 
it flows northward along the upper Portuguese Margin in an upper (750 m) and lower 
(1250 m) core layer (ZENK and ARMI, 1990). Immediately west of the Gulf of Cadiz, 
T-S values for upper and lower MOW are around 12.5ƒ/36.2 and 11.5ƒ/36.4, 
respectively; northward advection (compared to the 2000 dbar surface) in the upper 
layer is highest, around 2.73 Sv (1 Sverdrup = 106 m3 s-1), compared to 1.24 Sv in 
the lower layer (ZENK and ARMI, 1990).

The paleoceanographic evolution of deeper water masses in the Northeast Atlantic 
has been reconstructed by mapping benthic foraminiferal stable carbon isotope 
ratios from sediment cores at the Northeast Atlantic continental margin, the open 
North Atlantic, and the Norwegian- Greenland Seas (BOYLE and KEIGWIN, 1987; ZAHN et 
al., 1987; DUPLESSY et al., 1988; VEUM et al., 1992; OPPO and LEHMANN, 1993; 
SARNTHEIN et al., 1994; JUNG, 1996). These studies infer enhanced ventilation of 
the mid-depth North Atlantic, in response to the formation of a Glacial North 
Atlantic Intermediate Water (GNAIW, sensu DUPLESSY et al. (1988)) or enhanced 
formation of Upper North Atlantic Deep Water at the expense of Lower North Atlantic 
Deep Water (BOYLE and KEIGWIN, 1987; SARNTHEIN et al., 1994). Northward advance of 
AABW far into the northern North Atlantic caused significantly decreased 
ventilation there at depths below 3500. The net result of the reorganization of 
vertical water mass architecture in the North Atlantic was a steeper vertical 
gradient of biologically cycled nutrients between nutrient depleted mid-depth and 
nutrient-enriched deep and bottom waters.

From this pattern it is concluded that during the last glacial the upper Portuguese 
margin, at water depth above 1500 m, was influenced by the presence of a well 
ventilated water mass. Enhanced glacial benthic carbon isotope levels at the upper 
Moroccan continental margin have been inferred to document a stronger influence of 
MOW on the North Atlantic mid-depth hydrography (ZAHN et al., 1987). This 
hypothesis has also been used to explain enhanced benthic carbon isotope values 
further north, at the Portuguese margin and the Rockall Plateau area in the open 
northern North Atlantic (SARNTHEIN et al., 1994; JUNG, 1996). Evaluating benthic 
oxygen isotope in view of equilibrium dc fractionation as a function of ambient 
water temperature and salinity, however, implies that MOW contribution must have 
been reduced during the last glacial, and that enhanced mid-depth ventilation at 
the Portuguese margin must have come from a North Atlantic source, similar to 
today's North Atlantic Central Water (ZAHN et al., 1997).

An important aspect of the M39/1 paleoceanographic work was to collect water column 
data that will serve as an oceanographic ground-truth data base to better define 
the paleoceanographic proxy-signals of MOW close to the Strait of Gibraltar i.e., 
prior to large-scale mixing of MOW with Atlantic waters. T-S profiles in 
conjunction with water column oxygen, phosphorus and stable oxygen and carbon 
isotope analyses (as well as water column trace element analysis; see below) will 
serve as a modern control for the interpretation of paleoceanographic proxy records 
and their interpretation in terms of glacial-interglacial changes in physical 
circulation and regional nutrient inventories. To obtain high-quality water samples 
from paleoceanographically important depth intervals, CTD-derived T-S profiles in 
conjunction with Rosette and GoFlo water sampling were a central scientific 
objective of M39/1.

3.4.2	Plankton in Surface Waters off Portugal

Plankton organisms represent the base of the marine trophic chain. Seasonally 
varying abundances indicate varying bio productivity at the sea surface. During 
settling to the sea floor, the plankton assemblage changes mainly due to grazing 
and shell dissolution. Moreover, lateral advection of plankton organisms by ocean 
currents might as well affect the sedimentary assemblage. A comparative study of 
plankton at the sea surface and in surface sediments was carried out to shed light 
on the loss of primary produced material and the loss of species during settling. 
Analysis of living and the dead (fossil) assemblages and documentation of the 
autochtonous plankton signal in surface waters and underlying sediments, as well as 
an evaluation of MOW- related advection/transport of allochtonous plankton was thus 
an important objective of the cruise.

3.4.3	Benthic Foraminifera: Faunal Composition and Stable Isotopes

Benthic foraminiferal studies are part of an ongoing research project on late 
Quaternary water mass patterns at the western Iberian margin. Main objectives are 
to document (i) the impact of sporadic North Atlantic melt water events on water 
mass stratification and advection in the northeastern Atlantic during the late 
Quaternary and (ii) the dynamics of the Mediterranean Outflow Water (MOW) during 
the last glacial, deglacial, and Holocene. Benthic carbon isotope data from the 
western Iberian margin document distinct anomalies that are coeval with glacial 
melt water events in the open North Atlantic (ZAHN et al., 1997). The data imply 
that the hydrographic response to sporadic collapses of thermohaline overturn in 
the northern North Atlantic was felt outside the immediate region of maximum melt 
water fluxes i.e., at the Portuguese margin, and may have been of ocean-wide 
importance. Detailed evaluation of water mass patterns during these events is 
hindered by a lack of information on the advection history of MOW during the melt 
water pulses. M39/1 was designed to retrieve sediment cores close enough to the 
Strait of Gibraltar to allow for the documentation of MOW flow in that the proxy-
records would trace the source signal of Mediterranean waters at their entrance 
into the North Atlantic. The benthic foraminiferal community structure also shows 
distinct changes of faunistic constituents that are coeval with periods of sporadic 
thermohaline spin-down (Baas et al., submitted). The faunistic proxies closely 
complement the isotope data. They need to be refined and calibrated with 
oceanographic data to corroborate reconstructions of glacial and deglacial deep-
water circulation from benthic isotopes (KAIHO, 1994; BAAS et al., submitted). An 
epibenthic foraminiferal association indicative of recent current MOW advection off 
southern Portugal is to be traced further towards the MOW source in the Gulf of 
Cadiz to monitor the response of the biota to higher current strength. The study 
also needs to be extended further to the north to document the correlation between 
epibenthic foraminiferal assemblages and the spreading of MOW (SCH÷NFELD, 1997). 
New surface samples and sediment cores from suitable locations are needed to fill 
in gaps in the present data sets which inhibit a conclusive interpretation and 
application of foraminiferal faunal and isotope proxies. Sediment sampling is 
complemented by water column measurements of oxygen concentration, nutrients, 
stable isotopes, temperature and salinity of near-bottom waters to provide 
environmental data for calibration.

An important aspect of this work is the potential influence of pore water chemistry 
on benthic foraminiferal assemblages. The faunal composition of benthic 
foraminiferal assemblages in surface sediments is closely linked to organic carbon 
fluxes to the seafloor (ALTENBACH, 1985; LUTZE and COULBORN, 1984; ALTENBACH et 
al., 1989). A relation to oxygen concentrations of ambient bottom waters is also 
indicated (KOUTSOUKOS et al., 1990; HERMELIN, 1992; ALVE, 1995). Species adapted to 
dysoxic conditions such as Globobulimina affinis and Chilostomella ovoidea commonly 
prefer a deep endobenthic microhabitat (CORLISS, 1985), but they appear close to 
the sediment surface in regions of low-oxic bottom waters and/or of high flux rates 
of organic matter (HARMAN, 1964; MULLINEAUX and LOHMANN, 1981). A detailed 
examination of the relation between dysoxic species and pore-water oxygen levels 
will help to discern the impacts of both environmental factors (LOUBERE, 1997). 
Only few studies report on depth habitats of Globobulimina and oxygen 
concentrations in ambient pore waters (REIMERS et al., 1992). This is mainly 
reflects the fact that micropaleontological studies and geochemical measurements 
are rarely carried on the same sets of sediment samples. Our strategy is to provide 
in situ oxygen data for the same samples that will be used later for analysis of 
the benthic foraminiferal fauna. For the porewater oxygen measurements we use an 
oxygen needle-probe and determine pore-water oxygen concentrations in subsurface 
sediments of that multicorer tube, which was later sampled for benthic 
foraminiferal depth-habitat studies.

3.4.4	Trace Fossils and Bioturbation as Indicators of Paleo-Environmental 
	Conditions

Trace fossil assemblages are related to environmental conditions at the 
sediment/water interface e.g., temperature, salinity, oxygen and nutrient 
concentrations, sediment stability and grain size. Thus, a comparative study of 
trace fossil assemblages at different water depths is carried out to improve their 
paleoceanographic application. In particular, the relation of trace fossil changes 
to MOW-advection changes e.g., in the course of glacial-interglacial climatic 
cycles, will be studied. The primary intention is to revise and improve the concept 
of trace fossils as monitors of environmental change.

3.4.5	Temperate Water Carbonates

Modern and late Quaternary changes of biogenic carbonate production and carbonate 
accumulation are investigated at the western Iberian continental shelf and margin, 
and in the Gulf of Cadiz. The response of benthic carbonate organisms to 
environmental factors such as productivity of surface waters, terrigenous sediment 
input and redeposition and their relation to the global state of climate are 
studied. Warm temperate carbonate shelf sediments that are formed under variable 
upwelling regimes are compared to carbonate sediments in temperate, high boreal, 
and subarctic shelf settings.

3.4.6	Trace Metals in Calcareous Microorganisms as Paleoceanographic Tracers
a) Cadmium

The distribution of dissolved cadmium is globally correlated with the distribution 
of biologically cycled nutrients (BOYLE, 1988; FREW and HUNTER, 1992) and is used 
in paleoceanographic studies in conjunction with benthic delta-13C data as an 
independent tool to reconstruct past ocean circulation patterns and nutrient 
inventories (BOYLE, 1994). The great potential of cadmium as a paleoceanographic 
proxy comes from the fact that - in contrast to delta-13C - Cd is cycled within the 
ocean only and no ioexternallr pathways are know (except for leaching at some 
continental slope deposits; FREW, 1995). The ocean carbon cycle, on the other hand, 
also involves air-sea gas exchange which is associated with carbon isotope 
fractionation (BROECKER and MAIER- REIMER, 1992). In high latitudes, the isotope 
fractionation during outgassing or carbon uptake may exceed the biologically-driven 
iiRedfieldly delta-13C fractionation and severely hamper extraction of nutrient 
information from paleoceanographic delta-13C data sets. Cd is not involved in air-
sea fluxes and thus, it is considered a faithful recorder of ocean nutrient cycling 
(ZAHN and KEIR, 1994). Apparent disparities between benthic foraminiferal Cd and 
delta-13C signals thus bear information on water mass source regions and can be 
used in paleo-ocean circulation studies as conservative tracers for water mass 
tracking (LYNCH-STIEGLITZ et al., 1996).

Basin-wide compilation of benthic foraminiferal delta-13C from glacial sections of 
North Atlantic sediment cores documents large-scale changes in the regional water 
mass pattern that went along with changes in northern North Atlantic surface ocean 
conditions (DUPLESSY et al., 1988; SARNTHEIN et al., 1994). The principal change 
was a shift in depth of the core layer from 3000 m to around 2000 m during the last 
glacial in response to enhanced buoyancy of convecting water masses. Only in the 
immediate vicinity of convection, i.e. north of 45ƒN, did the influence of newly-
convected deep waters reach water depths similar to today (SARNTHEIN et al., 1994). 
At depths below 3000 m, depleted benthic delta-13C values signify an enhanced 
influx of a chemically aged water mass of presumably Southern Ocean origin 
(DUPLESSY et al., 1988; SARNTHEIN et al., 1994). Benthic delta-13C records from the 
upper Portuguese margin, at water depths of 1000-1200 m, display distinct negative 
anomalies that were associated with sporadic melt water events (ZAHN, 1997; ZAHN et 
al., 1997). The data imply a rapid slow-down of thermohaline circulation in the 
North Atlantic during these events. Benthic foraminiferal Cd records imply 
increased nutrient concentrations in ambient mid-depth waters during these periods 
and thus confirm convective slow-down. The data, however, are inconclusive as to 
whether these "old" waters originated from the southern hemisphere (e.g., a glacial 
Antarctic Intermediate Water) or whether limited convection still occurred in the 
northern North Atlantic.

Water column cadmium analysis in conjunction with the determination of oxygen and 
phosphorus concentrations was a primary scientific objective of M39/1. The data are 
intended to provide information on regional Cd distribution in the Gulf of Cadiz 
and at the western Iberian margin that would allow to calibrate the Cd-to-P 
relation in the northeastern Atlantic. Special emphasis is on MOW in terms of Cd 
and nutrients concentrations to better constrain the paleoceanographic patterns 
observed in sediment cores from the upper Portuguese and Moroccan margins.

b) Strontium, Magnesium

The general objective of this project is to test and improve the application of 
Sr/Ca and Mg/Ca records of calcareous planktonic and benthic microorganisms as 
proxies for paleoceanographic reconstructions. Aspects to be addressed are i) 
processes which determine the uptake of trace metals during biomineralisation in 
the water column; ii) the influence of diagenetic alteration on trace metal 
composition of fossil carbonate shells; iii) chemical variability during climatic 
changes. The western Iberian margin is well suited for these investigations, 
because: (i) distinct variations of surface water temperature during glacial-
interglacial times are documented from the N-Atlantic (BOND et al., 1993), changes 
that should also be documented in the Mg/Ca signals of planktonic foraminifera off 
Iberia; (ii) sporadic glacial melt water events documented by ice-rafted detritus 
and temperature anomalies (BOND et al., 1992, 1993; MASLIN et al., 1995) induced 
severe changes in the surface hydrography. Due to a insensivity of the Mg/Ca-ratio 
to minor salinity changes (NÐRNBERG et al., 1996a), Mg/Ca-time series should 
primarily reflect temperatures changes, and thus, should help to detect melt water 
events when compared to delta-18O -data. (iii) Fluctuation of the late Pleistocene 
Mediterranean outflow, that are documented in marked temperature and salinity 
anomalies (ZAHN et al., 1987), should have caused distinct chemical signals in the 
shells of benthic ostracods. The Western Iberian continental slope will therefore 
serve for a case study to test whether the temperature reconstruction from Mg/Ca-
ratios can compete against conventional temperature reconstructions based on stable 
oxygen isotopes and/ or faunal analysis. Furthermore, the characteristic MOW water 
properties should be clearly depicted in the shell chemistry of benthic ostracods. 
A primary goal is to study the relationship between foraminiferal Sr/Ca ratios and 
Sr-depletion in surface waters to improve the potential of foraminiferal Sr record 
as paleoceanographic tools. Comparison of trace metal concentration in seawater and 
benthic ostracods will elucidate if MOW carries a characteristic Mg/Ca signal, and 
if the signal is picked up by benthic organisms.

3.4.7	Sediment Geochemistry and Mineralogy

The Gulf of Cadiz has been one of the most interesting research areas for the ICM 
Marine Geology group of Barcelona. In this area, geophysical, geochemical, 
sedimentological and stratigraphic studies have been carried out, which resulted in 
a dense grid of seismic profiles and a large number of sediment cores of the 
eastern part. Here, gas-charged sediments and seafloor pockmarks-like features were 
recognized on the slope area and described in BARAZA and ERCILLA (1996). 
Furthermore, this work will focus on the impact of the Mediterranean Outflow on the 
sea floor, e.g. formation of contourites and sea floor bed forms. These processes 
are either linked to changes of sea level or the strength of the undercurrent 
itself (NELSON et al., 1993). Moreover, geochemical studies will be carried out to 
improve our understanding of contamination of suspended particles and surface 
sediments by heavy metals from mining factories, and its relationship to modern 
sedimentary processes of the area (PALANQUES et al., 1995; VAN GEEN et al., 1997).

The overall intention is, to study the paleoclimatic record in Pleistocene-Holocene 
sediments, based on different mineralogical and geochemical parameters. 
Mineralogically, smectite apparently offers a great paleoceanographic potential. 
Today, smectite is discharged through the Guedalquiver River into the Gulf of 
Cadiz, partially even into the Alboran Sea (AUFFRET et al., 1974; GROUSSET et al., 
1988; BOZZANO, 1996). Variations of this clay mineral, as recorded in the Alboran 
Sea cores possibly depend on changes of the Atlantic inflow during the past, a 
hypothesis, which we intend to verify with sediment cores from the Gulf of Cadiz. 
An important objective of this study is to follow the path of the smectite track 
from the Atlantic into the Mediterranean, and improve our understanding of the 
oceanographic constraints implied in this transfer process.

The main objectives of the geochemical study are to characterize the conditions of 
past sea surface waters in the Gulf of Cadiz. Based on a high-resolution biomarker 
studies, the paleoceanographic response in the Gulf of Cadiz to rapid climatic 
changes in the North Atlantic should be depicted. A second objective is to compare 
records from the Gulf of Cadiz and the Alboran Sea to elucidate the impact of the 
inflowing Atlantic water on water mass dynamics in the Alboran Sea. Finally, the 
Gulf of Cadiz, the Alboran Sea and the Agadir zone are ideally suited for a 
prospective study of slope-sediment instability. P-wave velocity, density and 
magnetic susceptibility of regional sediments will also be studied.

4	NARRATIVE OF THE CRUISE
4.1	Leg M39/1 (R. Zahn)

The M39/1 scientific party arrived in Las Palmas on 16 April 1997. After the ISO 
9002 certification of R/V METEOR was successfully completed, all scientists 
embarked R/V METEOR the next day. On April 18, 09:00, R/V METEOR left Las Palmas 
and headed north-north-east to the Gulf of Cadiz. After a transit of 53 hours in 
good weather and calm seas we reached our first working area in the outer Gulf of 
Cadiz (Figure 2). Functionality and handling trials were successfully run with the 
full suite of sediment sampling devices and the CTD/Rosette. During the following 
10 days, extensive PARASOUND and HYDROSWEEP surveys were carried out that were 
followed by sediment and water sampling at 29 sites. The sampling sites were 
targeted to cover the depth ranges of North Atlantic Central Water, MOW, upper 
North Atlantic Deep Water (NADW) and uppermost lower NADW. Spectacular temperature 
and salinity profiles were collected across the MOW flow path at four hydrographic 
stations and water samples were collected to measure stable isotope, nutrient and 
trace element compositions of the key water masses.

The second half of the cruise was devoted to sediment and water sampling along the 
western Iberian margin. 48 sampling stations between Cabo Sao Vincente in the south 
to Cabo Finisterre up north at water depths from 20 m to >3000 m were occupied. The 
shallow stations on the shelf were designed to recover surface carbonate sediments 
which are to be used to estimated the carbonate production potential on the 
Portuguese shelf and its influence on the sedimentary regime of the upper 
continental slope. Core log profiles, namely magnetic susceptibility and color 
reflectance, along sediment cores from the upper and central slope revealed quasi-
cyclic changes of sediment properties that could tentatively be correlated with 
high-frequency climatic oscillations known from Greenland ice cores. Distinctive 
positive anomalies in the susceptibility logs further indicated the sporadic 
incursion of ice rafted debris horizons which have already been documented in 
sediment cores that were collected during earlier cruises to the area. The 
scientific program of M39/1 was completed on 10 May, 13:00. After a 41 hour 
transit, R/V METEOR arrived in Brest in the early morning hours of 12 May. In 
total, 78 stations were occupied during the cruise and a rich collection of water 
and sediment samples, and of hydroacoustic profiles were retrieved. As such, the 
cruise was successful in that all major scientific objectives were achieved. This 
success to no small extent was made possible by the ship's master, Kapit”n Dirk 
Kalthoff, his officers and the crew who cooperatively collaborated with the 
scientists and made our work possible even under difficult conditions. To all of 
them we owe our sincere thanks.

We are also indebted to the Portuguese and Spanish governments for granting us 
clearance to carry out our scientific work in their national waters. In particular, 
we appreciate the good collaboration with the Portuguese naval command and the 
Spanish ship traffic control that made it possible for us to work in intricate 
terrain such as major ship traffic areas and at near-shore, shallow water sampling 
sites.

Fig. 2:	Location map of M39/1 sediment and water sampling sites in the Gulf of Cadiz 
	and at the western Iberian margin.

4.2	Leg M39/2 Brest - Cork (W. Zenk)

On the evening of the 13 May an informal reception was held for the participants of 
an Eurofloat meeting at IFREMER together with a number of local representatives 
from IFREMER and from the Service Hydrographique et Oceanographique de la Marine 
(SHOM).

On the afternoon of the 14th, the majority of cruise participants arrived in Brest 
and installation of equipment on board started immediately. After initial testing 
of the chemical instrumentation and of various computer systems was successfully 
concluded, the METEOR left Brest at 14:00. The next two days we sailed for the 
starting point of our scientific mission on the northwestern shelf edge of Ireland 
north of Porcupine Bank. This location was reached on the morning of May 17 on Sta. 
200 (see chapter 7, list 7.2.1). An essential test station had been occupied the 
day before. Starting from the continental slope, METEOR cruised straight (306ƒ) 
towards the Middle Atlantic Ridge, crossing Rockall Trough, Rockall Bank, and Maury 
Channel in the Central Iceland Basin (Fig. 3). This first hydrographic Sect. A 
(Sta. 200-224) was paralleled by a second (B) positioned 230 km southwestward 
between the Ridge and the southern flank of the Hutton Bank (Sta. 225-232). A third 
section (C) followed subsequently. It brought us back to the Middle Atlantic Ridge 
north of Charles Gibbs Fracture Zone (Sta. 240) where METEOR arrived on May 28.

On the initial Sections A-C, 40 full depth CTD stations were occupied, those at 
Maury Channel (215, 230, 234) being the deepest. With the exception of four 
stations during strong gale conditions on Sect. A the CTD system included a rosette 
sampler (RO) and an acoustic Doppler current profiler (LADCP). Two interruptions in 
the CTD work were necessary to launch moorings IM1 and IM2 (see list 7.2.2). They 
contain low-energy signal generators, an essential infrastructure for the 
application of the RAFOS technology (see Fig. 5). Nine RAFOS floats were launched 
up to May 26 (see list 7.2.3). Over the following 12-24 months they will monitor 
the spreading of Labrador Sea Water in the Iceland Basin at approximately 1500 m 
depth.

After reaching Sta.240 we set course on a fourth section (D) with CTD stations 243, 
242, 244, 249, 245-248 (see Fig. 3). The non-monotonic station sequence over this 
section was the result of the difficult weather conditions in the northern West 
European Basin. It is positioned just north of Charlie Gibbs Fracture Zone where we 
expected the Overflow Water to still be confined to the eastern flanks of the 
Reykjanes Ridge before escaping westward through the fracture zone into the 
Irminger Sea. For this reason, we deployed three current meter moorings (V386, V 
387, and V388 [IM3] see list 7.2.2) at this gateway. The array hosts 13 recording 
instruments and a further RAFOS generator at the depth of the Labrador Sea Water 
and at several levels below within the Overflow Water. From these long-term current 
observations we expect continuous records of transport fluctuations at intermediate 
and near-bottom depths at Gibbs Fracture Zone, the major conduit for water mass 
exchange in the central North Atlantic.

These efforts were be complemented by the installation of 'Float Park North' at 
Sta. 245, where four RAFOS floats were launched from the METEOR. While one of them 
descended to its mission depth, the rest have been temporarily moored at the bottom 
(3170 m) for 2, 4, and 6 months, respectively. The stepped delays of the three new 
dual-release floats will enable us to establish a modest Lagrangian time-series at 
the entrance of mid-depth water masses into the eastern basin (Fig. 4). The latter 
is a major research topic of the initiative SFB 460 of the University of Kiel. It 
features the dynamics of the thermohaline circulation variability, thought to be 
relevant for climate variability.

Fig. 3:	Geographical setting of METEOR cruise 39/2. Capital letters denominate 
	sections. Hydrographic stations (cf. list 7.2.1) are shown as circles. Stars 
	represent RAFOS float launch positions (cf. list 7.2.3). Dots stand for 
	mooring locations (cf. list 7.2.2).

Fig. 4:	Principle of the "Float Park" deployed during METEOR cruise 39/2. During 
	phase 1 RAFOS floats with dual-releases are moored temporarily at the 
	bottom. Phase 2 begins with the anchor release. It enables floats to reach 
	their mission level at the Labrador Sea Water (LSW) plume. Finally they drop 
	their balast weight (phase 3), return to the surface and transmit their 
	recorded data. For mission lengths see Table 7.2.3.

After we had lost more than a day due to unfavorable weather conditions with three 
attempts to occupy Sta. 245 at mooring V387, METEOR cruised towards the Gibbs 
Fracture Zone on 31 May, where a meridional hydrographic section (E) on 35ƒW was 
occupied. It consisted of seven closely spaced deep CTD stations (250-256) and was 
finished early in the morning on 2 June. Then, METEOR proceeded eastward, initially 
cutting through the Middle Atlantic Ridge at a nominal latitude of 51ƒN. During the 
next two days until 4 June, Sect. F consisting of Sta. 256 to 264, was completed. 
On Sta. 261, 'Float Park South' was installed (see Fig. 5 and 6). Again, it 
contains four RAFOS floats of which only one drifts immediately at its mission 
depth while the rest of the group remains anchored for the next 3, 6, and 9 months. 
We expect the combination of Sections D, E and F to allow a synoptic budget of the 
transports of Overflow Waters at the 3- way junction 'Gibbs Fracture Zone'. 
Furthermore, it is worth noting that the chemists on board detected elevated 
methane concentrations in the rift valley at Sta. 260, which is situated at the 
extension of the Middle Atlantic Ridge south of Gibbs Fracture Zone.

Fig. 5:	Deployment of RAFOS sound source (IfM Nr. V385) on Station 231.

Fig. 6:	Deployment of the CTD probe on Station 261 carrying a RAFOS float to be 
	moored temporarily in a float park on the ground.

The final Sect. G, with much widely spaced station intervals, was completed on 7 
June. It consists of Sta. 263, 265-271, connecting the Middle Atlantic Ridge with 
the western approaches of the British Isles. In the afternoon of 7 June, the 
hydrographic observations were terminated and the METEOR sailed towards Cork. All 
CTD stations, mooring and float deployments are compiled in lists 7.2.1, 7.2.2 and 
7.2.3.

While on passage to the western approaches of Ireland we contacted Prof. L. TALLEY 
from the Scripps Institution of Oceanography. She and her team had just started 
their hydrographic work aboard the research vessel KNORR. After the exchange of the 
latest information about our observations on the METEOR the American group on the 
KNORR considered an adjustment of their cruise track in order to optimize the 
hydrographic coverage of the Iceland Basin on a quasi- synoptic scale in early 
summer 1997. On an unexpected stop-over of the KNORR we missed our colleagues in 
the port of Cork by only a few hours.

METEOR cruise 39, leg 2, was completed in Cork, Ireland, on 8 June 1997. Because of 
tunnel construction work under the River Lee, METEOR had to stay the same day at 
the new ferry terminal outside of Cork. In the afternoon of the next day she moved 
to Tivoli pier, right in the centre of the city. Disembarkation of the scientific 
party had taken place at the container pier before reaching Tivoli pier.

4.3	Leg M39/3 (K. P. Koltermann)

METEOR sailed from Cork, Ireland on 11 June 1997 the single day of Irish weather we 
encountered in Ireland, rain. A test station (273) was worked on 12 June 1997 in 
more than 4300 m depth at 49ƒ30'W, 14ƒW. Tests of the 36 x 10 l Rosette were not 
successful. After finally testing the established 24 x 10 l rosette package 
successfully, a further test station was worked on stat. 274 on 3722 m of water to 
get blank values for the CFC measurements (274 KAL). The ship worked then the A2 
section (Figure 7) onto the European shelf towards East. At all station positions 
and halfway between stations XBT drop were added to the spatial resolution of the 
temperature field. In the mean time work on both the 36 x 10 l rosette and the DHI1 
CTD was continued. On 14 June 1997 after working the easternmost station of the 
section (stat. 282) the ship sailed for the position of the second test station 
(274) to finally take up the section work westward. We used mainly the 24x10 l 
rosette equipped for the L-ADCP on loan from IfM Kiel. No difficulties were 
encountered with either rosette, L-ADCP or the CTD NB3. In the mean time the repair 
work of the other CTDs, planned to be the main stay of this work, left us with the 
NB3, a MkIIIB and the BSH2 without an oxygen sensor, MKIIIC.

On 20 June 1997 with stat 302 we crossed the Mid-Atlantic Ridge MAR and worked this 
station at the deepest part of the Rift Valley. There we also deployed the first of 
three C-PALACE floats, #719. On 21 June the mooring K1 was successfully recovered 
and another mooring deployed. No damage or losses were incurred. After another 
hydro station at the site, section work was continued. C-PALACE #720 was deployed 
on 20 June at stat 304 on the west side of the MAR. The last C-PALACE #718 was 
successfully launched on 22 June at station 307. The next day the mooring K3 was 
recovered at dawn and a new mooring deployed. After reaching depths in excess of 
4100 m, on stations we deployed first the 24x10 l rosette B24 together with the CTD 
NB3 for a shallow cast to nominally 1200 m, followed by the deep cast with the 24 x 
10 l rosette K24 and the BSH2 CTD, that included the LADCP. Two bottle positions 
had been sacrificed to incorporate the LADCP. The deep North American Basin was 
crossed until 29 June. Single cast stations were resumed up the slope towards the 
tail of the Grand Banks. On 30 June 1997 the last station was worked at 59 m depth.

Rosette work, after settling in on the work packages, was only effected by 
leakages, slipped O-rings and occasionally leaking spittoons. These leakage 
problems were the only but quite numerous handicaps in the water sampling. At some 
time a re-definition of the starting position of the rosette trigger had to be 
checked and confirmed with deliberate firings on deck. Throughout the cruise, as on 
all other previous ones, we used the BIO sample numbering scheme. Again, all who 
did not have previous experiences adopted it right away.

After passage on 1 July towards St John's, Nfld, METEOR docked on 2 July, 1700 at 
pier 10. During the passage all wire work was concluded, the ship's measurement 
systems such as thermosalinograph, ADCP and underway measurements were stopped when 
passing the 50 nm limit of Canada.

Fig. 7:	Cruise track of METEOR cruise M39/3, WOCE Hydrographic section A2 between 
	Goban Spur on the Irish shelf and the Canadian Tail of the Grand Banks.

4.4	Leg M39/4 (F. Schott)

Since cruise leg M39/4 had as an essential objective the retrieval and redeployment 
of a variety of moorings, it had to be subdivided into two segments with an interim 
stop on 16 July in St. Anthony, in case last-minute repairs needed to be made on 
tomography transceivers or convection observing instrumentation. The cruise began 
in St. John's amidst festivities to celebrate the 500th anniversary of Cabot's 
crossing with the 'Matthews'. A Japanese TV camera team escorted the ship out of 
the port, filming for an educational channel; they passed along a camera to the 
METEOR for underway filming.

The first part of the cruise repeated the 'Valdivia' track of 1996, beginning north 
of Hamilton Bank along the WOCE line AR7 with retrieving moorings K2, K6 (Fig. 8) 
that had been deployed in August 1996 by 'Valdivia'. The moorings were both 
recovered on 8 July in good condition, thus alleviating fears that deep-reaching 
icebergs or shelf edge fishery might have jeopardized them. Across the boundary 
current 3 profiling ALACE floats (PALACE) were deployed to continue our Lagrangian 
observations across the boundary circulation that were started with deployment of 6 
PALACEs in February 1997 by the 'Knorr'. On 10 July, an Inverted Echosounder (IES) 
of URI was recovered under unfavourable conditions (insufficient acoustic tracking 
signals and fog). Working our way northwestward along AR 7 to tomography station 
K4, this mooring was recovered intact in the evening of 10 July, but two of its 
transponders only sent weak signals and did not release. Then a southwesterly 
course was taken, back to the Labrador shelf. On 12 July, tomography mooring K3 and 
its three navigation transponders were recovered and during 14-20 July the boundary 
current meter array K7-K16 (Fig. 8) was deployed, while at nighttime CTD/LADCP 
stations across the Labrador Current were taken. This time period was particularly 
intense for those of the scientific party dealing with the equipment, since many of 
the instruments to be used for these deployments (tomo-transceivers, acoustic 
releases, transponders, current meters, seacats) had to be turned around, after 
just having been retrieved. A special worry some problem was that the data 
evaluation of the tomographic stations just recovered indicated that there had been 
phases of large mooring inclinations. These were larger than experienced anywhere 
else, although the mean currents in the interior Labrador Sea were small. The 
effect appeared to be dominantly due to small-scale but deep-reaching energetic 
eddies, that slowly drifted by a mooring position. One remedy was to increase net 
buoyancy of the moorings to the absolute limit of wire breaking strength.

On 16 July this first part of M39/4 was terminated according to plan. The quality 
of the shipboard and lowered ADCP profiles was much improved by the significantly 
increased navigation accuracy that was made possible by the newly introduced 
GPS/GLONASS receiver. It reduced the scatter on the GPS positions noticeably, and 
thus even more on their derivatives which should constitute the ship's motion 
vector. The new 75 kHz shipboard ADCP had been successfully put to work and 
routinely yielded depth ranges of more than 500 m except under very rough sea state 
conditions. A system that did not satisfactorily work when we got on board was the 
Ashtech direction determination unit. Two reasons were discovered: First, the 
antenna locations are less than adequate for the purpose and second, a new firmware 
had been developed by the manufacturer that was not yet installed on the vessel. 
When we received that by e-mail, the data return improved drastically.

The interim stop in St. Anthony allowed the exchange of a number of personnel (3 
departing, 7 coming) and gave a welcome break for those aboard, which was used for 
an outing to a Viking settlement ('L'Anse aux Meadows'). From St. Anthony METEOR 
headed northward for deployment of tomography mooring K17 and of the moored cycling 
CTD (K15, Fig. 8). After deployment of tomography mooring K17 with the heavy HLF-5 
sound source it turned out that the station did not operate properly. In the night 
the mooring was picked up again, a highly commendable effort by the crew who had by 
now been up and working for long hours. After installation of K15 and K17 this time 
with a Webb transceiver on 20 July the ship headed to the southeastern end of the 
WOCE line. Tomography/convection moorings K12 and K11 (Fig. 8) were deployed on 
21/22 July and the last of the deployments was K14 on 23 July.

The northern boundary circulation was then investigated with 4 CTD/LADCP stations 
across the northern end of the WOCE-AR7 line whereupon the ship transited to Cape 
Farewell, past a beautiful scenery of icebergs and ice floes occupied by seals, to 
begin profiling the meridional section along 43.5ƒW. That meridional section away 
from the boundary was filled with energetic mesoscale eddies, but in order to have 
enough time for sampling the Gibbs Fracture Zone (GFZ) through flow and the other 
deep boundary currents, fairly wide station spacing had to be used until reaching 
Flemish Cap. There the Labrador Sea Water was found to circulate southeastward 
offshore, separated by a front from the "Northeast Corner" of the North Atlantic 
Current. After another connection section to 35ƒW, the investigation of the GFZ was 
begun on 1 August with increasingly closely spaced stations until reaching the main 
cross-connecting valley. On this approach, the Hydrosweep bottom observations taken 
on M39/2 could well be used for station planning, even more so since rough weather 
degraded the quality of our own soundings. The interesting result of that small-
scale survey was that much through flow also seems to originate in a valley a few 
km north of the main cross roads.

Following the axis of the Mid-Atlantic Ridge (MAR) northward it was found that it 
carries a deep valley along its crest that might play a role in the interbasin 
exchange through openings of other cross-ridge valleys in the north. On 6 August, 
the final transect was begun, running from the MAR to the Greenland coast just 
north of Cape Farewell (Fig. 8). Dense station spacing across the topographic 
slopes on both sides covered the deep boundary circulation. This last phase of the 
work was hampered by strong head wind. The station work was terminated in the night 
of 8/9 August and the transit to Iceland was commenced. After weeks and weeks of 
westward winds along this track the winds were now from the northeast, delaying our 
advance to port somewhat unexpectedly. Leg M39/4 had accomplished its objectives 
and ended around noon of 11 August in Reykjavik.

Fig. 8:	Cruise track and station map of METEOR leg M39/4.

4.5	Leg M39/5 (A. Sy)

After three days in Reykjavik to exchange the scientific staff and set up the 
laboratory installations, R.V. METEOR sailed from Reykjavik (Iceland) on 14 August, 
09:00 UTC heading for the startup position at 64ƒ45'N, 26ƒ40'W (stat. # 451; Fig. 
9). Station work began the same day. The dense station spacing in conjunction with 
quiet weather facilitated the establishment of the necessary station work routine. 
We worked 5 short sections down the Greenland slope which covers the range from the 
cold and fresh East Greenland Current of polar origin to the warm and saline 
Atlantic water of the Irminger Sea (Fig. 10). During the VEINS part of our 
programme, which was finished on 24 August, 23:30 UTC (stat # 505), we worked 43 
CTD/L-ADCP/Rosette stations, deployed 6 current meter moorings, 2 inverted echo 
sounders (IES) and recovered 4 moorings and one IES (see station listing 7.5.1, 
Fig. 9). Unfortunately, the recovery (dredging) of 5 moorings deployed in 1995 and 
1996 failed. Stat. # 505 was also used as a test station for a performance check of 
all 3 CTD systems available.

CTD station work was resumed on 25 August at 07:00 UTC at the western end of the 
WOCE section A1/E on the eastern Greenland shelf at 60ƒN, 42.5ƒW. Because wind and 
sea conditions (see section 6.5) were moderate throughout, and we encountered no 
serious technical problems, station work proceeded fast and without any 
interruptions until 6 September. We were thus in the favourable position of having 
time to spare, which we used for two additional sections. These were orientated 
normal to the WOCE section from Eriador Seamount to Hecate Seamount (stat # 537 - 
549) and from Lorien Bank to East Thulean Rise (stat # 558 - 563).

From 6 September, 17:00 UTC to 8 September, 04:30 UTC, station work had to be 
interrupted for the recovery of an ill crew member by an Irish rescue helicopter 
(MRCC Dublin). After that action and a detour of 360 nm, station work was resumed 
and the WOCE section was completed successfully on 9 September, 22:30 UTC. METEOR 
set course for the English Channel and reached Hamburg on 14 September 1997, at 
10:00 LT.

Fig. 9:	positions of CTDO2/rosette stations for R.V. METEOR cruise M39/5.

Fig. 10:Irminger Sea SST with M39/5 CTD stations (sea surface temperature composed 
	from NOAA-12 and NOAA-14, 8.8.-27.8.97).

5	PRELIMINARY RESULTS
5.1	SFB 460
5.1.1	Physical Oceanography of the eastern Basin (M39/2)
5.1.1.1 Hydrography (S. Becker, B. Lenz, T.J. M¸ller, W. Zenk)

A CTD in combination with a rosette sampler (21x10 l bottles) for the analysis of 
dissolved oxygen and nutrients was used to investigate the structure of water 
masses on sections (see Fig. 3) in The Iceland Basin north of 50ƒN. The water 
masses are:

*	Subpolar Mode Water (SPMW)
*	North Atlantic Central Water (NACW)
*	Intermediate Water (IW)
*	Mediterranean Water (MW)
*	Labrador Sea Water (LSW)
*	Lower Deep Water (LDW)
*	Iceland Scotland Overflow Water (ISOW)
*	North East Atlantic Deep Water (NEADW)
*	Antarctic Bottom Water (AABW) Fig. 11 shows the potential temperature 
	salinity (theta/S) relation in four selected regions:
*	Western European Basin (WE)
*	Rockall Trough (RT)
*	Northwestern Iceland Basin (NI)
*	Charlie Gibbs Fracture Zone (GF)

Three representative stations per region are plotted for each of the above regions. 
Surface and mode water vary between 9 and 15ƒC in potential temperature theta and 
35.0-35.7 in salinity S (Fig. 11a). Remainders of NACW occupy the main thermocline. 
Traces of Mediterranean Water are most prominent in the Western European Basin, 
with core salinities S>35.4. Isolated lenses of this water mass were found in 
Rockall Trough and even in the northwestern corner of the Iceland Basin. The base 
of NACW range overlaps with IW which primarily is identified by low oxygen (O2) and 
high nitrate (NO3) concentrations (VAN AKEN and DE BOER, 1995), and which is found 
at approximately 7-8ƒC in the relations of theta/O2 (Fig. 12) and theta/NO3 (not 
shown here).

The deeper water masses can be identified more clearly in for theta<4ƒC in Fig. 
11b. The minimum salinity in the core of the LSW is found in the Gibbs Fracture 
Zone (S-min=34.87). Also, LSW is coldest in this region, and with theta<2.95ƒC), 
its temperature is well below that observed by SY et al. (1997) who found minimum 
temperatures on WOCE section A2 (48ƒN) of 3.20ƒC one year before. The cold 
(theta<2.5ƒC), salty (S>34.96) and oxygen-rich ISOW like LSW shows pronounced 
horizontal gradients. Being almost at the same density as ISOW, LDW is marked by 
higher salinity and nutrients. In silica, e.g., the concentrations in water with 
high amount of LDW are about three times larger (> 45 µmol/l) than those for with 
high amounts of ISOW (< 18 µmol/l, Fig. 13). Note that in the deep Rockall Trough 
phosphate contents are relatively high when compared to the other regions in terms 
of the Redfield ratio (Fig. 14).

Fig. 11a:Potential temperature (q) salinity diagram from 4 representative regions 
	in the Iceland Basin. Their locations are shown in Fig. 3: WE-Western 
	European Basin (Sta. 267-269), NI-northern Iceland Basin (Sta. 216-218), RT-
	Rockall Trough (Sta. 203-205), and GF-Charlie Gibbs Fracture Zone (Sta. 254-
	256). Lines of equal density are shown as sigma-theta (kg m-3)-isolines. 
	Subpolar Mode Water (SPMW) primarily is found in the southwestern region of 
	the basin (GF), North Atlantic Central Water (NACW) is restricted to the 
	more easterly located regions off the European shelf and likewise the 
	remainders of the Mediterranean Water (MW) with their clear intermediate 
	salinity maximum. A subset of these stations with theta±4ƒC are shown in 
	Fig. 11b. Data are based on CTD stations from M39/2, equally spaced at 10 
	dbar.

Fig. 11b:Enlarged theta/S diagram for theta æ 4ƒC inferred from Fig. 11a (box). 
	Water masses of the Cold Water Sphere can be identified: LSW at sigma-
	1.5=34.7 kg m-3 is characterized by its clear minimum in salinity. While 
	progressing eastward through Gibb Fracture (SY et al., 1997) it mixes with 
	SPMW, resulting in a systematic increase of temperature and salinity 
	(arrow). Below LSW we encounter LDW penetrating into the Western European 
	Basins as an eastern boundary current derived from AABW (theta æ 2ƒC). At 
	comparable density levels we find ISOW on the flanks of the Reykjanes Ridge 
	in the NW corner of the basin. As this water mass follows the Ridge, it 
	mixes horizontally contributing to the NEADW formation.

Fig. 12:theta/O2 diagram from rosette samples from CTD stations indicated in Fig. 
	11a. Remainders of local deep winter convection result in highly ventilated 
	water masses of the thermocline, SPMW. Additional highs in O2 are found in 
	the LSW and the ISOW. The deepest water masses in the east have their origin 
	in remainders of AABW, called LDW. Lowest O2 values were encountered in the 
	Western European Basin where VAN AKEN and DE BOER (1995) define their 
	Intermediate Water (IW) at theta ~ 8ƒC.

Fig. 13:At the surface SiO4 is a deficit nutrient salt. The most distinct signal was 
	encountered in the LDW. Values > 40 µmol/kg identify clearly their origin in 
	AABW source waters. Some minor amount is advected through Gibbs Fracture 
	(>17 µmol/kg).

We briefly discuss two of the four sections (locations see Fig. 3) as examples: 
Section A from the northern edge of Porcupine Bank to the northern end of Reykjanes 
Ridge and section D which runs parallel to the array of current meter moorings.

At the thermocline level of the northern (ca. 58ƒN) section A (Fig. 15) we find the 
8ƒC-isotherm crossing the 250 m level as an indicator of the Subpolar Front which 
is closely related to the North Atlantic Current (KRAUSS, 1986). The thermal 
stratification decreases at the level of the Labrador Sea Water (1200-2000 dbar) 
where we also find the pronounced minimum in the _/S-relation. In the Iceland basin 
the associated core layer sinks from approximately 1200 dbar on the eastern flanks 
of the Reykjanes Ridge down to 1800 dbar above Maury Channel. Beneath the Labrador 
Sea Water we recognize the cold (theta < 2.9ƒC) and saline (S >34.96) contours of 
the Iceland Scotland Overflow Water. As expected, intermediate and bottom water 
parameters are absent in the Iceland Basin and less pronounced in the Rockall 
Trough.

Fig. 14:The Redfield ratio in the four test regions of the Iceland Basin. The slope 
	derived from all data excluding stations from the Rockall Trough (RT) is 
	12:1. Apparently the Rockall Trough is enriched by PO4.

We show the distribution of salinity, oxygen and silicate on Section D (Fig. 16) 
just north of Gibbs Fracture as background information for our current meter array 
(see Table 7.2.2 upper half). Current recording instruments are concentrated on the 
low saline and oxygen rich Labrador Sea Water and on the more saline Iceland 
Scotland Overflow Water which on its way southward has been already entrained by 
silicate-rich Northeastern Atlantic Deep Waters.

Fig. 15:Section A (see Fig. 3) at nominally 58ƒN showing the distribution of 
	potential temperature (a) and salinity (b).

Fig. 16:Distribution of salinity (a), oxygen (b) and silicate (c) on Section D (see 
	Fig. 3). Data (black dots) were collected by the rosette sampler operated 
	jointly with the CTD probe. Overlaid circules represent locations of moored 
	current meters for the observation of deep boundary currents along Reykjanes 
	Ridge.

5.1.1.2 Freon Analysis (CFC) (O. Pl”hn)
Methods

During M39/2 about 1200 water samples have been measured on 66 CTD station to 
analyse the CFC components F11 and F12. About 10 to 25 ml of seawater are 
transferred from precleaned 10 L Niskin bottles to a purge and trap unit. The gases 
are separated on a gas chromatographic column and detected with an electron capture 
detector (ECD). Before and after each station, a calibration curve with 6 different 
gas volumes was taken. Assuming a linear drift between both calibrations, the ECD 
signals are converted into CFC concentrations.

The observed temporal variations of the ECD were very stable for the F12 component, 
whereas for F11 the observed variability was in the order of 30%. The mean blank of 
the sample transfer and the measurements procedure was determined by degassing CFC 
free water, produced by purging ECD clean Nitrogen permanently through 5 L 
seawater. The blanks were in the order of 0.004 pmol/kg for both components.

The accuracy was checked by analysing about 350 water samples twice or more. It was 
found to be 0.6% for CFC-11 and 0.7% for CFC-12. At some stations, the F12 peak was 
disturbed by a high N2O level of the samples. Air samples were taken regularly, to 
find possible contamination inside the vessel and to analyse the clean air outside 
the vessel. The saturation at the surface of both components was about 100%±5%.

Preliminary results

Along the first section (Ireland-Reykjanes Ridge) the lowest CFC concentrations -
less than 1 mol/kg for CFC-11- were measured at the bottom of the Rockall Trough. 
The high silicate concentration (>20 µmol/kg) at that region, leads to the 
assumption that this water comes partly from the southern hemisphere. Overflow 
water masses from the Arctic are not found at this trough, in contrast to the Maury 
Channel. In this deep basin a significant signal of Iceland Scotland Overflow Water 
(ISOW) was found at the bottom. The high CFC concentrations (CFC- 11>2.3 pmol/kg) 
correlate with salinity (>34.95). The small tongue of overflow water had an 
vertical extension of only 200 m, with a density of sig >27.87. Above the ISOW 
water with lower salinities (<34.95) and lower CFC-11 (<2 pmol/kg) are found. 
Whereas the concentrations of the CFC minimum increase to the north, with values of 
less than 1.6 pmol/kg (CFC-11) at the southwestern edge of the Rockall Bank.

Along the eastern flank of the Reykjanes Ridge, ISOW spreads southward, with a mean 
CFC-11 signal of 2.5 pmol/kg at 60ƒN. Along its pathway the concentration 
decreases, and perpendicular to the flow direction, the concentration gradient 
increase. In the flow through the Charlie-Gibbs-Fracture-Zone, the CFC-11 
concentration was 2.3 pmol/kg in the core of the ISOW, at the northern edge of the 
fracture zone.

The largest freon signal of the LSW was measured southwest of the Charlie-Gibbs-
Fracture- Zone with concentrations of more than 3.2 pmol/kg. Spreading eastwards 
this strong signal decreases steadily. In the density range between 27.75 and 
27.78, the average CFC-11 concentration was less than 2 pmol/kg in the Rockall 
Trough and about 2.7 pmol/kg in the Iceland Basin. Due to vertical mixing along the 
Reykjanes Ridge, in some profiles no concentration maximum could be observed. Along 
the 51ƒN section the LSW signal was observed east of 15ƒW, marked by oxygen and 
CFC-11 maxima.

5.1.1.3 Carbon Dioxide System, Nutrients and Oxygen (A. K–rtzinger) 
a) Background

The ever increasing demands of our expanding human population have led to 
considerable anthropogenic emissions of greenhouse gases with carbon dioxide being 
the most prominent one. The well-known impact of these greenhouse gases on the 
radiative balance of our planet has brought the whole question of climate change 
into discussion. This problem has been fully recognized during the last decades and 
ambitious international research programs focusing on the different reservoirs of 
the global carbon cycle have been launched. The ocean has long since been 
identified as a significant sink of this anthropogenic or "excess" CO2. However, 
the marine carbon cycle with its complex coupling to physical, chemical and 
biological processes is still not fully understood. Reliable predictions of future 
climate change can only be achieved on the basis of a profound understanding of the 
natural carbon cycle, the largest rapidly exchanging reservoir of which is the 
ocean.

The North Atlantic plays a major role in the climate system with its large air-sea 
exchange fluxes. This is not only true for heat and freshwater but also for carbon 
dioxide. With the downward moving limb of the global ocean conveyor being located 
in the North Atlantic Ocean this part of the world ocean seems to play a key role. 
While the mean ventilation of the ocean constitutes the main kinetic barrier for 
equilibration with the perturbed atmosphere, the North Atlantic provides a "window" 
of the deep ocean to the atmosphere which allows the excess CO2 to penetrate more 
rapidly. We have shown previously that the anthropogenic CO2 has penetrated through 
the entire water column down to depths of 5000 m in the western basin of the North 
Atlantic. The eastern basin still shows much deeper penetration (3000-4000 m) than 
anywhere else in the oceans. The new Sonderforschungsbereich 460 at the University 
of Kiel on the decadal variability of the thermohaline circulation is focusing on 
the formation and modification of deep and intermediate waters in the North 
Atlantic Ocean. As part of this ambitious program a marine chemistry project has 
been implemented to study the importance of the thermohaline circulation and its 
variability for the natural carbon cycle and the uptake of anthropogenic CO2. After 
completion of the WOCE-WHP section A2 in Nov 1994 (METEOR 30/2) this project has 
now started field work in the ocean domain of the new SFB 460.

b) Methods
Nutrient and Oxygen Measurements

Dissolved oxygen was measured based on a titration method first proposed by Winkler 
as described in GRASSHOFF et al. (1983). This method yields an accuracy of the 
order of 0.5 µmol/l.

Nutrient concentrations were measured photometrically after conversion of the 
analytes into colored substances as described in GRASSHOFF et al. (1983). All 
measurements were carried out with an Auto-Analyzer continuous flow technique. 
Estimated accuracy is 0.02 µmol/l for nitrite, 0.1 µmol/l for nitrate, 0.05 µmol/l 
for phosphate and 0.5 µmol/l for silicate.

Measurements of Carbon Dioxide System Parameters

The collection of extensive, reliable, oceanic carbon data is a key component of 
the Joint Global Ocean Flux Study (JGOFS) and has also been an important aspect of 
the World Ocean Circulation Experiment (WOCE). Based on these international efforts 
to understand the marine carbon cycle on a global scale, standard methods and 
operating procedures have been defined to allow for a global synthesis of the vast 
amount of data obtained. All carbon dioxide system measurements carried out during 
cruise M39/2 of R/V METEOR are based on such well-tested analytical methods and 
procedures as described in DOE (1994).

Unfortunately, the concentrations of the individual species of the carbon dioxide 
system in solution cannot be measured directly. There are, however, four parameters 
(i.e. CO2 partial pressure, pH value, total dissolved inorganic carbon, alkalinity) 
that can be measured. Together with knowledge of the thermodynamics involved any 
combination of two of these parameters can be used to obtain a complete description 
of the carbon dioxide system in seawater. Two different sampling strategies were 
followed during cruise M39/2. The first comprised continuous measurements of the 
partial pressure of CO2 in surface seawater and air along the cruise track. The 
second sampling strategy followed "classical" collection of water samples from 
hydrocasts along 7 transects for measurements of total dissolved inorganic carbon 
and alkalinity. This also included sampling at selected sites for measurements of 
the delta-13C value of the dissolved inorganic carbon.

Underway Measurements 

Profiles of the partial pressure of CO2 (pCO2) in surface seawater and overlying 
air were obtained with a newly designed, automated underway pCO2 system (K÷RTZINGER 
et al., 1996). This system has shown excellent agreement with another system 
developed at the Institute for Baltic Research in Warnem¸nde/Germany (ibid). 
Seawater was pumped from the moon pool of R/V METEOR by means of a submersible pump 
(ITT Flygt Pumpen GmbH, Langenhagen/ Germany) at a pump rate of about 30 L/min. The 
flow of about 2 L/min required for the analysis was teed-off close the 
equilibrator. In-situ temperature and salinity were measured at the seawater intake 
with a CTD probe (ECO, ME Meerestechnik Elektronik GmbH, Trappenkamp/Germany). 
Clean air was pumped from an intake on "monkey's island". The measurement routine 
comprised recalibration of the system every six hours using two standard gases with 
known CO2 concentrations in natural air prepared by the NOAA Climate Monitoring and 
Diagnostics Laboratory in Boulder, Colorado/U.S.A. as well as nitrogen as a zero 
gas. The resulting accuracy of the measurements is better than 1 ppm. Air was 
measured every hour for two minutes. All data were logged as 1-minute averages 
together with T/S data from the CTD as well as navigational data (position, speed 
and course over ground) from a separate GPS receiver.

The pCO2 data are corrected for the non-ideal behavior of CO2 (i.e. they are given 
as fugacity of CO2 or fCO2 ). They are also corrected back to in-situ temperature 
accounting for the slight warming during passage of the seawater to the system. All 
fCO2 values are calculated for 100% humidity at the air-sea interface to allow for 
direct flux calculations.

Discrete Measurements 

The total dissolved inorganic carbon content (CT) was measured using the so-called 
SOMMA system, which has become the standard method for a major part of the JGOFS 
and WOCE activities especially in the U.S. community. The system consists of an 
automated extraction unit with a coulometric detector (JOHNSON et al., 1993). It 
was calibrated with known amounts of pure CO2. The calibration was checked 
regularly (i.e. roughly every 15 samples) with certified reference material 
provided by Andrew Dickson from the Scripps Institution of Oceanography, Marine 
Physical Laboratory, La Jolla, California/U.S.A. The obtained precision is of the 
order of 0.5-1 µmol/kg. The achieved accuracy is better than 2 µmol/kg as judged 
from repeated measurements of the certified reference material.

The alkalinity (AT) was measured by potentiometric titration of a known volume of 
seawater with hydrochloric acid basically according to MILLERO et al. (1993), but 
carried out in an open vessel (VINDTA system, MINTROP (1996), unpubl.). The 
progress of titration was monitored using a glass electrode/reference electrode pH 
cell. Total alkalinity was computed from the titrant volume and the electromotoric 
force data using a least-squares procedure based on a non- linear curve fitting. 
The titration factor of the hydrochloric acid was measured at high accuracy by 
Andrew Dickson. The system was also checked regularly (i.e. roughly every 15 
samples) with the same certified reference material provided by Andrew Dickson. The 
precision as estimated from repeated measurements of the certified reference 
material was about 3 µmol/kg. Due to the lack of a superior reference method the 
accuracy of the method is difficult to estimate. It is probably of the order of 5 
µmol/kg.

c) First Glance at the Data
Sample Statistics

A total of 1209 samples from 64 stations were analyzed for nutrients (nitrate, 
nitrite, phosphate, silicate) and dissolved oxygen. A total of 529 samples from 30 
stations were analyzed for CT and AT. All systems operated throughout the cruise 
without any major problems or unusual quality restrictions.

The pCO2 system was also operated throughout the cruise with two minor exceptions, 
an initial delay (until May 26, 08:30 UTC) caused by computer problems and a short 
break (May 24, 21:00 UTC to May 25, 10:00 UTC) due to failure of the submersible 
pump. The total distance covered by these underway measurements of pCO2 (in 
seawater and air), temperature and salinity is about 3600 nm.

Underway Measurements 

The measured CO2 mole fraction in dry air ranged between 367 and 370 ppm for most 
of the cruise. An atmospheric temperature inversion encountered during May 16 close 
to the coast of Ireland was accompanied by increased atmospheric CO2 concentrations 
of up to 380 ppmv. This increase reflects the influence of CO2 from sources on the 
European continent accumulating under the inversion, which serves as a barrier for 
vertical mixing in the atmosphere. Due to the relative large observed range in 
barometric pressure (approx. 997-1026 hPa) the resulting atmospheric fCO2 is 
roughly 366±6 µatm.

The observed range of fCO2 in surface seawater is 260 to 360 µatm. Lowest values 
were found close to the Irish coast, probably due to the influence of riverine 
freshwater input. The fCO2 in seawater generally increased towards the west and 
highest values were found at the western ends of most transects. The covered area 
of the eastern North Atlantic Ocean has been found to serve as a significant sink 
for atmospheric CO2. In the eastern part this sink was as large as 60- 80 µatm 
difference between air and seawater fCO2 (êfCO2 ), which translates into large air-
to- sea fluxes of CO2 under the prevailing high wind stress (i.e. high transfer 
coefficients). Close to the Mid-Atlantic Ridge the sink was considerably smaller 
with a êfCO2 of 5-50 µatm and some areas close to equilibrium. The mean under-
saturation of surface waters along the cruise tracks was of the order of 30-40 
µatm. The temperature range between up to 15ƒC in the east and around 7ƒC in the 
west was not found to be the major driving force behind the general fCO2 patterns 
in surface waters. These more likely reflect the different "history" of the surface 
waters, i.e. their source region and contact time with the atmosphere.

These findings are in good agreement with the current understanding of the role of 
the North Atlantic in the global carbon cycle. Large volumes of surface waters are 
transported northwards through the Gulf Stream and the North Atlantic Current. 
These waters are strongly cooled during their passage hereby decreasing 
significantly their fCO2 due to the temperature dependant solubility of CO2. This 
process generates a strong under-saturation of surface waters which drives large 
air-sea exchange fluxes of CO2. Furthermore this effect can be strongly enhanced 
during spring bloom situations as marine phytoplankton take up CO2 during 
photosynthesis. An indication of such bloom situations was found at some locations 
in the eastern part of some transects. While chlorophyll measurements were not 
carried out during this cruise the strong changes in water colour give valuable 
hints for biological productivity.

Water Column Data

From the broad set of water column data only the vertical distribution of total 
dissolved inorganic carbon (CT) shall be discussed here briefly. A typical CT 
profile shows lowest values at the surface, where waters are generally not too far 
from equilibrium with the atmosphere. Below the surface mixed layer CT values 
increase with depth as a result of the remineralization of particulate organic 
carbon in the water column and the dissolution of particulate biogenic carbonates. 
The first process takes place in much shallower depths generating a CT maximum at 
depths of about 800-1200 m. The second process generally takes place much deeper 
depending on the depth of the lysocline of calcite (and aragonite). These are 
deepest in the North Atlantic Ocean (>4000 m for calcite) so that carbonate 
dissolution is a minor process and no significant CT increase from this source is 
found a greater depths.

The CT profiles of three stations (205, 251, 268) are shown in Fig. 17. Station 205 
is located on transect "A" in the Rockall Basin, station 251 on transect "E" in the 
Charly Gibbs Fracture Zone and station 268 on transect "G" in the eastern basin of 
the North Atlantic Ocean. The three profiles show quite different patterns. At 
station 205 the extreme depth of the winter mixed layer is still reflected in the 
profile. While a much more shallow mixed layer of around 100 m was present at the 
time sampling; CT values around 2132 µmol/kg at depths of 100-700 m represent the 
remains of the very deep winter mixing in this area. This can also been seen at 
station 268 at 100-400 m depth. The remineralization maximum is found at depths 
between 400 m (station 251) and 1200 m (station 205). Station 205 and 268 show a 
strong increase in CT values of up to 50 µmol/kg at depths greater than 2000 m. 
This is indicative of much older waters which carry a higher signal of respiratory 
CO2 and represent the northernmost extensions of the Antarctic Bottom Water. There 
is no comparable increase in the deep waters at station 251.

As the distribution of CT in the water is influenced by different processes 
(physical, chemical and biological) the presence of "excess" CO2 cannot be 
identified directly. There are, however, techniques to identify the anthropogenic 
fraction which makes up between 0 and 60 µmol/kg depending on the time of 
ventilation. It is assumed that overflow water found at the western ends of the 
transects and in the Charly Gibbs Fracture Zone as well as the recently formed 
Labrador Sea Water carry a higher anthropogenic CO2 signal. With the present data 
set we have a very good basis to understand the distribution of anthropogenic CO2 
in the eastern North Atlantic and to improve previous estimates of total inventory 
of anthropogenic CO2.

Fig. 17:Profiles of total dissolved inorganic carbon (CT) at three selected stations 
	of METEOR cruise M39/2. Stations are located on transect "A" in the Rockall 
	Basin (205), on transect "E" in the Charly Gibbs Fracture Zone (251) and on 
	transect "G" in eastern basin of the North Atlantic (268).

5.1.2	Physical Oceanography of the Labrador and Irminger Sea (M39/4)
5.1.2.1 Technical aspects
a) CTD analysis (L. Stramma, C. Mertens)

The CTD probe used was a Neil Brown Mark IIIB additional equipped with a Beckman 
oxygen sensor. It was attached to a 24 bottle 10 l General Oceanic rosette water 
sampler. As a LADCP was built into the rosette frame, a maximum of 22 bottles was 
used throughout the cruise. Five of the bottles were equipped with deep-sea 
reversing thermometers for temperature and pressure calibration.

Calibration of the pressure and temperature sensors was done at IfM Kiel in July 
1996 and April 1997. The thermometer readings were used to check the laboratory 
calibration of the pressure and temperature sensors. Within the accuracy of the 
reversing thermometers no deviations were found and no further correction to the 
laboratory calibration was applied.

The salinity samples, typically six per profile, were analysed with two Guildline 
Autosal Salinometers. The IfM Kiel AS4 showed some jumps within the salinometer 
readings and stable calibrations could be done only after the jump in the readings 
happened. Therefore, part of the time the BSH-3 salinometer was used, which showed 
a very stable calibration and no reading jumps. In the CTD salinity calibration the 
readings of both salinometers showed similar variations, hence the IfM Kiel AS4 
salinometer despite the reading jumps did not result in a reduced accuracy. The 
calibration of the CTD salinities was carried out with an rms-error of 0.0025 for 
leg M39/4. The oxygen samples were analyzed in the marine chemistry group with 
traditional Winkler titration. Typically samples were taken from all bottles on 
each station plus additional double samples at some stations. The CTD oxygen sensor 
had hardware problems in recording continuous oxygen current and oxygen temperature 
values and filled gaps by zero or low values. This problem could be solved within 
the software of the CTD processing and calibration routines.

Due to time dependant drift of the CTD oxygen sensor, the calibration was done for 
three individual periods. The rms-error for the oxygen sensor was 0.044ml/l for leg 
M39/4.

b) Mooring retrievals and deployments (J. Fischer, F. Schott)
Mooring retrievals

The mooring work began 8 July with the recovery of moorings K6 and K2 near the 
shelf break at Hamilton Bank. Inspection of the recovered mooring hardware showed 
almost no corrosion, confirming that it should be possible to extend deployment 
periods to two years. The recovered instruments were in good shape, and with the 
exception of one acoustic current meter all instruments (SEACATS, ADCPs and 
Thermistor Strings) returned a full data set. With the following recovery of the 
tomography moorings K4 and K3, and the recovery of moorings K1, K5 and L by RV 
Hudson a month before the METEOR cruise, all moorings were successfully recovered. 
All 5 ADCPs (including one in the Canadian í'BRAVO" mooring) returned 100% data. 
The FSI inductive temperature probes, used for the first time worked fairly well, 
and data gaps occurred only for those sensors mounted at great distance from the 
data logger.

Inspection of the depth records either by the ADCPs or the pressure sensors in the 
tomographic instruments showed periods of large vertical excursions. To reduce 
mooring motion we increased the net buoyancy in moorings K11, K12, K14 and K17 to 
more than 700 kp and increased the anchor weight to 2000 kp.

The Deep Labrador Current Array 1997/99

Mooring positions and deployment dates of the Deep Labrador Current (DLC) array are 
summarized in table 4. The instruments (current meters, ADCPs and SEACATs) were 
programmed for two years duration, with the exception of the instruments in mooring 
K9 which will be recovered summer 1998.

Table 4 Mooring deployments during M39/4

MOORING	DATE		UTC	LATITUDE	LONGITUDE	COMMENT
K7	14. July 1997	22:31	52ƒ51.1'N	51ƒ35.8'W	DLC-array
K8	15. July 1997	13:30	52ƒ57.5'N	51ƒ18.0'W	DLC-array
K9	14. July 1997	14:20	53ƒ08.5'N	50ƒ52.0'W	DLC-array
K10	13. July 1997	23:30	53ƒ22.8'N	50ƒ15.6'W	DLC-array
K16	13. July 1997	13:04	53ƒ41.5'N	49ƒ26.2'W	DLC-array
K11	22. July 1997	23:39	56ƒ33.6'N	52ƒ39.5'W	Tomography/Convection
K12	21. July 1997	19:48	55ƒ19.5'N	53ƒ53.6'W	Tomography/Convection
K14	23. July 1997	22:35	58ƒ30.0'N	50ƒ34.2'W	Tomography
K17	20. July 1997	19:09	57ƒ24.8'N	55ƒ40.0'W	Tomography
K15	20. July 1997	09:44	57ƒ06.1'N	54ƒ40.0'W	moored CTD

Convection Moorings 1997/1998

As in the previous deployment (1996/97) two moorings, K12 and K11, are equipped 
with ADCPs to measure vertical currents associated with convection, and with 
temperature and conductivity sensors to measure the development of the 
stratification. Two new instruments are deployed for the first time, a new 
generation of Seabird sondes ("Micro-Cat") and small temperature/depth sondes 
(developed and assembled by C. Meinke). The latter are thought to replace 
thermistor strings in order to reduce the drag in the mooring (leading to large 
vertical excursions), and to increase the flexibility of the vertical distribution 
of temperature measurements in convection moorings. Both moorings had tomography 
sources.

The moored CTD The moored CTD was repaired and prepared for its second deployment 
period at Woods Hole Oceanographic Institution, and it arrived in St. Johns just 
prior to the cruise. The position of this mooring was planned to be near the center 
of the deep winter mixing regime west of the WOCE-AR7 line, and it should be 
located on the acoustic ray path between the tomography sources in K1 and K17. The 
deployment on July 20 went very smooth, and we were able to avoid any slippage of 
the CTD along the mooring wire; this was thought to be the reason for the 
instrument failure in the previous deployment. In addition to the CTD a down-
looking ADCP for three-dimensional current measurements was incorporated near 70 m.

c) Acoustic Tomography (U. Send, D. Kindler)

During the winter 1996/97 four moorings with tomography instruments had been 
deployed in the Labrador Sea (K1, K3, K4, L). Two of these were recovered already 
in May/June during a cruise of the Canadian research vessel íHudson', while the 
remaining two, K3 and K4, were retrieved on this METEOR cruise. The mooring 
operation proceeded without obvious problems; however, a small quantity of water 
was found inside instrument K4, below the electronics and the battery pack. At 
present, it is unclear how and when this leakage occurred.

The recovery of the acoustic transponders turned out to be problematic in some 
cases. These transponders are important for the mooring-motion navigation of the 
tomography instruments, and three transponders are located around each mooring. 
This time, we were using recoverable transponders, which can be released through an 
acoustic command. In total, 9 of these were to be recovered on the METEOR cruise, 
however one was not responding anymore, while the other was so weak (battery 
problem ?) that it could not be released. Thus a total of 7 transponders was 
retrieved.

During the cruise, 5 tomography instruments were originally planned to be deployed 
again. This number had to be reduced to 4 due to the leakage in the instrument from 
K4. The fifth unit was the larger HLF-5 sound source, which had been prepared in 
Kiel complete with two powerful lithium battery packs. The two instruments 
recovered on the 'Hudson' had in the meantime been at the manufacturer for service 
and repair, whereas the remaining instrument retrieved on the first leg of M39/4 
had to be serviced and prepared for re-deployment on board. These activities went 
according to plan, until a short-circuit occurred in both lithium battery packs 
during/after deployment of the HLF-5 source. This was due to a leaking underwater 
electrical connector. Fortunately, multiple fuses prevented a fire of these 
potentially dangerous batteries, but the packs were unusable afterwards. With help 
from the ship's electronics department an improvised battery pack with reduced 
capacity was then built from the alkaline batteries originally meant for the 
instrument from K4. This new pack would allow transmissions with the HLF-5 sound 
source once a day, starting November 1. Two short test transmissions shortly after 
deployment could not be verified, possibly due to high ship noise.

In total then four moorings with tomography instruments were deployed, which were 
K11, K12, K14, K17. Again three transponders were placed around each of these 
moorings, whose exact position was determined with a special acoustic survey.

d) Navigation requirements , shipboard ADCP and LADCP 
(J. Fischer, C. Mertens, F. Schott)
Lowered ADCP

On all of the CTD profiles an ADCP was attached to the rosette to obtain profile-
deep currents. The profiles were all referenced by GPS/GLONASS positioning, and the 
much improved positioning accuracy will reduce errors in the barotropic current 
component (see also "shipboard ADCP"). During the first leg of cruise M39/4 the 
Broad-Band ADCP S/N 1002 was used until a failure appeared and some profiles were 
considerably distorted. These profiles need individual processing and adjustment to 
shipboard ADCP currents.

From profile 17 onwards the Narrow-Band ADCP S/N 301 was used. This instrument was 
in already in use during the previous cruises M39/2 and M39/3. It worked fine with 
the usual unavoidable data loss by bottom interference; this needs careful 
postprocessing and checking with bottom tracking.

Shipboard ADCP

In St. Johns a new 75kHz shipboard ADCP was mounted in the ships well. This was the 
first use of a low frequency ADCP, as the standard METEOR ADCP was a 150 kHz 
system. Other components of the system were a 3D-ASHTECH GPS receiver for 
positioning and attitude (mainly heading) parameters, and the above mentioned 
GPS/GLONASS receiver as a standalone system for parallel storage of more precise 
positioning data.

During calm conditions the profiling range of the ADCP was near 700 m, but when the 
ship was heading into the swell the range was significantly reduced; there were 
even periods of total data loss during the more windy days.

At the end of the cruise all shipboard ADCP data were edited and calibrated. The 
calibration improved due to external navigation from the GPS/GLONASS system, and by 
using the Ashtech heading for gyro correction. During the cruise the ADCP had to be 
lifted up, as there was a seawater pump attached to the same mounting platform 
which had to be replaced. We suspected that this would reset the ADCP calibration, 
but fortunately the transducer orientation did not change. The accuracy of the 
transducer misalignement angle determination was estimated to 0.1ƒdegs on the basis 
of 160 reliable calibration points.

In general the vertical shear of the currents was rather weak, and the reference 
layer velocity (depth range 60 - 140 m ) is representative for the currents over 
the total depth range of the ADCP. An overview over the existing data base along 
the three major sections of the cruise is shown in figure 18.

As another example for the final shipboard ADCP data the section along the moored 
boundary current array is shown in figure 19.

GPS/GLONASS precision of navigation

This system was received in St. Johns, and it was planned to be used for improving 
the accuracy of lowered and shipboard ADCP data as well as for better transponder 
navigation.

During most of the time the number of satellites locked exceeded 10 with an 
equivalent number of GPS and GLONASS satellites; sometimes even 15 satellites were 
locked, resulting in a very smooth ship track. Only in rare occasions at a number 
of satellites less than 8, some noise could be detected on the plotted cruise 
track.

As the ship was underway wenn the GPS/GLONASS system was started we were not able 
to perform a statistical test with the ship at rest. Instead we compared the 
influence of pure GPS data stored with the shipboard ADCP data string (5 minute 
data) with that of GPS/GLONASS in terms of statistical noise in the absolute 
reference layer velocity. This is the vertically averaged ADCP current (bins 5 to 
10) minus the ships drift (the latter determined by either positioning system). 
While referenced with GPS only the scatter of the absolute reference layer velocity 
was large (12cm/s) it was significantly reduced (to 5cm/s) by using GPS/ GLONASS 
(Figure 20). As an additional benefit the higher accuracy of the reference layer 
velocity helped to improve the determination of the transducer misalignment angle.

Summarizing, the GPS/GLONASS receiver led to significantly higher accuracy of 
positioning data, thereby improving both shipboard and lowered ADCP data. In cases 
where the GPS P- code or differential GPS quality is not available this system 
should be routinely used. GPS/ GLONASS positioning for example should be linked 
directly to the shipboard ADCP as the primary navigation source.

Fig. 18:Shipboard ADCP currents during the second part of leg M394/4; St. Anthony to 
	Greenland.

Fig. 19:Shipboard ADCP currents (east and north component) along the boundary 
	current array and across the Newfoundland shelf to St. Anthony. The 
	topography is from the METEOR depth sounding system (Parasound).

Fig. 20:Navigation data comparison: top graph shows ADCP currents minus ships speed 
	over ground (SOG) determined from GPS positions, second graph shows the same 
	but SOG determined by GPS/GLONASS positions. The third timeseries shows the 
	difference between Ashtech 3D- GPS heading and gyro heading; note some gaps 
	between the dots. The lowest graph shows the coverage of reliable Ashtech 
	headings in %/day.

Ashtec 3DF attitude parameters

Gyro errors are one of the major error sources in shipboard ADCP data. High 
frequency (Schuler) oscillations show heading fluctuations of more than a degree 
during acceleration phases. Since these periods are important for calibration of 
the misalignment angle between ADCP-transducers and gyro heading, any improvement 
of heading accuracy should be considered. With METEOR's Ashtec 3DF-GPS receiver it 
is possible to obtain an independent estimate for ship's heading, which is not 
contaminated by these oscillations. However, due to data gaps this correction could 
not be done on a ping to ping basis, but for ensembles (5 min) with good data 
coverage. During the first part of the cruise the data coverage was in the 50% 
range, but with the new firmware (obtained underway) the data covered improved to 
near 80%.

A heading correction file was prepared by using the GPS-Gyro heading difference 
whenever the GPS data quality was sufficient. Short gaps were filled by 
interpolation, for longer gaps the difference was set to zero. Then all ensembles 
were rotated accordingly.

e) PALACE launches (J. Fischer)

Seven Palace floats were deployed during the cruise, two with CTD-sensors and 5 
with temperature and pressure. All floats were ballasted to drift at 1500 dbar, and 
they were programmed for surfacing every 5-days until April 1998 and for 14-day 
cycles afterwards. All floats were deployed in the boundary current regime; for 
dates and positions see table 5.

Tab. 5 Palace floats deployed during M39/4

FLOAT	CODE	SENSORS	DATE		UTC	LATITUDE	LONGITUDE
9L	8632	TD	09. July 1997	09:49	55ƒ15.55'N	53ƒ57.12'N
14L	8637	CTD	09. July 1997	10:58	55ƒ24.83'N	53ƒ48.45'W
8L	8631	TD	09. July 1997	12:04	55ƒ33.64'N	53ƒ39.96'W
15L	8638	CTD	14. July 1997	14:39	53ƒ08.84'N	50ƒ52.53'W
7L	8630	TD	15. July 1997	15:04	52ƒ56.99'N	51ƒ18.130'W
46	9211	TD	20. July 1997	22:14	57ƒ25.00'N	55ƒ40.94'W
23	9210	TD	21. July 1997	03:10	56ƒ48.11'N	55ƒ00.06'W

f) CFC analysis (M. Rhein)

During the cruise, the CFC system worked continuously and about 1850 water samples 
have been analysed. The survey was dedicated to the circulation of the deep water 
masses. During periods of dense station spacing, sampling was focused on the water 
column below 800 m depth. Calibration was done with a gas standard kindly provided 
by D. Wallace, PMEL, USA. The CFC concentrations are reported on the SIO93 scale. 
CFC-11 analysis was successfully carried out during the cruise, the analysis of the 
CFC-12 concentrations however was partly interrupted by an unknown substance with a 
similar retention time as CFC-12. The blanks for CFC-11 and CFC-12 were negligible. 
Accuracy was checked by analyzing 10 percent of the water samples twice, and was 
for both substances ±0.8%.

5.1.2.2 Analyses and Evaluations
a) Water mass distribution, Labrador Sea Water properties (M. Rhein, L. Stramma)
Labrador Sea Water (LSW)

Along the WOCE section AR7-W (Fig.21), the CTD stations were mainly centered in the 
boundary current regions leaving 5 stations for the central Labrador Sea. Two of 
these stations show peculiar features. Profile 7 (57ƒ23'N, 51ƒ47'W) exhibits the 
lowest salinities in the range of the LSW, which are associated with a temperature 
minimum (Figure 21) and with elevated CFC-11 concentrations at 1000-1600 m depth, 
higher by 0.6 pmol/kg than anywhere else in this water mass. All three parameters 
point to formation by deep convective renewal in late spring 1997, reaching to 
depth around 1500 m. The core density was s q = 27.76 (s 1.5 =34.67), lower than 
the density of the convective product in spring 1994, which still lingers in the 
Labrador Sea with core densities of s q = 27.78 (s 1.5 =34.69). The CTD profile at 
the nearby profile 28 (57ƒ56'N, 51ƒ10'W) was characterized by a low vertical 
temperature gradient at 500 - 900 m, lifting the isopycnal s q = 27.76 from 1000 m 
to 700 m depth. The lower bound of the LSW (s q = 27.8) was 2200 m (Prof. 7), and 
1800-2000 m for the other central stations. CFC-11 concentrations in the LSW along 
the AR7 section varied between 4.0-4.6 pmol/kg, except at the before mentioned 
profile 7 where values as high as 5.03 pmol/kg were observed.

South of the Gibbs Fracture Zone (52ƒ30' - 53ƒN) along the 35ƒW section (Figure 
22), the LSW layer is about 1300 m thick. Due to the rising of the lower bound of 
the LSW (s q = 27.8) over the Reykjanes Ridge from about 2100 m to 1500 m LSW grows 
thinner above the ridge. Salinities of the LSW were higher than 34.87 and CFC-11 
concentrations did not exceed 3.5 pmol/kg (profile 68, south of Gibbs Fracture 
Zone), the lowest values were measured on the northernmost station on the Reykjanes 
Ridge. The salinity minimum at sig 27.78, the product of deep convection in 1994, 
was only found on the stations south of profile 71 (52ƒ39'N, 35ƒ01'W), the salinity 
minimum further north was broader, less distinct and centered at higher densities 
(around 27.785).

Gibbs Fracture Zone Water (GFZW)

The Salinity-F11 relation of GFZW in the Eastern Atlantic differs from the one in 
the Western Atlantic: in the east, CFC-11 is elevated with increasing salinity, 
because the water surrounding the GFZW are less saline and CFC-11 poor. In the 
west, however, the GFZW encounters the low saline but CFC rich LSW and DSOW, 
leading to increasing CFC-11 values in the GFZW with decreasing salinity. When 
entering the western part, the CFC-11 concentrations in the high saline core of the 
GFZW can only decrease further when mixing with older deep water flowing into the 
subpolar North Atlantic from the south.

The 35ƒW section includes the detailed survey of the Gibbs Fracture Zone (Figure 
22), and of channels which might allow the GFZW to spill over the Reykjanes Ridge 
into the western Atlantic. In the Western Atlantic, the isopycnals s q = 27.8 -
27.88 enclose the GFZW. In the GFZ itself, the salinity maximum (S > 34.96) located 
on the northern flank reaches down to about 3200 m (s q = 27.882). Below, the 
salinity AND the CFCs decrease, indicating that this deeper part is also water from 
the Eastern Atlantic. The lowest GFZW concentration in the GFZ was 1.8 pmol/ kg. 
The concentrations in the GFZW increased towards the north up to 2.5 pmol/kg, north 
of 53ƒN, CFC-11 values were everywhere greater than 2.2 pmol/kg. The highest 
density found on the Reykjanes Ridge was 27.876 (s 2 =37.03, S=34.968, CFC-11=2.4 
pmol/kg, profile 85).

The salinity maximum, denoting the core of the GFZW is located in the Irminger Sea 
at densities s 2 =36.99 - 37.01 with increasing densities towards the west and more 
saline at the Reykjanes Ridge (34.93) than at 41ƒW (34.92). The salinity maximum 
could not be identified west of 41ƒW. The most saline and thus purest GFZW in the 
Irminger Sea has CFC-11 concentrations smaller than 1.9 pmol/kg, much lower than 
the concentrations above the Reykjanes Ridge, but close to the lowest values below 
the salinity maximum flowing through the GFZ.

A close investigation of the CFC-distribution showed that spilling of GFZW across 
the Reykjanes Ridge through gaps other than the GFZ can only influence the GFZW in 
the Irminger Sea at densities s 2 < 37.03, the CFC-11 - density relation seems to 
limit the density range < s 2 =37.0.

Along the 43ƒ30'W section and in the Labrador Sea, the most saline and CFC-11 
poorest GFZW was found away from the boundary regions. CFC-11 concentrations below 
2 pmol/kg are found along 43ƒ30'W between 51ƒ30'N and 57ƒ0'N and in the Labrador 
Sea on the easternmost profiles 11-15.

Denmark Strait Overflow Water (DSOW)

In 1996, the temperature minimum of the DSOW was found not in the Irminger Sea but 
in the Labrador Sea (1.12ƒC coldest temperature in the Labrador Sea in August 1996, 
found in the center (profile 61). Compared to 1996, the temperature in the Labrador 
Sea increased to 1.4- 1.6ƒC, with the coldest temperatures at profiles 14 and 15 in 
the southern section. Only two locations on our survey were colder: at the northern 
boundary at the 43ƒ30'W section (profiles 35, 36, 37) and in the western part of 
the Irminger Sea section west of 40ƒW with a minimum temperature of 1.19ƒC. The 
warmest temperatures (higher than 1.8ƒC) were found at the 43ƒ30'W section 
(profiles 40-46) and east of 37ƒW.

The CFC-11 concentration of the DSOW in the Labrador Sea has decreased, caused by 
the change in temperature. The CFC-11 values at the same temperature level showed 
no difference between the 1996 and 1997 data. The characteristic of the DSOW, i.e. 
decreasing salinities and increasing CFCs towards the bottom were found on all deep 
profiles except the region east of 37ƒW.

Fig. 21:Distribution of salinity (top), potential temperature (center) and CFC-11 in 
	pmol/kg (bottom) along section AR7-W. The isopycnals s q = 27.74, 27.8 and 
	27.88 as boundaries for the LSW (27.74 - 27.8) and Gibbs Fracture Zone Water 
	(27.8 - 27.88) are included as solid lines.

Fig. 22:Distribution of salinity (top), potential temperature (center) and CFC-11 in 
	pmol/kg (bottom) along 35ƒW. The isopycnals s q = 27.74, 27.8 and 27.88 as 
	boundaries for the LSW (27.74 - 27.8) and Gibbs Fracture Zone Water (27.8 - 
	27.88) are included as solid lines.

b) Boundary circulation and transports (F. Schott, J. Fischer)

The cruise track of M 39/4 was especially designed to investigate the deep boundary 
currents of the Labrador- and Irminger seas. Deep boundary current velocities are 
determined by geostrophy and by LADCP current profiling. The evaluation of both 
kinds of observations showed that on most boundary sections a satisfactory level of 
no motion cannot be determined. A significant barotropic component is mostly 
present.

The western Labrador Sea boundary currents were sampled by two sections, north of 
Hamilton Bank and near 53ƒN, where the array K7-K16 was then deployed (Fig.8), the 
northern Labrador Sea by the AR-7 line. The directly-measured (by LADCP) top to 
bottom currents across the western end of the AR-7 section yield quite substantial 
transports, of 33 Sv total between the shelf edge and 56ƒN. This number is in close 
agreement with the value of 31 Sv that was determined along the same section 
segment in August 1996 from LADCP profiling during "Valdivia" cruise VA161. A bit 
more will have to be added when the shipboard ADCP observations on the shelf are 
brought into the analysis. The total boundary current transport is made up by the 
addition of the near-barotropic flow due to Sverdrup forcing, superimposed by the 
deep boundary current. The Sverdrup flow and the thermohaline DWBC are both 
cyclonic, hence a zero-reference level cannot be expected.

The absolute current field along the boundary sections is determined by geostrophy 
referenced by vertically integrated LADCP currents. This procedure is recommended 
as the vertically integrated LADCP currents are accurate estimates of the 
barotropic flow component, while the baroclinic flow estimated from geostrophy is 
preferable to that obtained by the direct measurements. The resulting transports 
for the deep water masses (DSOW, GFZW and LSW) at the boundary sections are 
summarized in Table 6. However, the result is to be considered preliminary, since 
it is somewhat dependent on the treatment of bottom triangles and might also be 
subject to larger changes, when the direct measurements are corrected for tidal 
currents.

Tab. 6: Total transport at Boundary Current sections (Sv)

Section		DSOW	GFZW	LSW	DWBC
AR7-S		5.0	4.4	11.8	21.6
53ƒN		4.0	4.6	11.0	19.6
Cape Farw.	6.0	6.5	13.0	25.5
Flem. Cap	1.5	3.0	8.0	12.5

c) Convection moorings 1996-97 (C. Mertens, J. Fischer, F. Schott)

Four of the moorings, deployed over the winter of 1996/97, were designed for the 
purpose of observing deep convection activity using acoustic current meters and 
temperature/salinity recorders. Two of the moorings (K1 and K5) were located in the 
central Labrador Sea and the other two (K2 and K6) in the boundary current region.

The meteorological conditions during the winter of 1996/97 showed a dramatic 
transition of the flow regime over the North Atlantic which resulted in a 
significant change in the magnitude of surface cooling in the Labrador Sea region. 
Until mid January the presence of a blocking high over Europe and anomalously high 
pressure over Greenland caused a significant westward shift of cyclonic activity 
with the effect of rather low heat loss over the Labrador Sea. In contrast, 
February 1997 was a month in which the circulation pattern over the North Atlantic 
was significantly stronger than average, resulting in strong heat loss over the 
Labrador Sea. NCEP/ NCAR reanalysis data show peak values greater than 1000 W/m 2 
(Fig. 23a).

The temperature development at mooring K1 during the winter of 1996/97 is shown in 
Fig. 23b. In late autumn a warming is found in the near-surface sensors, resulting 
from the deepening of the summer mixed-layer. Owing to the first rather mild 
winter, only a slow cooling of the surface layer set in by mid December. After the 
transition of the meteorological conditions in mid January, strong cooling took 
place and a rapid deepening of the mixed-layer to about 1000 m. Temporary 
fluctuations in the records of deeper temperature sensors indicate convection 
activity to about 1300 m. Acoustic Doppler current profiler (ADCP) measurements 
show strong downward vertical currents for several hours duration during this 
period. The maximum vertical velocity of about 10 cm/s was found at the beginning 
of March.

The time series of horizontal currents obtained at K1 show, except for a number of 
eddy events, a rather small amplitude (Fig. 23c). Prior to the convection two of 
those barotropic eddies advected past the mooring, one at the beginning of December 
and one in January. Their low core temperature suggest, that their water-mass 
properties have been formed by convection during the previous winter. After 
convection a number of strong eddy events have been observed.

Mooring K2 was also equipped with a large number of temperature sensors in order to 
observe possible convection activity. In contrast to the central Labrador Sea, an 
instantaneous cooling of the upper 800 m has been observed here in mid February, 
which could not result from local convection activity and hence must have been 
advected by the Labrador Current. Further, no pronounced events of downward 
vertical velocity could be found in the ADCP records, most likely due to the 
reduced density of the lower-salinity Labrador Current on top.

d) Gibbs Fracture Zone study (F. Schott, J. Fischer, L. Stramma).

The Charly Gibbs Fracture Zone near 52ƒN is the key location for the exchange of 
deep water masses between the eastern and western basin of the subpolar North 
Atlantic. As detailed bathymetric surveys showed a bottom depth exceeding 3500 m 
this allows North East Atlantic Deep Water (NEADW) to pass the Mid-Atlantic Ridge 
(MAR) through the GFZ. Owing to its density this water mass, also called Gibbs 
Fracture Zone Water (GFZW), is located beneath the Labrador Sea Water (LSW). Framed 
by potential densities 27.8 and 27.88 the GFZW is clearly detectable by its high 
salinity.

Earlier moored observations of the throughflow by SAUNDERS (1994) had shown a mean 
westward flow organized in inter-mittent events with the currents even reversed to 
eastward during some periods. Such a situation was met during M39/4 when we 
conducted a detailed study of the water masses (CTDO 2 and CFC's) and flow (LADCP) 
in the passage (Figure 24), farther up north along the MAR, and across the Irminger 
Sea. Geostrophic shears revealed the expected structure with deep westward shears 
between the LSW and the GFZW, and currents relative to 1000 m showed deep westward 
flow in the range of the GFZW yielding a westward transport of approximately 7 Sv 
for the layers below 1500 m. However, the directly measured currents gave a 
different result. Although showing approximately the same baroclinic structure, 
even with the relative transports being in good agreement with the geostrophic 
estimates, the barotropic current component was directed towards the east leading 
to net eastward transport. Regarding the deep flow alone, i.e. below 1500 m, this 
led to net eastward transports of about 6.5 Sv. The surface flow at this time 
showed a well defined eastward jet accompanied by salinities above 35 and was 
presumably associated with the North Atlantic Current (NAC), which was located 
right on top of the GFZ at this time.

A study of historical hydrography and XBT data from the region showed that at some 
times in the past the NAC took a more northerly route than usual. The consequence 
seems to be a deep- reaching effect on the GFZ and deep-water through flow into the 
western basin. A paper on this subject was prepared for publications. 

e) Acoustic tomography (U. Send)

In some of the tomography moorings, isolated components had failed, which reduces 
the information available quantitatively or qualitatively. Among these is a gap in 
the data disk in instrument K1, mis-formatted information from the mooring 
navigator in instrument L, and two essentially non-functioning transponders in 
mooring K3. All these units had passed pre- deployment tests, and the source of the 
problem must be intermittent in nature.

The quality of the acoustic receptions was found to be highly variable. There are 
periods with good, clearly resolved receptions, while at times no signal is visible 
at all. Detailed analyses revealed increased noise levels (and sometimes also 
reduced signal levels) during the periods with worse signal-to-noise (S/N) ratio. 
These intervals are highly correlated with times at which the moorings are 
displaced horizontally and vertically due to currents, which might indicate a 
problem with mooring strumming, flow noise, or related effects. However, we cannot 
exclude the possibility of an instrumental problem in the receiver part of the 
electronics. There seems to be enough information still in the data to analyze the 
large-scale temperature stratification at various times from the tomography array, 
but these results depend on more careful evaluation of error sources and sizes, and 
choice of a suitable set of basis functions (vertical modes) for inversions.

For the redeployment of the instruments, every effort was taken to verify the 
functioning of the modules in each unit, and to reduce noise in the moorings (e.g. 
by covering shackles and rings). Also, the distances between the moorings were 
somewhat reduced in this deployment period, and the more powerful HLF-5 sound 
source should further improve the S/N ratio.

Fig. 23:a) Net heat flux from NCEP/NCAR reanalysis at a grid point near mooring K1; 
	b) potential temperature from all K1 instruments, instrument depths are 
	marked as squares; c) horizontal current vectors for selected depths.

Fig. 24:Zonal flow through the Charly Gibbs Fracture Zone obtained by LADCP (top) 
	currents relative to the flow in 1000 m depth (middle) and by geostrophy 
	relative to 1000 m depth (lower graph). Transports below 1500 m and between 
	stations 65 and 75 are included; units are in Sv.

5.1.2.3 Air-sea fluxes (U .Karger, H. G”ng)

Measurements of the turbulent structure of the wind were gathered using a 3-
dimensional sonic anemometer with a sampling rate of 30Hz. The spectra of turbulent 
wind speed fluctuations will give an estimate of the momentum exchange. Coincident 
temperature and humidity samples, measured with a fast-response psychrometer lead, 
together with the vertical fluctuations of wind speed, to the fluxes of sensible 
and latent heat. Since ship movements will have an impact on the measurement of the 
wind components, the pitch and roll angle of vessel was taken with a frequency of 
5Hz. Both instruments were located port beside the foremast at a height of 20 m. 
Most of the time these measurements were under good conditions, because the 
relative wind direction was often North to Northwest, so that the data should not 
be disturbed directly by the ship's superstructure and the foremast.

Different kinds of data of the vertical atmospheric structure for the evaluation of 
remote- sensing based air-sea flux algorithms were sampled. More than 160 
radiosonde launches were made, together with the German Weather service, during 
overpasses of DMSP-satellites with the SSM/ I (Special Sensor Microwave/Imager) 
radiometer on board. The soundings provide the real state of the atmosphere, 
measuring temperature and humidity profiles, which will influence the atmospheric 
microwave emission. With a ship borne 20-30 Ghz passive microwave radiometer down-
welling radiances of the atmosphere were obtained, from which also water vapour and 
especially cloud liquid water will be deduced. Additional information about the 
ocean surface skin temperature and the cloud-base temperature were detected by two 
infrared thermometers. Meteorological standard synoptical observations were 
performed hourly to give further information about the atmospheric conditions, e.g. 
distribution, height, and kind of clouds.

5.1.2.4 Carbon Dioxide System, Nutrients and Oxygen (L. Mintrop)
Technical aspects

On this leg the same methodology and sampling strategy for CO2, oxygen and 
nutrients was followed as on the second leg of the cruise (see 5.1.1.3.). This 
involved discrete water sampling from 46 hydrocasts on this leg. A total of 862 
samples were drawn and immediately analyzed for total dissolved inorganic carbon 
(CT) and total alkalinity (AT). The analytical methods involved have been described 
previously (5.1.1.3.). Due to some improvements of the alkalinity method, precision 
for AT could be raised further to 0.5 µmol…kg-1 (between-bottle reproducibility) as 
judged from regular measurements of duplicate samples. Accuracy of the data has 
been estimated to be about 2.0 µmol…kg-1 for AT.

The continuous determination of the partial pressure of CO2 (pCO2, closely 
equivalent to fugacity of CO2 which more correctly takes into account the non-ideal 
nature of this gas) in surface seawater and overlying air was carried out during 
the entire cruise using the automated underway pCO2 system described previously 
(see 5.1.1.3.). During the cruise a data set of more than 2600 one-minute-averages 
for atmospheric pCO2 and approx. 45000 averages for surface seawater pCO2 was 
generated.

In contrast to the situation in the Pacific, data on isotope ratios for 13C and 14C 
are scarce for the North Atlantic; one objective during legs 2 through 5 therefore 
was taking samples to improve this situation. Carbon isotope ratios will give 
additional information on anthropogenic CO2 invasion and assist in distinguishing 
the physical and biological carbon pumps. A total of 239 samples were taken on 12 
hydrographic stations on leg 4. A subset of samples will be selected for 14C AMS-
measurement.

The calculation of anthropogenic CO2 from measured concentrations of total 
dissolved inorganic carbon involves the reconstruction of the "history" of the 
water sample under consideration. So the measured value is to be corrected for the 
changes incurred due to remineralization of organic matter and the dissolution of 
carbonates since the water lost contact with the surface and the preformed pre-
industrial value. Difficulties associated with this approach is the role of mixing 
of different water types with poorly known initial concentrations, possibly leading 
to non linear effects, the difficulty of choosing appropriate pre-industrial end-
member water types and some uncertainties in the assumptions relating to the 
constant stoichiometric ratios and the resulting from the use of the apparent 
oxygen utilization (AOU) for determining the contribution of the remineralization 
of organic matter.

AOU was calculated from the measured dissolved oxygen concentrations; 1907 samples 
were drawn from a total of 99 hydrographic stations. The samples were measured 
using standard WINKLER titration, the method was refined to meet WOCE quality 
criteria (see 5.1.1.3.). Standard deviation as determined from sets of 10 
replicates were 0.12%.

The nutrient data, necessary to evaluate atom ratios in the remineralization of 
organic matter and therefore provide the stoichiometric factors necessary for 
anthropogenic CO2 calculation, were obtained from 1905 samples from 97 hydrocasts. 
Standard photometric procedures (see 5.1.1.3.) were applied using an autoanalyzer 
system. Standard deviation from measurements of 10 replicates were 0.09%, 1.1%, 
1.1% for nitrate, phosphate, and silicate, respectively.

First results

As mentioned earlier, the calculation of anthropogenic CO2 requires a number of 
assumptions, which have to be verified for the area under consideration. The data 
obtained on the various legs of the METEOR 39 cruise therefore should serve as a 
data baseline to elaborate from property- property plots relations of nutrients and 
oxygen with the carbon system parameters for different water masses. Also, 
preformed values from several water types found in the area were also taken from 
data collected on previous cruises covering their source regions. These relations 
are currently used to refine the method of back-calculation for the North Atlantic 
published recently (K÷RTZINGER et al. 1998).

Some more general features of the measured parameters shall be mentioned in the 
following:

CT: In contrast to profiles measured in the Eastern Basin of the North Atlantic 
earlier, those of the Labrador and Irminger Seas are characterized by very little 
variation below the top 500 meters approximately. Concentrations are about 2152-
2156 µmol/kg, only in the deeper waters at the Gibbs-Fracture Zone (St. 415-430) 
elevated values up to 2162 µmol/kg were found. However, despite the low 
variability, a close positive correlation with AOU and also with nutrient maxima is 
obvious, as should be expected due to remineralization processes. The little 
variation found is favorable to detect any alteration of the CT level in future 
cruises, as are planned in the SFB 460.

AT: Alkalinity as well shows remarkable little variation in the Labrador and 
Irminger Seas, ranging from 2302 to 2312 µmol/kg below 500 meters. The range is 
even reduced, when the specific alkalinity, normalized to S=35, is considered. This 
shows the partly conservative behavior of alkalinity. However, positive correlation 
with silicate is also observed. This is a feature of Southern Component Water, 
characterized by higher silicate and specific alkalinity. This water is found below 
3000 m, most pronounced between St. 393 and 399. Alkalinity rises to 2320 µmol/kg 
there.

Nutrients: The silicate profiles mainly reflect waters with southern origin, as has 
been mentioned above. Peak levels reach 16 µmol/L at depth below 3000 m. However, 
this is only a weak signal, considering a silicate concentration around 120-130 
µmol/L for the AABW endmenber. Nitrate and phosphate are correlated, but a more 
detailed investigation will be required to deduce Redfield ratios from the data. 
Nitrite is close to the detection limit throughout, with occasional peak values up 
to 0.5 µmol/kg in the 50 m samples. Nutrient maxima in the 1000 m level accompanied 
with low oxygen indicate the zone of mayor remineralization in the water column.

Oxygen: AOU calculated from oxygen concentrations reach fairly low maxima around 50 
to 70 µmol/L, both associated with silicate maxima in deep waters and 
nitrate/phosphate maxima at intermediate levels.

To give an example, Fig. 25 shows isoplots of several parameters along the transect 
between stations 381 and 404 (roughly a meridional transect along 43ƒ30'W). From 
the nitrate values the mayor remineralization zone between 500 and 1500 m is 
clearly visible. High silicate values centered at about 3500 m indicate the 
prevalence of Southern Component waters. High AOU accompanies both features. Maxima 
in CT parallel those in AOU, while the deep silicate maxima between 51 and 53ƒN is 
associated with a pronounced AT maximum. Low values of all parameters around the 
northern slope indicate the NADW boundary current.

Surface water pCO2: A first look at the pCO2 of surface water showed a constant 
undersaturation of 30-40 µatm throughout the cruise. It was closely related to 
surface temperature, but also correlated with salinity. The data will have to be 
compiled after the cruise.

The profiles of pCO2 co-vary with temperature, indicating that water mass 
characteristics and their short time variability and local patchiness govern the 
pCO2. Positive correlation between pCO2 and temperature would indicate rising pCO2 
when a water mass gets warmer (theoretically about 4% per ƒC). Since co-variation 
is observed also without positive correlation, it is more likely that temperature 
indicates different water parcels and their patchy distribution in this cases, 
which due to their inherent preformed pCO2 cause the observed pCO2 variability. 
Negative correlation would also be the result of CO2 uptake after a water parcel 
had been cooled due to higher solubility of CO2 in cold water. However, in most 
cases CO2 exchange is slow compared to temperature change of surface waters.

During the first part of the cruise, very low pCO2 values of as low as 180 µatm 
were measured. These are not accompanied by a temperature decrease and strongly 
indicate massive fixation of CO2 by a plankton bloom.

Fig. 26 gives an example of a pCO2 registration over 24 hours; given is the X CO2 
(molar fraction of CO2), the temperature and the salinity. The different water 
masses, characterized by salinity and temperature, are also reflected in their X 
CO2 values; the general trend of higher values with lower temperatures, as expected 
from increased solubility, is obvious. However, the strong minima found in X CO2 
are more likely resulting from biological uptake.

The data collected so far represent the molar fraction of CO2 in moist air. Taking 
into account the atmospheric pressure from the DVS data file and by calculating the 
water vapor pressure, the fugacity of CO2 in dry air was calculated. The data are 
about to be sent to the CO2 data center in Oak Ridge, Tennessee to serve in the 
development of a seasonal pCO2 model of the North Atlantic Ocean.

Fig. 25:isoplots of nitrate (a), silicate (b), apparent oxygen utilization (AOU, c), 
	total dissolved inorganic carbon (CT, d) and total alkalinity (AT, e) between 
	stations 381-404. Units are in Ïmol/l (a-c) and Ïmol/kg (d, e), 
	respectively.

Fig: 26:Continuous registration of molar fraction of CO2 in surface seawater 
	on July 8, 1997 (bold line). Also included are water temperature (dotted 
	line) and salinity (thin line). Positions at 0:00 and 24.00 hrs are ca. 
	53ƒN 51.4ƒW and 55.3ƒN 53.9ƒW, respectively.

5.2	WOCE and VEINS
5.2.1	Leg M39/3
5.2.1.1 Hydrographic Measurements

Hydrographic work on this cruise consisted of a routine 24 hour watch system to 
operate CTD/ rosette casts with a L-ADCP system on station, underway, besides 
regular XBT drops we maintained two thermosalinograph systems TSG for T and S 
measurements of the surface layer, the shipboard ADCP and a rain-gauge. Routine 
meteorological observations were made and recorded.

Hydrographic data collection was done in a 24 hour watch system with the watch 
running the CTD/rosette casts on station and the underway measurements. For the 
CTD/rosette casts we used again the BIO label system to uniquely identify water 
samples and subsequent sub-sampling right to their analysis. For further details 
see M39/5.

All TSG, XBT and CTD data were transmitted to BSH in the framework of IGOSS in the 
relevant formats. All data will be submitted to the relevant WOCE Data Centre after 
final processing, quality control and annotation.

The 48ƒN section in the Atlantic has been sampled first during the IGY in 1957, and 
intensively during the 1990s. This now is the sixth survey since 1957 and the 
fourth during WOCE  (KOLTERMANN u. LORBACHER, 1998). The hydrographic structure is 
dominated by the warm, salty waters from the South that cover the top 1400 m, with 
maximum salinities on the European side of the section. The intermediate waters 
between 1400 m and 2400 m are fresh and particularly well oxygenated. Properties 
are set in their area of origin in the West, the subpolar gyre to the north of the 
section and especially in the Labrador Sea. Below 2400 m and almost down to the 
bottom are waters with temperatures between 2.9 ƒC and < 2.0 ƒC, with an 
intermediate salinity maximum in both basins at ca. 2900 m. In both basins we find 
remnants of Antarctic Bottom Waters AABW, best identified by the high silicate 
signal. The largest contribution is found in the North European Basin. On both 
sides of the Mid-Atlantic Ridge boundary currents are marked well in the salinity 
fields by distinct cores.

The largest changes below the thermocline are found in the intermediate waters 
dominated by the Labrador Sea Water LSW. The strong cooling and freshening observed 
in the 1993 survey arrived at the European continental slope in the summer of 1996; 
the eastward spreading has now come to a rest. The core now is detached again from 
the slope (fig. 27 to 29). The northward progress of the AABW observed earlier on 
in the 1990s has also come to rest. In the west the 1997 section shows a colder and 
fresher Labrador Current in the top 500 m, and at ca. 2000 m a comparably 
pronounced core of the Deep Western Boundary Current. Indications at present are, 
that the meridional overturning circulation is returning to the one-cell case last 
observed in the 1980s (KOLTERMANN et al., 1998a).

Fig. 27:Potential temperature theta along the A2 section during M39/3, June 1997.

Fig. 28:Salinity S along the A4 section during M39/3, June 1997.

Fig. 29:Dissolved oxygen O2 in µmol/kg along the A2 section during M39/3, June 1997.

a) CTD Data Processing (H.-J. Weichert)

A total of 90 CTD profiles was processed from 66 full-depth stations. Due to CTD 
problems at the beginning of the cruise strict control of instrument combinations 
and the relevant acquisition software had to be assured.

The following CTD systems were used

	DHI-1	7 profiles
	DHI-2	11 profiles
	FSI	1 profile
	BSH-2	40 profiles
	NB3	31 profiles,

of which for the routine operation the CTD systems NB3 from Kiel and BSH-2 were 
deployed for alternating shallow and deep casts.

The individual steps in processing the CTD data are documented with the following 
file suffices:

*.FRM	ctd_form and inserting the Header (ctd_hdinj) for conversion from raw data 
	(counts) to physical units, 
*.ARF	ctd_clean with time-lag-correction, monotonized in pressure, 
*.ARC	ctd_cal with laboratory calibration polynom applied,
	DHI1:pressure and temperature 
	DHI2: pressure 
*.FLT	tsctd_filter filtered with double median and single running mean filters. 
	This includes optional correction by hand (ctd_inter). This is the last 
	version of processing onboard.

For processing the BSH-2 data the HDR-file had to modified, the previous version 
was saved as *.HDRor. For the NB3 probe the header was introduced under DHI1 in the 
HDR files. This was cancelled in the final version of the data. For the oxygen 
channels of the NB3 further software modifications had to be made to compensate the 
differing sampling rates.

Despite the problems in setting up the routine CTD/rosette packages, the CTD data 
are of good quality. Only for three casts we needed to use manual editing 
programmes. One of these profiles had to be "repaired" in its bottom part. 
Individual comments for these three profiles are:

#283002:distinct offset in C and T at ca. 1300 dbar, unrealistic values at the 
	bottom. Further processing required,
#284001:sudden offset in C only between 3000 and 3700 dbar; editing finished on 
	board, 88
#313001:non-linear offset in C between 1100 and 4100 dbar; to be processed 
	again in BSH.

All data were backed-up on different media and machines. For further information 
see leg M39/5.

b) Bottle Data Processing (G. Stelter)

During the cruise preliminary files *.SUM and *.SEA were produced according to the 
WHP Operations Manual subject to final inspection after the cruise. The *.SUM file 
contains all station information and is given in List 7.3.1. The *.SEA file gives 
all measurements available at this time from analyses of sea water samples drawn 
from the CTD/rosette system.

All data were merged from the onboard analysis streams into these files. They were 
cross-checked and inconsistencies discussed with the data originators. Corrections 
and comments were entered into a third, metadata, file *.DOC. For the first 
evaluation of the data, instrument and analysis performance from each cast profile 
and property/property plots were made. These were also compared to data from the 
previous cruises to assess the instrument performance and potentially detect 
changes in the ocean.

All data and the relevant information were used in a preliminary data report 
prepared for all participants at the end of this leg.

c) Salinity Analysis (A. Frohse)

Salinity analysis during the cruise encountered no problems besides the usual tear 
and wear. The same procedure and equipment was used as described under leg M39/5. 
The electronic stability (SBY, zero-reading) was extremely stable (±1 digit). Only 
the IAPSO batch P129 showed for two ampoules irreproducible results. We used 42 
ampoules for some 100 calibration measurements, that is after ca. 40 samples. In 
Fig. 30 we give the mean values of the deviations of all calibration measurements 
from a salinity of 34.998 against station number.

For 30 samples of a sub-standard of Atlantic Water (sampled on June 1, 1997 at 
52ƒ44.97 N and 35ƒ0.00 W from 1300 dbar depth Fig. 31 shows the deviations from the 
mean, 34.8973. It indicates that these deviations all lie within the 0.001 limit.

d) LADCP measurements (F. Morsdorf, G. Stelter)

The LADCP-system (153 kHz) used on legs M39/2 and M39/5 on loan from IfMK was also 
used during this leg. It was attached to the rosette system. For maintenance 
purposes the LADCP was not used on stations 287 to 289. In total 56 profiles over 
the entire water depth were sampled. All profiles were analyzed on board. 
Navigation of the data was done using the ship's GPS-system.

e) XBT measurements (Ch. Stransky)

For the entire length of the A2 section XBT probes were dropped after leaving the 
CTD station and at mid-distance points between stations. A total of 133 drops were 
made, resolving the temperature field of the top 1850 m at sub-eddy scale. Probes 
of the T-5 type were used for most drops. Only at water depths less than 800 m Deep 
Blue probes were deployed. During most measurements the ship's speed was reduced to 
6 kn to make maximum use of the probes maximum depth. The quality of the data is 
good, there were only few drops were either the probes did not work properly or 
other errors occurred due to bad grounding.

Data were processed on board and all profiles were submitted to BSH in near real-
time.

Fig. 30:Deviations of salinity measurements from the mean of all calibration 
	measurements, IAPSO batch P129.

Fig. 31:Deviations of salinity measurements from the mean of 30 samples of 
	Atlantic Water sub-standard

5.2.1.2 Nutrients and Oxygen Measurements
a) Nutrients Measurements (R. Kramer, H. Tacke)

We have analyzed sea water samples for the nutrients (PO4-P), nitrate (total sum of 
nitrate+nitrite, NO3 +NO2-N) and silicate (SiO4-Si) using automatic photometric 
methods. For quality assurance purposes during the cruise in each analysis run we 
measured mixing standards 3 and 5 as a sample. In addition three calibration casts 
were used to estimate the overall error of these measurements. The Q-standard (sea 
water samples of the first rosette cast) could not be analyzed because of a failure 
of the air conditioning unit. All analyses were worked in continuous shifts.

Equipment
We used
	a Skalar SA 4000 Analysersystem, Matrixphotometer Typ 6250
	Skalar Software 6.2
	calibrated Eppendorf-, Finn- and glass pipettes for the standard solutions
	calibrated flasks for the standard solutions

Methods
PO4-P, measurement range: 0,01-4,0 µmol/l
	According to MURPHY and RILEY (1962)
	Absorption of the blue Phosphorusmolybdat complex was measured at 880 nm,
	proportional to the concentration. Reaction at 38ƒC

NO3+NO2-N, measurements range: 1,0- 30,0 µmol/l
	According to BENDSCHNEIDER and ROBINSON (1952)
	The colour complex was measured at 540 nm. Chemical reaction at lab 
	temperature.

SiO4-Si, range : 1,0- 50,0 µmol/l
	According to KOROLEFF (1971)
	The absorption of the blue Siliciummolybdat complex was measured at 810 nm, 
	proportional to the silicate concentration. Reaction at ~30ƒC

Procedure:

Samples were drawn directly at the rosette bottle. PE-bottles at 250 ml were rinsed 
three times with the sample and filled up to the lower edge of the shoulder. The 
sample bottles were kept wet with the remnants of the previous sample. For the 
analysis samples were filled into 8 ml cups, after rinsing three times with the 
sample water or the standard. During the entire cruise 40 cups were in constant use 
and kept wet during that time.

Standards were prepared daily. For each CTD/rosette cast a linear calibration was 
made for all nutrient parameters.

Precision

On three stations calibration casts were added to estimate the reproducibility and 
overall error of measurements

Station	depth		NO3+NO2 ± std dev	PO4 ± std dev	SiO4-Si ± std dev
	dbar		µmol/l			µmol/l		µmol/l
274/1	3500.7±0.47	21.750±0.196 0.89 %	1.432±0.034	39.298±0.23 0.60 %
320/4	3758.5±2.31	17.451±0.130 0.74 %	1.114±0.040	21.599±0.18 0.83 %
326/1	2301.3±1.41	17.429±0.102 0.59 %	1.096±0.067	14.431±0.22 1.53 %

b) Oxygen Measurements (F. Schmiel, A. Gottschalk)

Dissolved oxygen was measured by the Winkler method modified by Carpenter with a 
Metrohm Titroprozessor and a double platinum electrode. The dissolved oxygen 
content of seawater was defined as ml per liter seawater.

Precision

Multiple samples from fixed depths were taken on three calibration stations. For 
oxygen the overall error estimated was

Station	depth		O2 ± std dev	percent
	dbar		ml/l		%
274/1	3500.7 ± 0.47	6.619 ± 0.041	0.74
320/4	3758.5 ± 2.31	6.282 ± 0.012	0.19
326/1	2301.3 ± 1.41	6.326 ± 0.014	0.23

c) Tracer-Oceanography (CFCs, Tritium and Helium) 
(K. Bulsiewicz, U. Fleischmann, G. Fraas, R. Gleiss, V. Sommer)

The investigated tracers are carbon tetrachloride (CCl4) and the 
chlorofluorocarbons (CFC) F-11, F-12, F-113 as well as tritium and the noble gases 
Helium and Neon. The time dependent input of the CFCs, CCl4, tritium and helium at 
the ocean surface is known. The tracer concentration of the surface water is 
altered by mixing processes when the water descends to deeper levels of the ocean. 
The helium concentration is altered additionally by degassing at the sea floor and 
by tritium decay. Measuring the concentration of the tracers delivers information 
about time scales of ventilation processes of subsurface water.

The atmospheric F-11 and F-12 contents increased monotonously with different rates 
from the forties until the beginning of the nineties. CCl4 increases since 1920 
while F-113 started to increase 1970. CFC and CCl4 concentrations and their ratios 
vary over wide ranges and are used to estimate the 'age' of water masses (i.e. time 
since leaving the surface). 'Younger' water is tagged with higher CFC 
concentrations compared with 'older' water.

Tritium and 3Helium are used to determine the 'age' by inverting the law of 
radioactive decay after the tritiugenic part of the 3Helium is separated from the 
other components. Helium can be used additionally to trace water masses with 
terrigenic helium as the Antarctic Bottom Water and the Mediterranean Water.

Sampling and Measurements

The CFC's F-11, F-12, F-113 and the tracer CCl4 were measured on board on the 
majority of stations using a gaschromatographic system. All measurements were done 
according to the WHP- standards.

For Helium and tritium measurements (on shore) water samples were filled in copper 
tubes and glass bottles respectively on approximately every second station. A new 
sampling procedure for helium was tested, for which the water is filled in flame-
sealed glass ampoules. The advantage of this sampling procedure is to shorten the 
measuring process in the laboratory.

Altogether we occupied 53 stations and analyzed 779 water samples for CFCs. 550 
samples were taken for helium and tritium. 80 water samples were taken in flame-
sealed glass ampoules.

Preliminary results

The antarctic-influenced bottom water of the eastern North-Atlantic is identified 
in the eastern basin close to the European shelf break by the lowest CFC values 
(Fig. 32) deep eastern basin below 2500 meters the values are rising on isobaths 
from east to west. This is due to the influence of ventilated overflow water from 
the Norwegian Sea, which reaches the eastern basin as Iceland- Scotland-Overflow-
Water and is fed into the recirculation of the Westeuropean Basin. In the depth 
range between 1500 and 2500 meters a maximum layer is found in both basins that is 
related to the Labrador Sea Water. Different cores can be seen in the CFC maximum-
layer. At 30ƒW a core with very fresh LSW is found with extremely high CFC-values. 
The surface water concentrations are slightly supersaturated compared with air 
concentrations.

In the western basin the deepest samples of most of the station had higher CFC 
values than the water above. The absolute minimum was mostly reached between 300 
and 1000 meters above the bottom. The elevated values at the bottom are again 
caused by the influence of overflow water from the Norwegian Sea, here the Denmark-
Strait-Overflow-Water. Close to the North American Shelf the Deep Western Boundary 
Current can be identified. One core with high CFC (Fig. 33) and CCl4 values is 
found in a depth of about 4000 meters and high values are found from the surface 
down to more than 1500 meters.

The structures described above are very similar for all tracers measured on board. 
There is a broad minimum in the range of the intermediate waters for CCl4. This is 
caused by its instability for water above 10ƒC.

The preliminary results for the CFC measurements show a significant rise in tracer 
concentration in comparison with the data set from the WHP-A2 section 1994 (M30/2). 
An exception was found in the eastern basin. A LSW-core with very high 
concentration was found there in 1994, but not this time. In 1994 some deep 
stations were found in the eastern part of the North American Basin that had an 
obvious CFC-minimum at the bottom due to an influence of northward flowing 
Antarctic Bottom Water. No such stations were found this time.

The water sampling for Helium in sealed glass ampoules turned out to be quite 
successful [ROETHER et al. 1998]. The ampoules were safe to handle also under rough 
field conditions. The new method is capable of giving good data, especially for the 
ratios of Helium and Neon, which are the basis of our interpretation of helium 
data. The new sampling method has about the same blank as the copper tube sampling. 
But a certain air contamination still exists in the glass ampoules which shows up 
as an offset and a lesser reproducibility in helium concentrations compared to 
copper tube sampling.

Fig. 32:CFC-113 measurements along the WHP section A2 during M39/3, June 1997.

Fig. 33:CFC-11 measurements along the WHP section A2 during M39/3, June 1997.

5.2.1.4 Mooring work and float deployment (H. Giese, K. P. Koltermann)
a) Mooring work

West of the Mid-Atlantic Ridge two moorings were recovered and re-deployed. They 
were set to cover over the full water-depth the eastern boundary current system 
which shows a complicated baroclinic structure in hydrographic surveys. Besides the 
question whether the core of the Labrador Sea Water LSW is arriving from the south 
or north a further core at ca. 2200 m with slightly higher salinities is monitored. 
These details are imbedded in the general circulation west of the ridge and is not 
clear if there is a re-circulation within the Newfoundland Basin, feeding the 
boundary current from the west and south or whether this re-circulation is 
instationary. These sites have been maintained intermittently since July 1993. 
Moorings deployed during the Gauss cruise G276 in May 1996 were recovered without 
any problems.

Each of the moorings deployed in 1996 and recovered during this cruise is made up 
of 5 current- meters, 3 thermistor strings and 5 SeaCats each. Further 
instrumentation details are given in Tab. 7.

Tab. 7: Table of moored instrumentation recovered during M39/3*

Tab. 8: Table of moored instrumentation deployed during M39/3*

* Tables 7 and 8 are shown in the pdf file.

For the deployment during this cruise the mooring instrumentation varied slightly. 
Mooring K1/97 was instrumented with 5 current-meters, 3 SeaCats and no thermistor 
strings, K3/97 was fully instrumented with 5 current-meters, 3 thermistor strings 
and 3 SeaCats. These moorings have been recovered without losses and problems 
during the Gauss cruise G316/1 in May 1998. Further instrumentation details are 
given in Tab. 8.

Preliminary results

At both sites the flow is largely barotropic and stationary. At the easternmost 
site K1 it has mainly an E-W preference, at K3 in the West is SW - NE. The main 
baroclinic feature is the stronger flow in the LSW layer, roughly between 1000 and 
1700 m. As in previous deployments the flow is from June to December towards the 
East. At site K3, the western mooring, it then changes from SW to directly West, 
whereas at site K1 it changes direction from SW to North. The salinity and 
temperature data at the moorings and particularly at K1 again show the arrival and 
existence of the LSW in the first half of the year, roughly from December to about 
June/ July. In the second half temperatures and salinities increase dramatically 
and coincide with the increased northward component of the flow at site K1.

b) Float deployments (K. P. Koltermann)

Three C-PALACE float were deployed during this cruise leg to add information on the 
larger- scale Lagrangian flow-field at 1500 m depth and monthly CTD-Profiles around 
the mooring sites. Sensor and mission details comply with the WOCE float programme 
in this region. These float with a duty cycle of 30 days therefore complement the 
present intense WOCE Float Programme in the Subpolar and Subtropical Gyres.

The deployment details are:

float	stat	start time	deploy. time	deploy. position
#719	302	6/20/97		6/20/97		lat: 46 54.772 N
		18:19:16	20:41:10	lon: 27 18.393 W
#720	304	6/20/97		6/21/97		lat: 46 32.419 N
		16:57:40	10:40:00	lon: 29 08.404 W
#718	307	6/22/97		6/22/97		lat: 45 49.733 N
		09:35:21	14:14:00	lon: 31 36.639 W

Note: All times are UTC.

5.2.1.5 "TCO2 and Total Alkalinity Measurements along 48ƒN on the WHP section A2, 
	1997" (C. Neill, E. Lewis)

Samples were collected and analyzed on ship for total alkalinity and dissolved 
inorganic carbon (DIC). Other samples were collected for on-shore analysis for 
dissolved organic carbon by Dr. Dennis Hansell of the Bermuda Biological Station 
for Research and for 13C by Dr. Arne Koertzinger of the Kiel Institut of Marine 
Research. This report discusses the total alkalinity measurements.

Methods
General

Samples were collected and analyzed in alternating 12-hour shifts. Samples were 
first analyzed on the SOMMA (single operator multi-parameter metabolic analyzer) 
for DIC, after which they were titrated for alkalinity. DIC was analyzed first 
since it is affected by CO2 exchange with the atmosphere, unlike alkalinity. 
Software and hardware from Kiel was used to determine the total alkalinity in units 
µmol/kg. All post-cruise data processing was done by Ernie Lewis.

Sample Collection and Storage

Samples were collected in 700 ml bottles with ground glass stoppers directly from 
the Niskin bottles, allowing for an overflow of at least one full bottle volume. 
They were stored in the dark at 3ƒC until being analyzed for DIC, then they were 
warmed in a water bath to 25ƒC before being titrated to determine total alkalinity. 
All samples were analyzed within 24 hours of being collected.

Instrumentation

The titrations were made using a Metrohm 665 Dosimat and a Metrohm 713 pH meter 
with an Orion Ross electrode and an Orion double junction reference electrode 
filled with 0.7 molar NaCl. The equipment is computer controlled, and other than 
filling and rinsing the cell, the titration and data collection is fully automatic. 
The cell was a plexiglass cell containing about 100 ml of sample and was 
thermostated to remain at 25ƒC. The equipment used was on loan from Dr. Ludger 
Mintrop of the Institut of Marine Research at Kiel. It was already on board and was 
used by researchers from that laboratory for the previous leg and the following 
leg. A glass pipette for sample delivery is an integral part of the system and was 
calibrated both before and after the cruise by researchers at Kiel. The volume 
determination performed after the cruise suffered from poor reproducibility, so the 
volume determined before the cruise was used: 99.014 (±.043) ml. This was used with 
the density of the sample (calculated from the bottle salinity and measured 
temperature) to determine the mass of seawater being titrated.

Titration Analysis

Samples were equilibrated at 25ƒC and titrated with the HCl/NaCl mixture. The EMF 
of the electrode pair was recorded for 20 volume additions of the acid mixture. 
These values were fit using Kiel's software to determine the values of alkalinity, 
DIC, E0 for the electrode pair, and pK1 for carbonic acid which result in the least 
square deviation from the measured values of the EMF. The value of SSS (the rms 
error of the fit in units Ïmol) is also given. Values of DIC, E0, and pK1 
determined in this fashion are not reliable as they are highly correlated, but the 
method is very robust for determination of alkalinity. The value of SSS is 
sometimes an indicator of problems during a titration. Generally values <.5 are 
considered acceptable, with higher values meaning that the fit is poor, though the 
alkalinity value determined from that fit might still be accurate.

The strength of the acid (a mixture of HCl and NaCl) used for titration was 
determined by Dr. Andrew Dickson of the Scripps Institute of Oceanography to be 
0.097723 mol/kg, with a density of 1.0232 kg/l at 24.13ƒC. Using the formula given 
in the DOE Handbook the density at 25ƒC was found to be 1.0228 kg/l, yielding a 
value of .099951 mol/l as the value used for the acid mixture. Since the dosimat 
gives the volume of the acid dispensed, this value will tell the number of 
equivalents (moles) of acid used to titrate the sample.

Quality Control

Replicate analyses were performed on 1 out of every 10 samples. Typically samples 
with Bedford ID numbers ending in 0 were sampled twice and analyzed separately as 
independent samples. In addition, two different batches of CRMS (Certified 
Reference Materials) provided by Dr. Andrew Dickson of the Scripps Institute for 
Oceanography and certified for alkalinity, were analyzed to check the overall 
accuracy as well as the precision of the analyses.

Sampling Locations

Of the more than 1500 samples which were taken on 86 casts at 66 stations, 689 
samples (including 61 replicate samples) from 33 stations were analyzed for 
alkalinity. At least one station per day was fully analyzed, except for one day 
when the SOMMA was down. Samples from the following stations were analyzed for 
alkalinity (# of depths sampled in parentheses):

275 (19)	277 (20)	279 (13)	282 (5) 	283 (22)	285 (21)
288 (19)	291 (37)	293 (31)	295 (21)	297 (21)	299 (22)
301 (22)	302 (17)	304 (21)	305 (20)	307 (20)	309 (20)
311 (10)	314 (22)	317 (23)	319 (21)	321 (18)	322 (12)
323 (32)	325 (23)	327 (22)	329 (21)	331 (6)	332 (22)
334 (13)	336 (8) 	337 (4)

Salinities Used for Calculations

Salinity is needed to convert from the volume of the pipette to the mass of 
seawater so the alkalinity can be expressed in µmol/kg. Errors in salinity affect 
alkalinity only slightly: an error of 1 in salinity will result in an error of 
about 1.5 µmol/kg in alkalinity, which is less than the precision as determined by 
replicate analyses.

The salinity values were taken from the CTD data provided by the chief scientist. 
For six samples bottle salinities were not available and were estimated from CTD 
salinity and bottle salinities of nearby samples:
	Bedford ID#	salinity
	200688		35.600
	200969		34.950
	201238		35.843
	201266		34.940
	201470		36.010
	201846		35.050

Sample 201468 misfired and the salinity from the SOMMA salinity cell, 36.010, was 
used instead of the value 30.077 given in the CTD reports.

ID values 200985-200994 and 201803-201804 were used twice. We only sampled on the 
second occurrence, so I deleted the first occurrence of these. All of these changes 
were documented in the hydrography master file.

Data

The values from the calculations are in the file M39_3AT.XLS. This file has 13 
columns, one for each of the following: Bedford ID (unique for each sample), QC 
flag, station, cast, Niskin, salinity, pressure (dbar), alkalinity, DIC determined 
from the alkalinity titration, DIC determined from the SOMMA, E0, pK1, and SSS (the 
error of the titration fit).

QC flags were assigned to each sample as follows:
	2 = acceptable measurement
	3 = questionable measurement (value of SSS > .5 µmol but < 1 µmol)
	4 = unacceptable measurement (value of SSS > 1 µmol)
	5 = sample analysis failed (-9 entered for all values)
	9 = sample not analyzed for alkalinity

The alkalinity analyses on the cruise were remarkably free from errors. The vast 
majority of the samples (666) were assigned a flag of 2. Only 17 samples were 
assigned a flag of 3, and 6 samples were assigned a value of 4. Two samples were 
assigned a flag of 5, and two samples were assigned a flag of 9.

The 6 samples which were assigned a flag of 4 all occurred during the first station 
(275). It is typical for electrodes to become conditioned with use and perform 
better than if they have been sitting unused, so the fact that all of these 
occurred on the first station is understandable. It is worth noting that although 
high values of SSS indicate that the fit is poor, it does not necessarily indicate 
that the alkalinity value determined from the fit is inaccurate.

The two samples with the flag 5 were those for which alkalinity titrations were 
started but did not finish. In one case the computer hung and the titration had to 
be aborted (201275); in the other the stir bar was not turned on and the titration 
was aborted (201178). All samples which were analyzed for DIC were also analyzed 
for alkalinity except for two (200602 and 200623) on the first station (274), which 
was used for testing purposes.

Other possible errors which may occur in alkalinity titrations include bubbles in 
the acid line and incomplete rinsing. In the first case, it appears that more acid 
was added than actually was, leading to an over- estimation of the alkalinity. In 
the second case, some alkalinity is titrated before any acid is added, leading to 
under-estimation of the alkalinity. Both of these are difficult to determine. Plots 
of alkalinity vs. depth show a few points which look out of profile which may be 
due to these reasons.

Precision and Accuracy

Precision is determined by analyzing replicate samples and by analyzing Certified 
Reference Materials. Accuracy is estimated from comparing values of the Certified 
Reference Materials with the certified values.

A total of 61 pairs of replicate samples were analyzed. The replicate sample data 
are summarized in file M39_3RAT.XLS. The mean difference was 2.9 µmol/kg, which is 
good compared to other cruises on which I have performed alkalinity measurements. 
Three of the replicates were between 9 and 11, which are higher than desired. This 
is also typical of other cruises on which I have performed alkalinity titrations.

A total of 59 analyses of Certified Reference Materials were made after they were 
analyzed on the SOMMA for DIC (usually three times per day). Two different batches 
(34 and 36) were used. Data for these are summarized in the file M39_3CAT.XLS. 
Results are summarized in the table below.

CRM	certified	# bottles	mean	standard 
Batch	alkalinity	analyzed	result	deviation
34	2284.35		44		2287.9	3.7
36	2283.83		15		2285.9	3.4

All of the 15 samples of Batch 36 which were analyzed resulted in values which were 
within two standard deviations of the mean. In total, 44 samples of batch 34 were 
analyzed. One sample was started and the cell was found to be open, thus 
invalidating the sample, which was not completed. One sample (bottle 217) was 
analyzed twice. The values obtained during the cruise ranged from 2279.2 to 2299.2. 
No overall drift was detected during the cruise, and the standard deviations, as 
well as the differences between the mean and certified values, are in line with 
values obtained on other cruises.

5.2.2	Leg M39/5
5.2.2.1 Hydrographic Measurements
(A. Sy, K. Bakker, R. Kramer, D. Machoczek, H. Mauritz, F. Schmiel, K. Schulze, 
G. Stelter, M. Stolley, N. Verch)

Operational Details

Following the WOCE Hydrographic Programme requirements, the hydrographic stations 
were worked in one-time survey mode. The station spacing was designed in accordance 
with bathymetry and varied between some 5 nautical miles (nm) and 30 nm. To 
increase the spatial resolution of the hydrographic sampling, temperature profiles 
up to 2000 m depth were also obtained by use of expendable bathythermographs (XBT).

Hydrographic casts were carried out with an NBIS MK-IIIB CTDO2 unit, labeled "DHI-
1". The underwater unit was mounted vertically inside a rosette frame with a 24-
place General Oceanic pylon and 22 x 10 litre Niskin bottles uniquely marked. All 
bottles were equipped with stainless steel springs and grease-free O-rings to avoid 
contamination in CFC sampling. Also attached to the CTD/Rosette system were Benthos 
altimeter, SIS digital temperature meters and pressure meters (DSRT) and, instead 
of 2 Niskin bottles, a self contained lowered ADCP was mounted. The mean constant 
maximum descent rate was 1 m/s. CTDO 2 data were collected at a rate of 64 ms using 
a PC based data acquisition software designed by BSH. A video tape unit was 
operated as a backup system. Hardware and software instrumentation ran without 
serious problems during the whole cruise leg. The rosette system used proved to be 
well adapted to the CTD unit, and thus only few mistrips occurred.

The bottle sampling sequence was as follows. Oxygen samples were collected soon 
after the CTD system had been brought on board and after CFC and 3 He had been 
drawn. The sample water temperature was measured immediately after the oxygen 
sample had been drawn. The next samples drawn were TCO2, 14C, 3H, nutrients (NO2 + 
NO3, SIO3, PO4), 18O and salinity. Salinity samples were collected as pairs of 
replicates to allow cross checks of ship-based and shore based salinity analysis. 
The rosette sampling procedure was completed by readings of electronic DSRTs for a 
first quick check of the scheduled bottle pressure level and for in-situ control of 
the CTD pressure and temperature. An overview of the bottom topography of the WOCE 
section and the locations of water samples is given in Fig. 34a.

47 CTDO2/Rosette profiles at 43 stations were occupied along 5 VEINS sections and 
72 CTDO2/Rosette profiles at 69 stations during the WOCE part of the cruise (Fig. 
9). 7 of the casts were used for system test purposes (cable, CTD/Rosette system 
performance etc.). 3 casts were used for rosette sample quality tests at stat. # 
483, 501 and 534 by means of multi-trips at the same depth level. Activities, 
occurrences and measured parameters are summarized in the attached station listing.

To meet WOCE quality requirements, the processing and quality control of CTD and 
bottle data followed the published guidelines of the WOCE Operations Manual (WHPO 
91-1) as far as their realisation was technically possible on this cruise. Standard 
CTD data processing and bottle data quality control (including salinity, oxygen and 
nutrient samples) were carried out on board during the cruise using BSH designed 
software tools. For salinity analysis of samples a standard Guildline Autosal 
salinometer model 8400 was used on board together with processing software designed 
by SIS. Dissolved oxygen was measured by the Winkler method modified by Carpenter 
with a Metrohm Titroprocessor and a double platinum electrode. Nutrients were 
analysed with a Technicon TRAACS 800 flow autoanalyser. XBTs were dropped following 
the corresponding WOCE requirements (SY, 1991; HANAWA et al., 1995).

Measurements of the classical parameters were supplemented by continuous 
registrations of current profiles using a vessel mounted acoustic Doppler current 
profiler (VM-ADCP) and of sea surface temperatures and salinities using a Seabird 
SBE-21 thermosalinograph (TSG). CTD, TSG and XBT data were transmitted to BSH and 
distributed worldwide in the framework of IGOSS (Integrated Global Ocean Services 
System) in quasi real-time (i.e. within 30 days) as BATHY, TESAC and TRACKOB 
reports. All data will be submitted to the responsible WOCE Hydrographic Programme 
Data Assembly Centre after data processing and quality control has been finished.

Preliminary Results

A selection of property sections from bottle data and CTD data are presented in 
Figs. 34 and 35, which show the main water masses encountered along WHP-A1/E. 
Positions of XBT drops and the temperature field of the main section are shown in 
Figs. 36a,b.

Fig. 34:a) Distribution of water samples along section WHP-A1/E, b) Sample oxygen 
	(ml/l), c) Phosphate (µmol/l), d) Nitrate (µmol/l), e) Silicate (µmol/l).

Fig. 35:CTD property section WHP-A1/E, a) Temperature (ƒC), b) Salinity,
	c) Density.

Fig. 36:a) Positions of XBT profiles, b) XBT temperature section along WHP-A1/E.

The characteristic water mass of the upper layer is the Subpolar Mode Water (SPMW) 
from the North Atlantic Current which has the highest temperatures and salinities. 
At the continental slope off east Greenland, the influence of the East Greenland 
Current is visible transporting polar surface water southwards. The Intermediate 
Water (IW) below SPMW is characterized by an oxygen minimum (VAN AAAKEN and BECKER, 
1996). South of Rockall Plateau and in the same density layer as the IW the 
influence of Mediterranean Water is visible due to its high salinity.

The upper part of the deep layer in both basins shows the Labrador Sea Water (LSW), 
well marked by its low salinity and high oxygen content. In the layer below LSW we 
find dense overflow-type water masses with their well distinguishable cores at the 
East Greenland continental slope (Denmark Strait Overflow Water, DSOW) and at the 
eastern slope of the Reykjanes Ridge (Island Scotland Overflow Water, ISOW). 
Further to the east and after leaving the bottom layer in the deep basins of the 
Porcupine Abyssal Plain, ISOW is transformed into North East Atlantic Deep Water 
(NEADW) by mixing with LSW and the Lower Deep Water (LDW). LDW is marked by low 
salinity, low oxygen content, and a very high silicate concentration of Antarctic 
origin. Therefore, the name Antarctic Bottom Water (AABW) is also used instead of 
LDW. Here, close to the north-western terminus of the AABW tongue, we observed the 
core of this water mass lifting from the bottom (Fig. 37).

Fig. 37:Property profiles of stats. # 551 and 552.

Fig. 38:Change of Labrador Sea Water core properties along WHP-A1/E from 1991 to 
	1998 a) Temperature, b) Pressure.

The outstanding event in the North Atlantic of the late 80s and early 90s was the 
convective Labrador Sea Water formation (LAZIER, 1995) and the spreading of the new 
LSW vintages throughout the North Atlantic. It is believed that the LSW formation 
period, which reached its maximum in the winters of 1992 and 1993, is linked with 
the North Atlantic Oscillation (NAO) (DICKSON et al., 1996). Based on the 
observations along WHP sections A1 and A2, rapid changes of intermediate-depth 
water-mass characteristics were observed (SY et al., 1997), and we were able to 
trace the propagation of a series of new modes of LSW ("1988 LSW cascade") and to 
link these modes to the series of intensifying deep wintertime convection events 
after 1988 in the central Labrador Sea. The appearance of these LSW vintages is 
marked by substantial cooling, deepening and densification of the local LSW core. 
Using the T/S and CFC data independently, the trans-Atlantic travel time from the 
source region to the eastern boundary was estimated to be 4 - 5.5 years (SY et al., 
1997). This surprisingly rapid spreading is confirmed by investigation results 
recently reported by CURRY et al. (1998). Observations made during cruise METEOR 
39/5 reveal no appearance of newly formed LSW (i.e. of vintage 1996 or 1997) in the 
Irminger Sea but show clearly that the exceptional cooling of the intermediate 
waters is still in progress in the West European Basin (Fig. 38a). We found that 
the LSW core layer east of 22ƒW deepened by about 170 m (Fig. 38b) and that the 
mean temperature had decreased by -.13ƒC within the last 13 months.

In the upper ocean we encountered another interesting feature. BERSCH et al. (1998) 
report a strong warming of the Subpolar Mode Water (SPMW) layer between June 1995 
(V152) and August 1996 (V161), which they explain by the contraction of the 
Subpolar Gyre. The westward shift of the Subarctic Front reduces the eastward 
spreading of cold and less saline waters from its western part and increases the 
supply of warm and more saline SPMW from the North Atlantic Current. Obviously this 
is not a short-time event because METEOR 39/5 data show that compared to August 
1996 (M39-V161) the SPMW layer remained anomalously warm also in September 1997 
(Fig. 39). Preliminary estimates of the geostrophic current field reveal 3 branches 
of the North Atlantic Current: west of the Reykjanes Ridge between 35ƒW and 36ƒW, 
and south of the Rockall Plateau between 22ƒW and 25ƒW and at 19ƒW.

Since the early days of WOCE it has been stated that the industrial production of 
expendable CTDs (XCTD) had to be extended with the accuracy and precision needed 
for large-scale measurement of heat and salt storage of the upper ocean in the WOCE 
voluntary observing ship programme (WCRP, 1988). As in the past (SY, 1996) we 
therefore took the opportunity of this WHP cruise to test a new expendable device, 
designed by Tsurumi-Seiki Co. (TSK), Yokohama, against a controlled and accurate 
CTD reference to check the manufacturer's claimed system performance independently. 
The test result shows that the new XCTD system is close to provide the performance 
required by the oceanographic community for upper ocean thermal and salinity 
investigations. Details on the test procedure and results are published in SY 
(1998).

5.2.2.2 Tracer Measurements
a) Chlorofluorocarbon (M. Rhein, M. Reich, L. Czechel)
Technical Aspects

During leg M39/5, the Kiel CFC system worked continuously and about 1550 water 
samples on 99 stations have been analysed. CFC-11 analysis was successfully carried 
out during the cruise, the analysis of the CFC-12 peak, however, was disturbed by 
an unknown substance with a similar retention time as CFC-12. The unknown peak 
affected the precision of the CFC-12 data, but did not influence the accuracy. The 
blanks for CFC-11 and CFC-12 were negligible. Accuracy was checked by analysing 10 
percent of the water samples twice, and was for both substances ±0.5%. The result 
was confirmed by the accuracy obtained at the test stations, where several bottles 
were tripped at the same depths. The accuracy at these test stations was better 
than 0.5% for both substances. The water samples are calibrated with gas standard 
provided by D. Wallace, PMEL, USA and the CFC concentrations are reported on the 
SIO93 scale. All data were analysed on board.

Fig. 39:Differences of horizontally averaged temperature in the SPMW layer of 
	A1/E. Data are vertically averaged at 100 m intervals.

Leg 5 completed the Kiel CFC data set of the M39 cruise, covering the subpolar East 
Atlantic (M39/2) and the West Atlantic (M39/4). A first comparison of the three 
data sets showed that the data are internally consistent.

Preliminary Results

The aims of the CFC analysis are to study the formation and circulation of the deep 
water masses in the subpolar North Atlantic. At the CFC-11 section along A1/East 
(Fig. 40), the thick lines denote the isolines Û-theta = 27.2, 27.8, and 27.88, 
which are chosen as boundaries for the deep water components, the Labrador Sea 
Water (LSW) between 27.74 and 27.80 and the Iceland Scotland Overflow Water (ISOW) 
between 27.80 and 27.88. In the western Atlantic one finds Denmark Strait Overflow 
Water (ISOW) as the densest water mass below Û-theta = 27.88, centred on the 
western flank of the Irminger Sea. In the eastern Atlantic, however, this isopycnal 
is no longer suitable as a water mass boundary. The core of the LSW is shown with 
the stippled line, which denotes the salinity minimum, taken from the CTD stations. 
The lower stippled line represents the salinity maximum of the ISOW, which crosses 
into the western Atlantic through the Gibbs Fracture Zone, and thus is also called 
GFZW (Gibbs Fracture Zone Water).

Fig. 40:CFC-11 section of WHP-A1/E.

In the western Atlantic, the CFC distributions show two intermediate maxima, which 
characterize in mid-depth the LSW and the DSOW, which is found near the bottom. 
Both water masses receive their CFC load by contact with the atmosphere in their 
respective formation regions. The CFC-11 minimum and the salinity maximum belong to 
the ISOW spilling through the GFZ. The ISOW is present in the eastern Atlantic on 
the flank of the Reykjanes Ridge, showing a CFC-11 maximum in the east, because the 
surrounding water masses are CFC poor. At the Reykjanes Ridge, the highest 
salinities and CFCs of the ISOW were found near the bottom. CFC poor water 
penetrates between the LSW and the ISOW, separating the two CFC maxima. The lowest 
CFC-11 concentrations were found in the LDW below 4000 m depth.

The CFC concentrations of the LSW are highest in the Irminger Sea and decrease east 
of the Reykjanes Ridge. Elevated CFC-11 values in the LSW east of the ridge were 
found near 25ƒW. Compared to November 1994 (METEOR cruise M30/3), the CFC-11 signal 
at the salinity minimum of the LSW did not change significantly in the Irminger 
Sea, but increase in the eastern Atlantic. The CFC-11 increase was accompanied by 
cooling of about 0.1ƒC. Both features confirm the short spreading time of LSW into 
the eastern Atlantic.

b) Tritium/Helium, 18O/16O, SF-6 sampling (H. Hildebrandt)
Tritium/Helium

The measuring of tracer concentrations in oceanic water samples provides important 
information in addition to the analysis of the classic hydrographic parameters. One 
particularly useful tracer is tritium (3H) since it takes part in the hydrological 
cycle as 1H3HO and is therefore an almost 'ideal' tracer. Furthermore, this 
radioactive hydrogen isotope decays into 3He with a mean-life of 17.93 a. Since 
tritium is only supplied to the oceans at the atmosphere-ocean boundary, and its 
input function at the surface is well known, the simultaneous measuring of the 
tritium and helium concentration of a water sample allows for the determination of 
an apparent 3H/3He age which yields important information about different water 
masses, such as their time of isolation from the atmosphere and the year of their 
formation ('vintage' age). Taking into account the information gathered from the 
hydrography or other transient tracers the mixing and spreading rates of these 
water masses can be determined as well.

For this purpose, a set of 384 tritium and helium samples was taken during M39/5, 
both on the VEINS and WOCE section. The main focus of the sampling was on the 
Labrador Sea Water and the Denmark Strait Overflow Water. The measurement of 
tritium concentrations and isotopic helium ratios (3He/4He) will be done after the 
cruise at the IUP Heidelberg using mass spectrometry techniques.

18O/16O

Due to the fractionation of the oxygen isotopes 18O and 16O during phase 
transitions of water (e.g. freezing/melting of ice) oceanic samples can have a 
characteristic 18O/16O ratio which allows to identify their origin and to describe 
the mixing rates of different water types. In particular, water containing a 
considerable amount of fresh water (e.g. due to ice melting or river-runoff) shows 
a significantly decreased 18O/16O ratio. This ratio is usually expressed as the 
percent deviation from Standard Mean Ocean Water (delta-18O).

During M39/5, a total of 120 18O samples was taken. If needed, additional 
measurements can be done using the water collected for tritium analysis. Most of 
the samples were taken in and around the East Greenland Current which is much 
fresher than the surrounding water due to its content of Polar Water and melted ice 
from the glaciers of Greenland. The analysis of the samples will again be done at 
the IUP Heidelberg using a mass spectrometer.

SF-6

Sulfur hexafluoride (SF6) has recently become of interest in tracer oceanography 
and is already used in tracer experiments. To determine its usefulness as a 
transient tracer a set of 22 samples was taken during M39/5 for on-shore analysis: 
several surface samples, a profile in the Irminger Sea and one close to the Rockall 
Trough. To check the equilibration of the surface water with the atmosphere 25 air 
samples were taken along the WOCE A1/E section which could also yield information 
about spatial trends in the atmospheric concentration of SF6.

5.2.2.3 Current Measurements
a) Vessel Mounted ADCP (C. Mohn)

Water velocities relative to the ship were recorded continuously in the upper 600 m 
during the whole cruise using a ship-mounted 150 kHz ADCP. The measurements were 
carried out in depth intervals of 16 m within sampling intervals of 6 minutes. Data 
gaps occurred only at a short period of 8 hours at one day during the last week of 
the cruise.

The processing and a preliminary calibration of the ADCP data was performed on 
board using the CODAS software system developed at the University of Hawaii. The 
calibration of the misalignment between the transducer and the ship's axis was 
carried out using a short period of bottom tracking at the beginning of the cruise. 
The tidal correction and final calibration will be performed after the end of the 
cruise using a 2 day period of bottom tracking at the Celtic shelf.

During the cruise high resolution GPS position fixes from the GLONASS GPS 
positioning system were available, which will also be applied to the ADCP data 
after the cruise.

The results of the on board ADCP data processing without tidal correction are 
presented in Fig. 41a - c (VEINS transects) and 42a - c (WOCE transect A1E) for the 
three depth layers 25 - 200 m, 200 - 400 m and 400 - 600 m, respectively. The 
strongest currents during the VEINS transects are associated with the southwestward 
moving East Greenland Current with speeds up to 40 - 50 cm/s in the upper 400 m 
(Fig. 41a, b). Below 400 m the reduced data quality yielded a much coarser current 
pattern.

Fig. 41:VM-ADCP currents along VEINS sections

Fig. 42:VM-ADCP currents along WHP-A1/E

Fig. 43:LADCP currents during M39/5

Fig. 44:LADCP section with WHP-A1/E

Along the WOCE A1E transect the East Greenland Current (40 cm/s) west of the 
Reykjanes Ridge is still clearly visible (Fig. 42a). A divergence of the eastward 
moving North Atlantic Current is visible at approximately 22ƒW near the Rockall 
Plateau. West of Porcupine Bank the northward path of the Shelf Edge Current is 
marked by current speeds in the order of 30-40 cm/s. A comparison between the 
results of the LADCP measurements and the VM-ADCP measurements at the LADCP 
positions at the actual state of data processing showed a satisfying agreement.

b) Lowered ADCP (M. Rhein, M. Reich)

During leg 5, the self contained 153 kHz LADCP from IfM Kiel was used, the same 
system as during leg 4. The LADCP was attached to the CTD/Rosette system. On 
stations 555 - 557 the LADCP was removed from the rosette due to bad weather 
conditions. In total, 98 profiles were obtained reaching from 40 m depth about 100 
m above sea floor. The longest profiles (4270 m) were sampled at stations 559 and 
566, water depths = 4340 m. All profiles were analysed on board. The navigation of 
the LADCP was done with the GLONASS system, which worked successfully during the 
cruise. Comparison of the upper 600 m of the profiles with the data from the vessel 
mounted ADCP confirmed the good quality of the LADCP profiles (Fig. 43). The 
highest velocities were observed in the Irminger Sea sections off Greenland. There, 
the boundary current exhibits southward velocities greater than 20 cm/s throughout 
the water column (Fig. 44). The velocity distribution show band like structures, 
with high velocities reaching down to the bottom. The strongest velocity signal in 
the deep eastern Atlantic near 20ƒW at 2800 - 3900 m depth directed to the 
northwest (Fig. 44) are also present in the geostrophic computations.

c) Mooring Work (J. Read, G. Hargreaves, J. Ashley)

The mooring work is summarized in the table 9 and 10.

Tab. 9: Moorings recovery programme

1. 9504 laid by Bjarni Saemundsson Nov 1995 not found by Valdivia July 1996, traced 
   but not recovered by Bjarni Saemundsson Dec 1996 (dredge failed)
2. 9601 laid by Valdivia, July 1996 (dredge failed)
3. 9602 laid by Valdivia, July 1996 (dredge failed)
4. I.E.S laid by Poseidon August 1996 (recoverd)
5. 9603 laid by Bjarni Saemundsson Dec 1996 (recoverd)
6. 9604 laid by Bjarni Saemundsson Dec 1996 (recoverd)
7. Veins 21 laid by Valdivia, July 1996 (recoverd)
8. Veins 11 laid by Valdivia, July 1996 (dredge failed)
9. Veins 2 laid by W. Herwig 1995 not recovered by Valdivia 1996 (failed)

Tab. 10: 1997 Mooring Positions (Deployments)

MOORING	(OWNER)	 LAT		LONG		DEPTH	DATE/TIME
							19.08.97
FI	(FIMR)	 63ƒ38.20'N	36ƒ47.40'W	1638 m	06:30 UTC
F2	(FIMR)	 63ƒ33.24'N	36ƒ30.14'W	1785 m	08:12
UK1	(CEFAS)	 63ƒ28.63'N	36ƒ17.90'W	1993 m	09:20
IES1	(POL)	 63ƒ28.73'N	36ƒ17.87'W	1991 m	09.29
G1	(IfM-HH) 63ƒ21.85'N	36ƒ04.18'W	2208 m	11:31
IES20	(POL)	 63ƒ21.97'N	36ƒ03.88'W	2209 m	11.46
UK2	(CEFAS)	 63ƒ16.65'N	35ƒ51.47'W	2368 m	13:44
G2	(IfM-HH) 63ƒ07.00'N	35ƒ32.30'W	2590 m	15:15

5.2.2.4 Carbonate chemistry in the Northern Atlantic Ocean
(H. Thomas, B. Schneider, N. Gronau and E. Trost)

The investigations performed on the WOCE A1/E transect during the cruise M39/5 
mainly were focussed on the air sea exchange of CO2 and the analysis of the 
distribution of dissolved inorganic carbon (DIC) within the water column with 
respect to the biological pump. The surface distribution of the partial pressure of 
carbon dioxide (pCO2) was measured continuously during the whole leg, completed by 
surface samples of DIC on each station. Furthermore, at each second station the 
depth profiles of DIC were recorded.

Fig. 45:4 profiles of dissolved inorganic carbon (DIC)

Preliminary results

The common feature of the pCO2 (raw data) is an increase from approx. 300 µatm in 
the northwestern part to approx. 320 µatm in the southeastern part of the 
investigation area. This feature corresponds to the decrease of the nutrient 
concentrations and oxygen saturation as well as to the increase of temperature 
within the surface layer showing the proceeding of the summer in the same 
direction. The distributions of DIC are discussed using the following 4 profiles 
recorded in the different regions of the cruise (Fig. 45). Along the east coast of 
Greenland (Veins leg) below the mixed layer an homogenous level of approx. 2150 
µmol/kg DIC was found. At some stations branches of Denmark Strait Overflow Water 
are visible characterized by slightly lower values, because the increase of the DIC 
due to remineralisation of organic matter within the younger water mass is lower 
than within the overlying older ones. Due to the same reason along the WOCE 
transect the lowest value are observed within the Labrador Sea Water increasing in 
lower and higher depths. The highest values are found within the Antarctic Bottom 
Water with values of approx. 2200 µmol/kg DIC observed clearly at station 559 on 
the Thulean-Lorien transect.

5.3	Other programs
5.3.1	Methane (R. Keir, G. Rehder)
Background

Methane is a trace gas in the atmosphere, and its concentration has varied over 
time. Proxy measurements made in ice cores indicate that over the last 200 years, 
the atmospheric methane has risen from about 700 to 1800 ppb volume, and, on a 
percentage basis, the rise has accelerated during the last decades at a rate faster 
than the rise of atmospheric CO2. As with other transient tracers such as tritium 
and chlorofluorocarbons, the changing atmospheric concentration should result in a 
time dependent net input/output of methane to the ocean, the signature of witch 
should be observable in recently formed deep waters.

In addition to the atmosphere, methane is also influenced by production and 
consumption within the ocean. In the upper ocean, methane appears to be generated 
slowly by some microbial process, judging from weak maximums that sometimes occur 
under the base of the mixed layer. In addition, at hydrothermal vents and cold 
seeps found on compressional margins, methane is released into the deep sea. 
Nevertheless, older deep waters generally appears to have quite low methane 
concentrations due to slow oxidative consumption.

Since the majority of the ocean's deep water is produced in the northern Atlantic, 
it is an area where the changing atmospheric exchange should influence the 
distribution of methane most strongly. In conjunction with the program being 
carried out by the SFB 460, measurements of the distribution of dissolved methane 
and its 13C/12C isotope ratio were carried out on M39/2. The isotope measurements 
should provide an indication of the extent of the methane decrease in the water 
column that is due to oxidation, because this process consumes the lighter isotope 
preferentially. On the other hand, the carbon isotope ratio of methane in the 
atmosphere has remained nearly constant over time, and changes in the distribution 
due to varying atmospheric concentration should not strongly affect the isotope 
ratio in the ocean.

Surface Water pCH4

Since deep waters are formed from surface waters, one needs to observe whether the 
atmosphere does indeed tightly control the methane concentration in the open ocean 
where this formation occurs. During the entire cruise, the partial pressure of 
methane in the surface layer of the ocean as well as in the atmosphere was 
surveyed. This was accomplished by pumping from 5 meters below the surface directly 
to a gas equilibrator located in the wet lab. A sample of the air recirculated in 
the equilibrator is periodically shunted into a gas chromatograph equipped with a 
flame-ionization detector. Both the methane and the CO2 partial pressure were 
measured, the latter by catalytic conversion to methane. These measurements were 
also carried out continuously on air pumped from overtop the bridge into the wet 
lab. The apparatus provides a semi-continuous measurement of the partial pressures 
in the water every twenty minutes and atmospheric measurements every 40 minutes.

The methane partial pressure in the surface water was close to that of the 
atmosphere over the area covered by the cruise track. During the last section as 
warmer waters were encountered, the methane partial pressure of the surface became 
slightly supersaturated, by about 5%.

The CO2 partial pressure measurements by gas chromatography followed closely those 
made by the IfM group using the infrared detector. The CO2 partial pressure was 
more variable than that of methane, but the surface water was always under-
saturated relative to the atmosphere (see 5.1.1.3). Our measured atmospheric CO2 
concentrations agreed very well with those measured with the infrared technique, 
but the pCO2 values measured in the water by gas chromatography were systematically 
lower than obtained from the IfM equilibrator system, by two or three percent. The 
reason for the discrepancy is not known, and this will be investigated subsequently 
ashore.

Discrete CH4 Measurements

In order to measure the dissolved methane in discrete samples from the hydrocasts, 
a new procedure for separating the gas phase from the water was employed. Water 
from the Niskin bottles is drawn into a 200 ml glass syringe without contact to the 
air. The syringe is then connected to an evacuated 500 ml bottle. As the water is 
drawn into this bottle from the syringe, most of the dissolved gas separates from 
the liquid phase. Altogether, 400 ml of water from 2 syringes is added to each 
bottle. The gas is now led into an evaculated burette by injecting a degassed brine 
into the bottom of the sample through a sidearm at atmospheric pressure. At this 
point, 1 ml of gas is extracted and injected into a gas chromatograph equipped with 
a flame ionization detector. The gas remaining in the burette is collected in an 
evaculated vial for isotopic analysis by mass spectrometry ashore. In addition to 
the gas samples, on a few stations separate water samples were collected in air 
free bottles, and these will be returned to the shore-based laboratory for carbon 
isotope analysis. The dissolved gas in these samples will be stripped using helium, 
and the trapped methane injected directly into the mass spectrometer. These isotope 
measurements will be compared to those on the already separated gas samples.

Preliminary results from M39/2

The calculation of the dissolved methane concentration from the measured data 
involves estimation of the total volume of all dissolved gases using nitrogen 
solubility in seawater, which requires temperature and salinity data, and the 
observed dissolved oxygen measurements. Thus, the final work up of our measurements 
will be conducted following the cruise.

The measured methane mole fraction in the gas phase gives a qualitative indication 
of the dissolved concentration in the water, since the total dissolved gas volume 
typically varies by about ±10% in the northeastern Atlantic. As an example of 
results obtained so far, we show the vertical profiles of the methane concentration 
in the extracted gas at Stations 260, 262, 264 and 266 along sections F and G. 
Station 260 was taken directly over the rift valley of the Mid-Atlantic Ridge, just 
south of the Charlie Gibbs Fracture Zone. The other three stations lie 
progressively eastward of the ridge, reaching to the Porcupine Basin. The profiles 
illustrate that the vertical distribution of methane in the upper 2500 meters along 
this line remains relatively constant. Methane in the upper 500 to 600 m is 
relatively uniform at about saturation with the atmospheric partial pressure. The 
concentration decreases over the next 100 meters or so, and then remains fairly 
constant at a value somewhat less than that equivalent to the atmosphere over the 
800 to 2000 m depth range.

In contrast, the deeper methane concentrations show a marked variation in their 
horizontal distribution. Below the rim of the rift valley, the methane 
concentration increases rapidly to values greater than found in the surface water. 
Evidently, hydrothermal venting is supplying a source to the waters within the 
valley, but overtop the rim, the deep circulation sweeps away the excess. Away from 
the ridge, in the eastern basin, the deepest waters contain quite low methane 
concentrations. This is apparently due to the fact that this water is relatively 
old, having a component of Antarctic Bottom Water that has found its way into the 
eastern basin through the Romanche Fracture in the Mid-Atlantic Ridge at the 
equator.

Preliminary results from M39/4

As for leg M39/2, the final work up of our measurements will be conducted following 
the cruise. However, the measured methane mole fraction in the gas phase gives a 
qualitative indication of the dissolved concentration in the water, since the total 
dissolved gas volume typically varies by about ±10% in the northwestern Atlantic. 
The vertical distribution of this property is presented along 3 sections consisting 
of profiles 22-33, 34-57, and 88-103. As a preliminary observation, it appears that 
the pattern of these distributions is quite similar to those of chlorofluorocarbon 
and dissolved oxygen. This clearly indicates that water mass "age" or degree of 
ventilation with the atmosphere has an important influence on the methane 
concentration in relatively recently formed waters.

In regard to methane in the upper water column, the methane partial pressure in the 
surface water was consistently in equilibrium with the atmosphere over the most of 
the area covered by the equilibrator survey. A slight over-saturation occurred 
during the short transit over shelf waters (200 m depth) near Greenland. A 
preliminary indication from the station data indicates that the upper few hundred 
meters of the water column generally have concentrations equivalent to the 
atmospheric concentration. However, a subsurface maximum was found at about 54ƒN on 
the N-S section from Cape Farvel, indicative of production in the upper water 
column (Section profiles 34-57). The maximum is found at the top of the 
thermocline, at a depth of about 200 m.

5.3.2	Tritium/helium sampling program results from M39, legs 4 and 5
(H. Hildebrandt, M. Arnold, R. Bayer)

The preparation of the water samples obtained during M39 for analyses of the helium 
isotopes and the tritium content started soon after arrival of the samples at the 
Heidelberg laboratory. The procedure includes the quantitative extraction of helium 
from the water and transfer of the gases in a glass ampoule as well as storage of 
the degassed water for ingrowth of 3He in a preconditioned glass bulb. The 
measurements are performed in a dedicated helium isotope mass spectrometer which is 
accessible for helium measurements of samples from M39 since January, 1998. Mass 
spectrometric tritium analyses may be performed after a sample storage time of 
typically six months and the high quality tritium data production will start in 
summer 1998. Nevertheless, a preview of the tritium distribution at selected 
positions was obtained in the meanwhile by our low-level counting facility (data 
precision lower than obtained from mass spectrometric measurements).

First results obtained from profiles taken along the WOCE WHP-A1/AR7 leg are shown 
in Figure 46 where the spatial and temporal evolution of the mean tracer content in 
the density range of Labrador Sea Water (LSW) is depicted. Evidently and 
principally according to the transient input and the radioactive decay of tritium 
the concentrations (upper panel of the figure) decreased since our last occupation 
of the leg in 1994, the same trend was observed between 1991 and 1994. The second 
panel attributes to the transient character and shows all the data points currently 
available normalized to a common date, i.e. start of 1991 (tritium concentrations 
are given as TU91); in this plot almost no temporal variability is visible. On the 
contrary the 3He excess concentrations in LSW at least in the western part of the 
subpolar North Atlantic changed since 1994 (third panel, 3He is presented in a 
delta notation giving the per cent deviation of the 3He content of the samples from 
that of surface water in equilibrium with the atmosphere): in the Labrador Sea and 
in the Irminger Sea delta-3He increased from 2% to 3-4%, a feature that is probably 
related to the ventilation rate of LSW which, according to hydrographic 
observations, diminished since 1994. This is also visible from the lower panel of 
the figure which presents formally calculated tritium/3He ages in the LSW: 
apparently the LSW ages obtained from the M39 cruise increased by about 3-4 years 
compared to the situation in 1994. Further measurements are in progress and a more 
detailed discussion of the tracer distribution and its variability will be 
performed as the data set growths.

Fig. 46:Spatial and temporal evolution of tritium and delta 3He in the density 
	range of the Labrador Sea Water.

5.4.	Paleoceanography
5.4.1	Water Column T-S Profiling (M. Huels, S. Jung, R. Zahn)
Methods

During METEOR cruise M39/1, a CTD/Rosette water sampler was deployed at 9 stations 
in water depths of 500-3500 m to obtain vertical temperature and salinity profiles 
as well as water samples. The Seabird Electronics CTD device consisted of 
supplementary oxygen and transmissivity sensors, a twelve-10l-Niskin bottle rosette 
and a Seabird Electronics 911 Plus deck unit. The CTD/Rosette unit was coupled on-
line to a PC. The raw data set will be post- processed shore-based. Firing 
sequences for the Niskin bottles were chosen based on the downcast T/S-profiles. 
Down-cast and up-cast speeds were 0.5 m/s. Close to the sea floor, down-cast speed 
was reduced to 0.2 m/s. In order to prevent a touchdown on the sea floor. A 
"pinger" echosounder was used in addition to a bottom sensor to monitor the CTD's 
approach to the sea-floor.

Immediately after retrieval on deck a series of water samples was siphoned off for 
a suite of geochemical analysis (see below). Water samples for _18O and _13C 
analyses were poisoned with HgCl2 to suppress biological activity. Subsequently, 
these samples where closed airtight with a high-vacuum paste and taped for 
transport. A set of water samples was sealed airtight in glas bottles for later 
salinometry to check the calibration of the salinity probe. Stable isotope analysis 
will be performed on selected water samples post-cruise at the Leibniz Labor for 
Isotope Research, Kiel University.

Results

The most prominent T-S component in the hydrographic profiles is derived from warm-
saline MOW that enters the Gulf of Cadiz at a depth of approximately 280 m. T-S 
anomalies that are associated with MOW are strongest developed in the northern Gulf 
of Cadiz where MOW flows along the southern Portuguese margin. Advection of MOW it 
has resulted in the development of the Faro Drift, a vast sediment body that 
consists of sediments accumulated and sorted under MOW-related current activities. 
Acoustic surveys of the Faro Drift show distinct subbottom reflectors that clearly 
document the current-induced built-up and lateral extension of the Faro Drift (see 
Figure 57 below) due to the advection of MOW. To trace the evolution of MOW upon 
its entry in the Gulf of Cadiz and further North, along the western Iberian margin, 
CTD stations were targeted at the flow path of MOW (Figures 47, 48).

CTD casts from stations in the Gulf of Cadiz, i.e. close to the MOW "point-source" 
at the Strait of Gibraltar, most distinctly display the vertical T-S-variations 
into the MOW. At these stations, MOW impinges on the sea floor and is recorded in 
elevated T-S values in the near-bottom layer (Figure 47) , it is encountered except 
of cast M39029. At Stations M39017 and M39021, a separation into an Upper MOW (T-S-
maxima at 430 and 500 m water depth, respectively) and a Lower MOW was possible 
(upper boundary at 510 m and 610 m water depth, respectively; Figure 47). Along the 
MOW flow path, the surface of lower MOW deepens from 500-600 m water depth at 
Stations M39017 and -021 in the northern Gulf of Cadiz to 1000 m at Station M39029 
in the outer Gulf of Cadiz. Maximum MOW temperature at Station M39029 barely 
reaches 10ƒC and remains well below MOW temperatures of >12ƒC at stations in the 
inner and northern Gulf. Likewise, maximum salinities of some 36 at Station M39029 
are distinctly lower than those recorded in the immediate MOW flow path where 
values exceed 36.5 (Stations M39014 and -021; Figure 47). Rapid decreases of T-S 
values mirror the admixture of Atlantic water masses which results in a continued 
decrease of the T-S anomaly as one moves out the Gulf of Cadiz and northward along 
the western Iberian margin (Figure 48).

Fig. 47:Water column temperature and salinity profiles from CTD runs in the Gulf 
	of Cadiz (M39001-029) and at the western Iberian margin (M390035-073). CTD 
	stations were targeted at the advection path of MOW. Note logarithmic 
	depth sale that was used to better identify T-S fine structure of the 
	upper water column.

5.4.2	Seawater Sampling for Trace Element and Nutrient Analysis 
(A. M¸ller, C. Willamowski)

GoFlo bottles were used to collect water samples for determination of dissolved 
cadmium. With a bottom weight of 40 kg, 5 to 7 bottles with volumes of 3 x 12 l and 
2-4 x 2.5 l were deployed at a time. Down-cast winch speed was 0.5 m/s, up-cast 
speed was 0.8 m/s. Sampling depths were determined based on the CTD T-S profiles. 
After recovery, the GoFlo bottles were brought immediately to the laboratory to be 
emptied under Nitrogen atmosphere. Water samples were then filtered under clean 
conditions of a clean bench. 200 ml of each water sample were discarded, 1 l was 
filtered through a 0.45 µm membrane filter, acidified and stored at +4ƒC. Another 
liter was acidified and stored without previous filtering. Additional samples were 
taken for onboard phosphate analysis. Because the GoFlo bottles are not equipped 
with depth sensors, additional water samples were taken from the deepest bottle for 
salinity analysis. Comparison of the GoFlo salinity values with those from the CTD 
T-S profiles will serve as a control to monitor GoFlo sampling depths in addition 
to the wire length readings. Cd analysis will be performed post- cruise at the IfM 
Kiel.

Water samples for oxygen analysis (double sampling) were taken in 50 ml dark brown 
glass bottles from each CTD-Niskin bottle immediately after retrieval on deck. 
After addition of 0.5 ml of alkaline Iodide and 0.5 ml of Manganese (II) chloride, 
the bottles were vigorously shaken. Prior to analysis, 1 ml of sulfuric acid was 
carefully added and the bottles were shaken to re-dissolve precipitated hydroxides. 
The solution was quantitatively transferred into a beaker with distilled water. 
Titration was carried out immediately with 0.01 mol/l sodium thiosulphate. Shortly 
before disappearance of the yellow color, 1 ml of starch solution was added 
(solution turned blue) and titration finished as soon as the blue color 
disappeared.

For analysis of phosphorus concentration, 50 ml of seawater from CTD Niskin and 
GoFlo bottles were transferred to plastic sample containers. Subsamples of either 5 
or 10 ml were taken and 0.1 (0.2) ml of two mixed reagents were added (reagent 1: 
12.5 g ammonium heptamolybdate tetrahydrate ((NH4)6Mo7O24 * 4H2O) dissolved in 125 
ml distilled water, added to 350 ml of 4.5 mol/l sulphuric acid (while well 
stirring) - and under mixing added 0.5 g of potassium antimonyl tartrate, 
(K(SbO)C4H4O6) in 20 ml water; reagent 2: 10 g of ascorbic acid in 50 ml of 4.5 
mol/l sulfuric acid and 50 ml of distilled water). Samples were transferred into a 
5 ml (10 ml) cuvette and absorbency was measured at 880 nm against acidified 
distilled water as reference. Calibration was carried out with standard solutions 
of 0 to 2 µmol/l Phosphate. Water column oxygen and phosphorus profiles are shown 
in Figures 49 and 50. The data will be used for calibration of dissolved carbon 
isotope and Cd concentrations to regional nutrient inventories.

Water samples for analysis of magnesium, strontium, calcium and CO3 - concentration 
were filled into 250 ml PE-bottles. Before use, all bottles were put in a 2% 
Mucasol-solution for at least one week after which they were rinsed three times 
with normal water to remove tensids and washed twice and finally filled with Milli-
Q water. 1ml of concentrated hydro-chloric acid was added. The bottles were then 
closed and stored at room temperature for three days, subsequently turned upside-
down and again kept at room temperature for three days. Then, the bottles were 
twice rinsed and filled with Milli-Q water, and finally 1ml of concentrated nitric 
acid was added to oxidize remaining particles. The containers were then closed and 
remained at room temperature for three days. This step was repeated after turning 
the bottles upside-down. Finally, the bottles were rinsed twice with, and then 
filled with Milli-Q water. For conservation, 5 drops of concentrated nitric acid 
were added. The bottles were closed, sealed with parafilm, wrapped in foil, and 
stored at 4ƒC. The first step of the pre-sampling treatment of the duranglas 
bottles (250 ml/350 ml) that were used to sample for CO3 - analysis consisted of a 
one day bath in 61ƒC hot solution of Mucasol (3%) to remove fatty compounds. Then, 
these bottles were rinsed once with destilled water and three times with Milli-Q 
water in order to remove tensids. Finally, they were dried at 62ƒC and wrapped in 
foil.

Fig. 48:T-S diagramm showing the hydrographic anomaly that is associated with the 
	advection of warm and saline MOW. Strongest T-S anomalies are recorded at 
	stations close to the immediate flow path of MOW in the northern Gulf of 
	Cadiz (Stations M39001, -014, -017, -021). Decreased T-S values are 
	observed in the outer Gulf of Cadiz (M39029) and at the northern section 
	of the western Iberian margin (M39065, -073) documenting the continued 
	admixture of Atlantic waters.

Immediately after retrieval of the CTD/rosette water sampler (Multicorer) on deck, 
250-350 ml of seawater for CO3Ø analysis were siphoned off the Niskin-bottles to 
prevent CO2-exchange with the atmosphere. The head space of the filled sample 
bottles was kept below 2%. All samples were poisoned with saturated mercury-II-
chloride-solution (250 ml bottles with 50µl saturated mercury-II-chloride-solution 
and 350 ml bottles with 75µl saturated mercury-II-chloride-solution). The bottles 
were immediately closed with a Duranglas cap lubricated with Apizon-L, and 
subsequently sealed airtight. In a second sampling run, 250 ml of seawater (for Mg, 
Sr-analysis) were taken from the CTD-bottles and Multicorer tubes (the PE-bottles 
were emptied 1-3 h before). Prior to sampling, each bottle was washed three times 
with sea water. For conservation, 5 drops of hydrochloric acid were added. The 
bottles were then closed, sealed with parafilm, wrapped in foil, and stored at 4ƒC. 
Trace metal analysis will be performed shore-based in cooperation with the IfM 
Kiel.

Fig. 49:Water column titration oxygen profiles from Niskin bottle water samples in 
	the Gulf of Cadiz (M39001-029) and at the western Iberian margin (M39035-
	073). See Figure 2 for hydrocast positions.

Fig. 50:Water column phosphate profiles from Niskin bottle water samples in the 
	Gulf of Cadiz (M39001-029) and at the western Iberian margin (M39035-073). 
	See figure 2 for hydrocast positions.

5.4.3	Shipboard Sediment Sampling and Core Flow
(G. Bozzano, C. Didie, M. Huels, S. Jung, L. Lembke, N. Loncaric, P. Sch”fer, J. 
Sch–nfeld)

During M39/1 a gravity -, box-, and Multicorer as well as a grabber and a dredge 
were deployed for sediment sampling. Subsampling according to the detailed sampling 
schemes (Figures 51, 52; Table 11) was restricted to sampling of box cores, slicing 
of multicorer tubes, washing of grab samples and dredged material. Sampling of 
sediment cores was mostly postponed to a post- cruise sampling party to facilitate 
standard laboratory procedures and precise determination of physical properties. 
After retrieval of the sediment cores on deck, they were cut into 1 m sections and 
subsequently routinely run through the core logger. Only few sediment cores were 
opened for visual inspection of sediment composition and core quality. These cores 
were routinely cut into working and archive halves. Macroscopic core description, 
color scanning and core photographs were done on archive halves while sediment 
samples were taken from working halves.

Tab. 11: Shipboard Sample Distribution Scheme

INVESTIGATOR		DEVICE		SAMPLE INTERVAL		VOLUME
B. Bader/P. Sch”fer	GKG1, BG2,	surface1, whole		100 cc1,
			Dredge3		sample2,3		macrofauna1
G. Bozzano		SL1,2, GKG1	5 cm1, 1 m2		10 cc1, 4 cc2
S. Jung/R. Zahn		GKG1, SL2	0,2, then 5 cm1, 10 cm2	10 cc
A. Kohly/C. Didi	MUC1, GKG2,	1 core1, top of archive	100 cc2
					core2	
N. Loncaric		MUC1, (GKG2),	1 core1, 10 (5) cm2,3	1-3 cc and 20 cc
			SL3		
A. M¸ller		MUC1, GKG2	1 core1, surface2,	100 cc2,
P. Sch”fer		MUC1 GKG2,	1 core1, archive core2,	x-ray slabs2,3, 100 cc2
			SL3		entire section2,3 (x-ray),	
					surface2	
J. Sch–nfeld		MUC1, GKG2 ,	1 core1,surface2,5 cm3	3 x 88 cc2, to be shared
			SL3					with Anja M¸ller3
C. Willamowski		MUC		1 cm			2 cores
U. Pflaumann		GKG		0, 2, then 5 cm		10 cc
(onshore)			
MUC: multicorer, GKG: box corer, BG: Van Veen grab, SL: gravity corer

The color scanning system consisted of a hand held Minolta photo-spectrometer and a 
transformer. The photo-spectrometer was coupled on-line to a Macintosh Powerbook 
170, on which the ODP- software package "Spectrolog" was run for data management. 
During the color scanning, the sediment sections were covered by ceran wrap to 
prevent sediment smearing onto the measuring unit. Sediment cores were routinely 
scanned at 2 cm intervals.

Fig. 51:M39/1 sampling scheme for Giant Box Core (GKG) sampling.

5.4.4	Plankton Hauls (A. Kohly)
Methods

To study the transfer of living plankton assemblages (and its change) into the 
sediment, plankton net hauls, filtered water samples from the CTD, and sediment 
samples were taken. In total, 32 plankton hauls (mesh width 20 µm) from the 
uppermost 10-12 m were taken. All samples were treated with Formalin to stop 
biological activity. After settling, 3-4 drops of the concentrated plankton 
material were placed on a cover slip for on board microscopic analysis. The seston 
of mostly two liters of CTD/rosette water samples was (vacuum) pumped through a 
cellulose membrane filter with a pore width of 45 µm (diameter of 5 cm) (list 
7.1.2). After drying, the filters were placed in plastic petri dishes, sealed in 
plastic bags and kept dry by using silica gel. This material will be used to 
investigate the vertical distribution of coccolithophors and diatoms and to compare 
it with the species distribution in the underlying surface sediments and sediment 
cores. Detailed scanning electron microscope (SEM) analyses on the plankton samples 
will be carried out post-cruise.

Fig. 52:M39/1 sampling schemes for (a) multicorer tubes, (b) gravity cores. 
	Detailed sampling of gravity cores will be done post-cruise in 
	collaboration with shore-based scientific partners.

Results: Phytoplankton and Zooplankton

Diatoms were the most abundant plankton group in most of the samples. Mainly 
fragile species such as Proboscia alata, Bacteriastrum hyalinum, B. delicatulum, 
Guinardia flaccida, Rhizosolenia fragilissima, R. delicatula and several species of 
the genus Chaetoceros were found. At one station (M39073), coincidentally a bloom 
of Proboscia alata was sampled . A list of identified phyto- and zooplankton 
species or groups is given in list 7.1.3. Dinoflagellates were the second most 
abundant plankton group; at Stations M39001, M39002, M39003, M39017, M39058 they 
even dominate the plankton community. Species of the genera Ceratium, Dinophysis, 
Peridinium, and Prorocentrum frequently occurred, whereas genera Ceratocorys, 
Oxytoxum, Gonyaulax and Diplopeltopsis were less abundant. Specimens of Actiniscus 
pentasterias solely occurred in samples M39006 and M39025 (list 7.1.3). 
Coccolithophorids were merely sampled at single stations, and never reached high 
concentrations. These lower than expected concentrations are probably due to the 
inappropriately coarse mesh width for sampling the small sized coccoliths. 
Furthermore, silicoflagellates (Distephanus speculum and/or Dictyocha fibula) 
occurred in almost 50% of the samples.

Tintinnids were the most abundant zooplankton organisms in the net hauls. Several 
genera were observed such as Amphorides, Rhabdonella, Parafavella, Steenstrupiella, 
Dictyocystis, Tintinnus, Dadayiella and some others with uncertain identification. 
Radiolarians occurred in small amounts and initial stages of their skeletons were 
frequent at a few stations. Both spinous and non-spinous species of planktic 
foraminifera were present in the net hauls.

Macro-zooplankton larvae of different organisms such as copepods and polychaets 
were present in most of the samples, occasionally reaching significant abundances.

In general terms, the highly diverse diatom assemblage is typical for warm water 
regions. The lack of spore specimen in the vegetative cells of Chaetoceros species 
indicates, that the bloom cycle had not been completed. Chaetoceros dadayii and C. 
tetrastichon, warm water (mediterranean type) diatoms were observed with the 
parasitic tintinnid (Tintinnus inquilinus). Areas with low diatom content (outer 
Gulf of Cadiz), are dominated by dinoflagellate species. This group shows a 
dominance of species of Ceratium, Peridinium, and Gonyaulax. Possibly, the diatom 
bloom had finished at these stations or else the surface water was too oligotrophic 
for high diatom abundances.

5.4.5	Porewater Oxygen Profiling: Reference for Benthic Foraminiferal Assemblage 
	Studies (J. Sch–nfeld)
Methods

The profiling instruments were mounted in a shipboard temperature-constant 
laboratory ("Gravimeter-Raum"). A Diamond General 768-20R needle oxygen electrode 
was fixed in an aluminum tube which was centered in the multicorer tube attached to 
the frame (Figure 53). The multicorer tube was pushed upwards with a standard 
laboratory lifting platform, while the electrode remained in a fixed position so 
that the needle was driven into the sediment. The penetration depth is displayed on 
a scale at the platform. The electrode current was measured with a conventional 
picoamperemeter. Electrode specifications and measuring procedures are described by 
DIAMOND GENERAL (1997).

Ambient laboratory temperature was set to the expected bottom-water temperature at 
least twelve hours before the measurements. The room temperature was kept constant 
during the measurements with variations of ±0.25ƒC. The electrode was stored in 
deionized water during transit times and was submersed in seawater at least 4 hours 
before the measurements for stabilization. Calibration of the electrode was done 
immediately before the measurements by relating the current measurements to oxygen 
concentrations of two water samples which were subsequently analyzed by using a 
standard Winkler method (GRASHOFF, 1983). First, we determined the dissolved oxygen 
content of the super-standing water of the multicorer, i.e. the bottom water. A 
second calibration point at low oxygen values was obtained by analyzing a seawater 
sample through which nitrogen was bubbled for at least 30 minutes.

Immediately after retrieval of the multicorer on deck, one tube was sealed with two 
rubber plugs and brought to the temperature-constant laboratory. The upper lid of a 
second tube was opened and the over-standing seawater was transferred into two 
Winkler bottles for bottom-water oxygen determination. Prior to pore water oxygen 
analysis with the needle probe, over-standing seawater was carefully siphoned off 
down to a level of 1 to 3 cm above the sediment surface. The tube was then set on 
the lifting platform, fixed to the frame and the tip of the electrode was moved 
down to a level of one millimeter above the visual upper boundary of the bottom 
nepheloid layer, and was fixed there. The measurement at this point was related to 
the oxygen concentration of the over-standing water. Oxygen readings were allowed 
to stabilize for 12 to 30 minutes. When the readings remained constant for more 
than five minutes, the data were recorded . The lifting platform was then moved 
upwards a few millimeters for the following measurement. The values were recorded 
down to either that level below the sediment surface at which the electrode current 
remains constant or the maximum length of the needle and holder, i.e. 80 mm.

After the measurements, the needle probe was cleaned and submerged in deionized 
water. The sediment was pushed out of the core tube and was cut into 5 or 10 mm 
thick slices which were conserved in a Rose Bengal Methanol solution.

Results: Pore water Oxygen Profiles in Selected Surface Sediment Samples

Pore-water oxygen profiles were measured at four multicorer stations, three from 
the Gulf of Cadiz (M39002-3, M39003-2, and M39029-6 at 1209, 800, and 1918 m water 
depth respectively) and one station off Cape Sines (M39035-3 at 1082 m water 
depth). The depth distribution of dissolved oxygen in the pore waters display a 
characteristic exponential mode as expected from theoretical models (BERNER, 1980; 
GOLOWAY and BENDER, 1982). The shape of the curves is very similar at the shallower 
sites whereas the deep-water site displays a much lower gradient (Figure 54). The 
redox boundary was recorded at depths between 3.9 and 7.1 cm below the sediment 
surface at the shallower sites and it was not encountered at the deep-water site 
from the Gulf of Cadiz indicating that oxygen consumption is low here. Relations to 
Corg contents and sedimentation rates have to be tested and will be a subject of 
post-cruise studies. The boundaries between low oxic, suboxic, and dysoxic pore 
waters are documented at different sediment depths in each core thus offering a 
good opportunity for a core-to-core comparison of the depth distribution of deep 
infaunal species as a function of oxygenation levels at different depths in the 
sediment.

Fig. 53:Laboratory rack with oxygen needle-probe for pore water oxygen 
	measurements. Ambient temperature in the laboratory was held constant at 
	8ƒ-14ƒC, depending on locval bottom water temperature from where the core 
	was retrieved.

Fig. 54:Pore water oxygen profiles at four stations in the Gulf of Cadiz and off 
	Cape Sines. Differential penetration depths of oxygen likely are a 
	function of sedimentation rare and bottom water oxygen concentration. The 
	data will serve as estimators for environmental control on the depth 
	distribution of infaunal benthic foraminifera.

5.4.6	Trace Fossil Recording and Grab Sampling (P. Sch”fer, B. Bader)
a) Instrumentation and Sample Conservation

Sediment samples were taken from within and outside the drift sediments in the Gulf 
of Cadiz as well as from three primary areas along the western Iberian continental 
margin at water depths of 110 to 2170 m i.e., across the MOW flow path. At least 
one radiograph was taken from each giant box core. Following a standard technique 
developed at the GPI Kiel, a thin slab was taken from each box core using a 
plexiglas cover of 27 to 15 cm size and 1 cm thickness, then put into plastic bags, 
evacuated, sealed, and stored at 4ƒC. Radiograph sampling of gravity cores will be 
done onshore.

Additional sediment samples taken with Van Veen grab and giant box core were 
archived in plastic bags and liners and were stored in the shipboard reefer. 
Surplus sediment was washed on deck through a sieve to retain the coarse fraction 
>1mm. This was especially important, were the carbonate content was low due to 
strong terrigenous input (siliciclastic sediments of the Faro drift; glauconitic 
quartz sand apron between 200 and 500 m water depth along the Western Iberian 
continental margin). Living organisms were stored in 70% alcohol or 10 % formaline 
buffered with sea water.

b) Trace Fossil Assemblages

In general, all sediments show strong bioturbation that covers nearly the complete 
sediment column. Preservation/intensity of bioturbation, however, is poorest in the 
upper 5 cm of the sediment column ("Homogenous top layer" after WETZEL, 1981) and 
in sediments from shallow sites. A pronounced trace tiering was found in sediments 
from deep water sites. Both vertically and horizontally arranged feeding traces do 
occur. Burrows of crustaceans were observed in giant box cores as conical mounds of 
5cm height; they were commonly found at shallow sites in the Gulf of Cadiz. They 
occur as vertical burrows with uneven burrow lining in radiographs. A preliminary 
description of trace fossils is given in Table 12.

At first inspection, radiographs taken from box core material revealed trace taxa 
of Scolicia, Planolites, Teichichnus, Chondrites, Helminthopsis and Trichichnus. On 
shore radiographs from gravity cores taken during METEOR cruise M39/1 (and 
additional material will be collected during METEOR cruise M40/1 into the 
Mediterranean Sea) will be studied in detail. These analysis include a visual 
description of bioturbation phenomena in sediment cores, the analysis of trace 
morphology and of trace associations from radiographs, and finally computer 
tomographic scans and image processing of traces in order to better illuminate 
their three dimensional structure. Stratigraphic and sedimentary analysis will be 
done post-cruise in conjunction with stable isotope analyses.

Tab. 12: Trace Fossil Occurrence in the Gulf of Cadiz and at the Western Iberian 
Margin Sites

Sample		water depth	Onboard sediment/trace description	
M39002-2A	-1209m		Zoophycos, Scolicia, Chondrites trace tiering	
M39002-2B	-1209m		poor trace record			trace tiering
M39003-1A	-801m		Planolites, trace tiering	
M39003-1B	-801m		Teichichnus, Planolites			Zoophycos, trace tiering
M39004-1	-966m		Chondrites, ?Helminthopsis		Zoophycos, ?Planolites
M39005-3	-118m		poor trace record	
M39006-1	-214m		crab burrows	
M39009-1	-681m		Chondrites, ? Planolites		poor trace tiering
M39010-1	-878m		Sand layer overlying silt layer		poor trace record
M39016-1	-581m		poor trace record	
M39017-5A	-533m		poor trace record	
M39017-5B	-533m		poor trace record	
M39018-1	-496m		poor trace record	
M39019-2	-730m		?Teichichnus, ?Planolites		poor trace tiering
M39020-1	-726m		trace tiering	
M39021-5	-901m		Sand layer overlying silt layer		poor trace record
M39022-1	-668m		trace tiering	
M23023-2	-730m		?Planolites, ?Trichichnus		trace tiering
M39029-3	-1917m		Zoophycos, Planolites			trace tiering
M39036-1	-1747m		Trichichnus				trace tiering
M39037-3	-2532m		?Helminthopsis	
M39058-1	-1975m		Helminthopsis, Lophoctenium		Planolites
M39059-2	-1605m		Zoophycos	
M39061-1	-544m		poor trace record			trace tiering
M39070-1	-1220m		sand layer overlying silt layer		poor trace record
M39072-1A	-2170m		Scolicia, Zoophycos, Planolites		trace tiering
M39072-1B	-2170m		Scolicia, Zoophycos			trace tiering

c) Sediment Composition

A depth transect was sampled in the Gulf of Cadiz at water depths between 100 and 
800 m along which Van Veen grab, sediment dredge, giant box corer and gravity corer 
were deployed. The transect was chosen so as to span the depth range of MOW and 
water masses immediately above and below. The Faro Drift was an important target 
area in the Gulf of Cadiz (Figure 2).

At the southern Portuguese margin, a depth transect from 50 to 500 m water depth 
was sampled with the Van Veen grab and the sediment dredge. Further samples were 
taken with a Van Veen grab and dredge from the isolated pinnacles of the Principles 
de Avis as well as from the Tejo Plateau off Cap Finisterre, grab and dredge 
samples were taken from 50 to 80 m water depth. Off NW Galicia, a spur of the 
continental shelf elevating up to 400 m water depth was sampled with a Van Veen 
grab. Further sediment samples were taken with a giant box corer from deeper water 
locations.

Sediment dredge sampling revealed pebbles and solid rock fragments, lithified coral 
framework and some living macroorganisms such as corals, bryozoans, and echinoids. 
A large amount of ship slag occurred in sediments below the major ship route in the 
Gulf of Cadiz and around Cabo de S“o Vicente. It showed intensive overgrowth by 
epibenthic organisms such as hydrozoans, sponges, bryozoans, serpulids, 
polychaetes, bivalves, and sessile foraminifers. Most of the material was dried, 
only few slag pieces were stored in 70% alcohol.

Van Veen grab and giant box core samples were taken along a profile in the Gulf of 
Cadiz between 36ƒ03,0N/007ƒ13,8W and 36ƒ31,9N/006ƒ44,0W at water depths between 110 
to 850 m. Parasound profiles displayed a gentle topography and sediment 
accumulation is indicated by several parallel reflectors. Sediments typically 
consist of bioturbated siltic clay to clayish silt, partly with bivalve coquinas. 
Surface sediments typically consist of fine- to medium grained sand with abundant 
biogenic fragments (echinoid spines, gastropods, bivalves, corals and bryozoans). 
High abundances of endobenthic species indicates a high content of fine sediment 
fraction (i.e. compared to the carbonaceous lag deposits in high boreal to subpolar 
shelf settings; SCHŸFER et al., 1996; HENRICH et al., 1997).

The deepest sampling locations (M39013-1; M39014-1,2) are characterized by a rough 
topography on the Parasound/Hydrosweep profiles. The sediment dredge recovered 
solid rocks and pebbles of red, fossiliferous sandstone colonized by a diverse 
epifauna (hydrozoans, bryozoans, ascidians, serpulids, actinians). Coral fragments, 
sea-urchins (Cidaris cidaris) and gastropods also occurred.

Typical deep water coral reefs were not found but the considerable abundance of 
coral fragments in sample M39014-2 implies the nearby presence of reef-like coral 
structures. The coral fragments show strong alteration (corrosion, bioerosion, 
epigrowth) and cementation, that either suggest a fossil age of the fragments or 
unusually early cementation. The lack of fine grained sediment and the abundance of 
sessile epibenthic suspension feeders are indicative of strong bottom currents 
(MOW).

The Faro drift consists of sandy, silty, and muddy contourites. The clayish silt to 
fine sand of the contains mainly endobenthic bivalves, associated with large 
solitary corals (Flabellum sp.) and terebratulid brachiopods. Due to increasing 
sediment coarseness at sites closer to the coast, the robust Van Veen grab was used 
at several near-shore sites. Except for a narrow erosion belt, which is indicated 
by slightly greater water depth and coarser sediments, clayish silt occurred up to 
shallowest depths of 103 m.

Sediments on the flanks of the DÈcouvreur seamounts (M39030 to M39034) consist of 
silty fine to coarse sands that are enriched in pteropods, sponge spicules, and 
benthic and planktonic foraminifers. The tops of these seamounts are covered by 
blankets of coarse sand and fine gravel with high carbonate contents. This sediment 
includes a rich epibenthic fauna dominated by bryozoans, bivalves, and gastropods. 
Sediment distribution and facies types of the DÈcouvreur seamounts correspond to 
that on the Principes de Avis. However, samples from the latter revealed siliceous 
sponges and ophiuroids.

A depth transect off Sadao (M39047 - M39054) covers the upper shelf slope between 
500 and 100 m water depth and retrieved glauconitic medium to coarse sands with a 
high contents of small bivalves, gastropods, echinoid spines, benthic foraminifers, 
and skeletal debris. Sediments at depths shallower than 100 m are characterized by 
coarse sands with variable carbonate contents, and by well rounded pebbles 10-15 cm 
in diameter that were intensively encrusted by bryozoans, coralline red algae, and 
the foraminifer Minicea minima. An apron of glauconitic medium to coarse sand 
covering the outer shelf and uppermost slope that is found along the entire western 
Iberian continental margin was tracked up to the northernmost M39/1 sampling sites 
off Galicia.

The Tejo Plateau presumably is the most extended shelf area on the western Iberian 
margin where biogenic carbonate production and accumulation occurs between 50 and 
200 m water depth. Coarse sand and fine gravel with a high carbonate content was 
found on the Tejo Plateau in water depths of 160 m. The coarse fraction >2 mm is 
composed of bivalves, gastropods, erect bryozoans, skeletal fragments of 
cirripedians (Verruca stroemia), and serpulids. The fraction 1- 2 mm is dominated 
by branchy bryozoans, bivalve debris, and benthic foraminifers. Interestingly, at 
Tejo Plateau the epifauna dominates the endofauna in contrast to the Gulf of Cadiz 
and the glauconite sand apron along the Portuguese coast. The distribution of 
carbonate rich sediments apparently is linked to the delivery of terrigenous 
material. Off Tejo Plateau, on a topographically isolated submarine mound (132 m 
below the sea surface) angular pebbles and solid rocks up to 50 cm in diameter were 
collected that were intensively overgrown by Miniacea minima, a diverse encrusting 
bryozoan fauna, and serpulids.

Off Cabo Finisterre, sites between 500 and 200 m water depth revealed a glauconitic 
medium to coarse sand apron. Solid rocks in water depths of 50 to 70 m were 
colonized by large bryozoans and corals. Solid rocks seem to be the preferred 
habitat for the epibenthic fauna, whereas endofaunal elements are present in 
glauconitic sand aprons and drift sediments.

Along the northern margin of Galicia, the shelf is bordered by a fracture zone 
forming a very steep topographic relief cascading into the deep Gulf of Biscaya. 
Glauconitic sands, poor in carbonate were found up to the northernmost position. 
Framed by steep walls, solid rock is exposed in 500 m water depth. Pebbles and rock 
boulders collected with a dredge show intensive overgrowth by sponges, bryozoans, 
serpulids, and benthic foraminifers. Post-cruise studies include sediment component 
analysis including carbonate and organic carbon contents, radiocarbon datings of 
carbonate skeletons, (paleo-) ecological analysis of dominant organisms, taphonomic 
analysis of carbonate skeletons (bioerosion, mechanical destruction, transport 
processes), characterization of areas of carbonate production and accumulation, and 
carbonate budget, terrigenous component analysis (reconstruction of sediment origin 
and transport patterns), and analysis of microorganisms: benthic and planktonic 
foraminifers, diatoms, and ostracods.

5.4.7	Geochemistry and Mineralogy (G. Bozzano, I. Cacho)

From all opened cores samples were taken shipboard for various sedimentological and 
geochemical analysis. Surface samples will be used to study clay mineralogy and 
some cores will be selected for studying the complete mineralogical record. 
Additionally, three gravity cores (M39002-6, M39004-5, M39029-7) were wide spaced 
sampled (every 50 cm) onboard for a prospective molecular biomarker study. A total 
of 32 samples was collected by a 2.5 ml syringe (1 cm), stored in glass vials and 
immediately frozen. These samples will be processed post- cruise to determine the 
quality of the samples for molecular biomarker analysis. According to these results 
one core will be selected for a high resolution study (every 2 cm). The analysis 
will focus on a series of molecular biomarkers originated by marine and terrestrial 
organisms: C29 n- alkane, C26 n-alkan-1-ol, phytol and long chain di and tri-
insaturated alkenones (37 and 38 carbons). These compounds are present in most 
marine sediments and, after a lipid extraction, they can be clearly identified and 
quantified by gas-chromatography. Their abundance records serve as proxies either 
for marine paleoproductivity (Phytol and long chain alkenones) or for terrestrial 
input (C29 n-alkane and C26 n-alkan-1-ol). Furthermore, these compounds enable a 
reconstruction of the past sea surface temperature (Uk 37 unsaturation index).

5.4.8	High-Resolution Acoustic Mapping and Core Logging: Paleoceanographic 
Application (K. Heilemann, F.-J. Hollender, T. Karp)
a) Instrumentation

Parasound and Hydrosweep profiling during M39/1 concentrated on sediment drifts in 
the northern part of the Gulf of Cadiz and were carried out as part of the STEAM 
MAST Project. R/V METEOR's Parasound echo-sounder applies two simultaneous primary 
frequencies (a fixed frequency of 18 kHz and a variable frequency of 18 to 23.5 
kHz). Due to a Parametric Effect in water, a secondary frequency is produced (2.5 
to 5.5 kHz). In ocean sediments a penetration of up to 100 m can be reached. 
Onboard, paper plots were used for prospective studies, digital data were stored on 
magnetic tape for post-cruise processing. The Hydrosweep system, a multibeam echo 
sounder system operates at a frequency of 50 kHz. The combined use of Parasound and 
Hydrosweep allows a three-dimensional imaging of superficial acoustic units.

Sediment cores were logged using a GEOTEK Multi Sensor Core Logger (MSCL; P. 
SCHULTHEISS, GEOTEK, Surrey, UK) that provides continuous, high resolution and non-
destructive measurements of physical properties that are used for stratigraphic 
correlation and lithologic interpretation. The MSCL used during M39/1 consisted of 
a p-wave logger (PWL; determination of compressional wave velocity), a gamma ray 
source (137Cs and detector; estimation of sediment density), and a Bartington 
magnetic susceptibility meter. The system is fully computer-driven. Whole-round 
core sections were placed on a core boat and transported by a stepper motor through 
the tracking system for a high resolution measurement (2 cm) of physical 
properties. Data files are stored in ASCII format.

The p-wave-logger consists of two transducers, which send and receive a 500 kHz 
ultra-sound signal through the core at a rate of 1 kHz. The travel time of the 
signal and the diameter of the sediment core are used to calculate p-wave velocity 
in the sediment. The true diameter of the core liner is monitored for each 
measurement by an electronic caliper. A detailed discussion of MSCL application is 
given in SCHULTHEISS and MIENERT (1988) and SCHULTHEISS and MCPHAIL (1989).

The Gamma Ray Attenuation Porosity Evaluation (GRAPE) measurements are based on the 
attenuation of gamma rays in marine sediments by Compton scattering (BOYCE 1976). 
The attenuation of gamma rays through the core is referred to the attenuation of 
aluminum standards. For calibration, two pieces of a PVC liner and 20 aluminum 
plates (5.3 mm thick) were each placed between the source and the detector. The 
expected theoretical attenuation can be calculated from the density data (about 2,7 
g/ccm), the thickness of the aluminum plates and the count-rate measurement of 
gamma rays. During the measurement, a gamma ray beam of 0.662 MeV is emitted out 
from a hole (f6 mm) and passes through the core. The 137Cs-source is shielded by a 
lead case. A scintillation detector (NaJ-crystal) measures the diminished 
radiation, which represents an indicator for wet bulk density. The physical 
principle of the Magnetic susceptibility meter is based on the magnetizability of 
atomic magnetic moments by external magnetic fields. A sensor loop with a diameter 
of 168 mm produces a weak, magnetic field. Interference with magnetic sediment 
particles induces changes of the oscillation frequency of the electric circuit. 
These variations are detected and transformed into the magnetic susceptibility 
values that are given in SI-units. A detailed description of the GEOTEK Multi 
Sensor Core Logger and its use in sediment logging is given by CHI (1995).

Approximately 100 m of sediment cores were logged on board during M39/1. Prior to 
the measurement all cores were stored horizontally for 12 hours for thermal 
equilibration. During the cruise (sediment) temperatures varied between 16,6 and 
21,2ƒC. Core liners were wetted with distilled water to ensure optimum acoustic 
coupling between the p-wave transducers and sediment cores. The drift of the 
susceptibility sensor was checked by measuring an iron ring that has a defined 
susceptibility signal.

Changes in acoustic and physical properties of marine sediments are closely related 
to the mean grain-size, bulk density, porosity, terrigenous material and percentage 
of sand, silt and clay. The p-wave velocity varies between 1450 m/s and 1500 m/s. 
In sections with a high amount of sandy components, the p-wave velocity increases 
up to 1600 m/s. Unrealistic high or low velocities (below 1450 or above 1600) were 
measured when coupling between p-wave transducer and the sediment was insufficient. 
In an ideal case there are no air-gaps between the liner and the sediment. But in 
practice the sediment does not fill the liner completely, having gaps mostly at the 
beginning and the end of a section. In this case the 500 kHz transducer signal is 
significantly weakened. Sediment gaps in the liners also distort the GRAPE 
measurements. For a satisfactory interpretation it would be necessary to correlate 
the p-wave velocity with the density data. In sections with a good correlation 
between compression-wave velocity and density, the physical properties can be used 
for interpretation of sedimentary processes. The density of marine sediments range 
between 1.45 and 1.9 g/ccm in the Gulf of Cadiz and at the Portuguese margin and, 
as expected, increases from top to bottom of these cores. Density variations on top 
of these general trend indicate changes of the mineralogical composition or of the 
water content. The magnetic susceptibility depends on the flux of terrigenous 
magnetic minerals. Generally susceptibility values are about 20 SI-units. In 
several cores prominent peaks up to 50 occur. Most magnetic susceptibility curves 
show a positive correlation with the curves of the p-wave-velocity and GRAPE-
density.

b) PARASOUND and HYDROSWEEP Profiling in the Gulf of Cadiz

Due to good weather conditions and locally deep penetration high quality PARASOUND 
and HYDROSWEEP records from the Gulf of Cadiz were gained (Cadiz 4, Cadiz 5, Faro 
1, Santa Maria 1, Santa Maria 2, Albufeira 1, Albufeira 2; Figure 55). Profile 
Cadiz 4 covers water depths from 700 m to 1100 m. Several pock marks were observed. 
These marks most frequently were V-shaped, either with or without levees (Figure 
56). Vertically, they measure several meters, in cross sections up to one 
kilometer. The topography of the whole area is extremely rough. Profile Cadiz 5 
covers 650 m to 1000 m water depths. The topography at the southern end of the 
survey box is extremely rough. This area is influenced by the tectonically active 
Gibraltar Fracture Zone. The other parts of the profile box has a smooth 
topography. The thickness of the stratified sequences in the smooth areas reaches 
up to 30 m and shows up to 12 reflectors. In the rough parts the penetration 
reaches up to 5 m, usually without subbottom reflectors.

Drift sediments in the northern Gulf of Cadiz were surveyed in three profiles. 
Profile Faro 1 covers the Faro Drift (Figure 57). The water depths ranges from 550 
m in the North up to 800 m in the south and the profile lines were run N-S. The 
three-dimensional HYDROSWEEP Map shows the luv and the lee flanks of the sediment 
drift body. The penetration in the middle part of Faro drift body reaches up to 20 
m, at the distal ends it is lower. The lines of Profile Santa Maria 1 and Santa 
Maria 2 were N-S oriented and show the sediment drift body east of profile Faro 1. 
The water depths ranged from 375 m in the north up to 950 in the south. At the 
northern end of the sediment drift body a channel like structure followed by a 
steep ascent occurred. The penetration in the middle part of the sediment drift 
body reaches up to 20 m, at both ends it is about 10 m. Profile Albufeira shows the 
east part of the sediment drift body in the Gulf of Cadiz. The lines of Profile 
Albufeira have a S-N orientation. The water depth decreases from about 350 m in the 
North to about 1000 m in the south. The penetration in the middle part of the 
sediment drift body reaches up to 25 m, at the distal ends about 10 m. At the 
northern end of the sediment drift body the channel structure of profiles S. Maria 
1-2 reappeared. The sediment thickness of the drift body increase from E to W 
(profile Faro 1 to profile Albufeira).

Fig. 55:Location of acoustic survey boxes Cadiz 4, Cadiz 5, Faro 1, Santa Maria 
	1, Santa Maria 2 and Albufeira.

Fig. 56:Three dimensional HYDROSWEEP profile Cadiz 4. Water depths range from 760 
	m to 1140 m. Pock marks measure several meters in vertical direction and 
	several hundreds of meters up to one kilometer in diameter.

Fig. 57a:Three dimensional HYDROSWEEP profile Faro1. Shown are the luv and lee 
	flanks of the sediment drift. Water depths range from 700 m to 1100 m.

Fig. 57b:Stratified sequence of the luv and lee flank of a PARASOUND profile of 
	the Faro Drift. Location: 36ƒ53'N, 7ƒ37'W/36ƒ43'N, 7ƒ37'W. Water depths 
	range from 528 m in the north to 588 m in the south.

c) Core Logs as Indicators of Climate Change (S. Jung, R. Zahn)

Organic and inorganic composition as well as physical properties of deep sea 
sediments are controlled the ocean's physical circulation and chemical cycling. 
Carbonate dissolution, for instance, is driven by the state of carbonate saturation 
of ambient water masses which, in turn, is a function of carbon input and of 
chemical water mass "aging". Continuous high-resolution core logging is an 
indispensable tool for the evaluation of sediment composition and provides valuable 
data of fine-scale changes of sediment parameters that are intimately tied to state 
of ocean circulation and, ultimately, of global climate. Magnetic susceptibility 
logs and color scans of M39/1 sediment cores show numerous anomalies that can be 
correlated e.g., with horizons of enhanced concentration of terrigenous sediment 
components. Such horizons have been found previously in the northern North Atlantic 
and at the upper Portuguese margin and have been linked to periods of enhanced 
iceberg melting during the last glacial period (BOND et al., 1993; LEBREIRO et al., 
1996; ZAHN et al., 1997). Figure 58 gives an example of the core logs that have 
been obtained during M39/1. The color scans show a series of positive reflectance 
excursions that can be tentatively correlated to oxygen isotope anomalies in the 
GISP2 Greenland ice core record. The isotope anomalies signify short-lived warm 
(interstadial) episodes that are well know from continental European paleoclimate 
data bases and point to rapid climatic oscillations in the North Atlantic region 
(DANSGAARD et al., 1993; GROOTES et al., 1993; TAYLOR et al., 1993).

Fig. 58:Shipboard color reflectance and magnetic susceptibility logs for core 
	M39037-1 from the western Iberian margin at 2533 m water depth (top). 
	Arrows mark depth positions in the sediment core of 'Heinrich' meltwater 
	events (labelled H1-H5) as predicted from reflectance minima and/or 
	susceptibilty maxima. YD=Younger Dryas cold event. The Greenland GISP2 ice 
	core oxygen isotope record is shown for reference of northern North 
	Atlantic climate variability (bottom). Prospective correlation between the 
	GISP2 record and the M39037-1 color reflectance log is indicated and 
	implies a close link between sediment property variations at the western 
	Iberian margin and northern North Atlantic climate. Age scale along the 
	ice core record is in 1000 years before present.

The apparent correlation between the color scan of core M39037-1 and the Greenland 
ice core record implies that the climate oscillations reached the western Iberian 
margin and conceivably affected climates of the western Mediterranean region. 
Planktonic isotope records that monitor surface ocean conditions will be generated 
for this core at the same resolution as the color scans i.e., at an average sample 
interval of 2 cm. This high-resolution isotope record will allow to test the 
predicted correlation with the ice core record as indicated in Figure 58. It will 
also allow to estimate the magnitude of environmental change at the western Iberian 
margin, far south of Greenland but reasonably close to the glacial position of the 
North Atlantic polar front at approximately 40ƒN. Statistical analysis of the 
planktonic foraminiferal assemblage will allow to estimate the variability of 
regional surface water temperature. The combined faunal and isotope data sets will 
help to better constrain the paleoceanographic patterns off Portugal and to 
determine the role of the Portugal current in transmitting northern North Atlantic 
climate signals as far south as Cape Blanc at 21ƒN off northwest Africa (WANG et 
al., 1995).

6	SHIP'S METEOROLOGICAL STATION
6.1	Meteorological conditions during leg M39/1 (K. Flechsenhar)

RV METEOR left Las Palmas harbor on April 18th 1997 and sailed to her first working 
area in the Gulf of Cadiz, where they arrived in the evening of April 20th. During 
this track the weather was influenced by a low centered west of Portugal, which 
caused northwesterly winds of 6 to 7 Bft on April 20th and 21st, and swells of 
about 3.5 m height. On April 22nd wind and seas decreased and from April 23rd to 
May 1st the scientific program was carried out under optimum conditions. On April 
30th however RV METEOR for a while got into dense fog at 36.0ƒN8ƒ20'W. On May 1st 
the ship passed Cabo de S“o Vicente with Westsouth-west Gale 7 to 8 Bft, and wave 
heights of about 3 m. This wind was primarily caused by a low approaching from the 
west, but its intensity was strengthened by the orographic effect of the steep 
cape. On May 2nd and 3rd the station works continued under fair weather off SW 
Portugal, but a westerly 3 m high swell caused some rolling and pitching of the 
ship. On May 4th, RV METEOR proceeded to the North an passed Cape Roca, height of 
swell now about 4 m. From May 5th on the weather was dominated by a low pressure 
system with center near Scotland and became rather bad. A strong southwesterly to 
northwesterly wind (6 to 7 Bft) made the sea very rough. During passages of cold 
fronts even Northwest gale 8 with gusts up to 10 occurred and the scientific was 
carried out under difficult conditions.

In the evening of May 7th RV METEOR passed Cape Finisterre with northwesterly winds 
of 5 to 6 Bft and swells of about 5 m. Until May 10th off Cape Finisterre, the Wind 
decreased to Bft 5, but a 5 m high swell, rolling on continuously from the North 
Atlantic Ocean, hampered station works. On May 10th all research operations were 
terminated and the ship headed towards Brest across the Bay of Biscay, wind 
Southwest to West 4 to 6 Bft, swell about 4 m. In the morning of May 12th RV METEOR 
moored in Brest.

Twice a day a weather report was compiled and published in the morning and in the 
evening. Additional comments were regularly given to the ship's command, the chief 
scientist and upon request. The necessary data and weather maps were received from 
the wireless stations Bracknell and Pinneberg, as satellite pictures (satellites 
METEOSAT and NOAA), and by fax (forecast charts from Bracknell or Offenbach). The 
forecasts of weather conditions and height of sea and swell were based essentially 
on surface analysis charts of the North Atlantic Ocean of 00.00 and 12.00 UTC every 
day. Surface observations of land stations and voluntary observing merchant ships 
were compiled by hand and analyzed by hand.

Meteorological parameters have been measured and recorded continuously and were 
transferred to the ship's data collecting system. Sensors and meteorological 
equipment were maintained regularly, some repairs were done. Every day at 0 and 12 
UTC a rawin sonde was launched with the ASAP-System, determining a vertical profile 
of pressure, temperature, moisture and horizontal wind up to an altitude of 20 to 
25 km. The evaluated data (temps) were transmitted into the GTS of the WMO. Every 
hour a World Meteorological Organization (WMO) standard weather observation was 
practiced. 8 of them were transmitted into the WMO Global Telecommunicating System 
(GTS) including eye observations done by meteorological staff.

6.2	Meteorological conditions during leg M39/2 (B. Brandt)

METEOR left Brest on May 15, 1997. After intense discussion of the weather 
development over the next five days it was decided to go Northwest and to travel 
the course of METEOR cruise M39/2 in the originally intended counterclockwise 
direction.

The weather during the first week of the cruise was determined by high pressure 
over the Norwegian Sea and depressions moving from Newfoundland to the Bay of 
Biscay. Mostly moderate easterly winds were prevailing, bringing favourable 
conditions for the first cross section across the Iceland Basin to the Mid Atlantic 
Ridge. Only on May 20 easterly gales prevented an intended mooring which had to be 
postponed for one day.

On May 23 the high pressure centre began to move southward to the British Isles, 
and depressions now moving northwards from Newfoundland to Greenland caused 
prevailing winds to veer from East to South. This southerly air current was 
frequently accompanied by fog. On May 28 and 30 two fast moving storm depressions 
caused southerly gales and consequently a mooring had to be delayed until May 31 
(Figure 59).

The first days of June were determined by moderate to strong northerly and later 
easterly winds between high pressure near Iceland and a stationary low north of the 
Azores. On June 5 METEOR got under the influence of a depression originating from 
Labrador, intensifying east of Newfoundland, and later moving east. But due to the 
rapid disappearance of the Icelandic anticyclone winds were only light to moderate 
from northeasterly directions. During the last two days of the final leg of the 
cruise the ship was lucky to stay near the centre of the depression with mostly 
moderate northeasterly winds. METEOR put in at Cork on June 8, 1997.

6.3	Meteorological conditions during leg M39/3 (B. Brandt)

After leaving Cork harbour on June 11, 1997, RV METEOR passed the rear side of a 
depression moving northeast across the Irish Sea with northwesterly winds up to 7 
Bft. Between June 13 and 16 two weakening depressions moving from the Labrador Sea 
to the Bay of Biscay brought winds of 6 Bft at the most from different directions, 
but heavy shower activity.

Fig. 59:Observations of wind and air pressure during Leg M39/2.

On June 17 a steady westerly air stream with sometimes high swell built up between 
the intensifying Azores anticyclone and a storm depression moving from Cape 
Farewell to the Hebrides. Westerly to northwesterly winds were mostly moderate to 
strong, only reaching 8 Bft on June 19. Thus conditions for the first mooring 
station on June 21 were rather favourable.

After passing 30ƒ W METEOR reached the western slope of the Azores anticyclone with 
winds backing southwest and the air becoming warm and moist. With winds being 
southwesterly to southerly 6 Bft conditions were again favourable for the second 
mooring on June 23. On June 24 and 25 southerly winds were increasing to 7 Bft due 
to depressions connected with a 500mb trough stretching South from Newfoundland. 
Fog or drizzle was almost continuous.

With METEOR proceeding West and passing the trough line the air became clear on 
June 26 with light northwesterly winds increasing to 7 Bft on June 27. The final 
days of the cruise were determined by an almost stationary and weakening depression 
South of Newfoundland in the centre of which METEOR experienced light to moderate 
winds from variable and later north- easterly directions, accompanied by fog 
patches and later by widespread fog. METEOR docked in St. John's on July 2, 1997.

6.4	Meteorological conditions during leg M39/4 (G. Kahl)

When METEOR sailed from Saint John's, Nfld, on July 6, 1997, a trough trailing 
behind an occluded front had passed that city in the early morning hours. Moderate 
to strong westerly winds were blowing as the low of 1000 hPa slowly drifted 
southeast-wards from the Labrador coast and the ship went northward. Meanwhile, a 
high of 1020 hPa had formed over North Quebec, extending into the Labrador Sea by 
July 9, so that winds were light. However, a new low 1010 hPa had slowly formed 
over the New England States and moved northeast, reaching North Quebec with a 
central pressure of 1005 hPa on July 11. During these days the research vessel 
still enjoyed the presence of a wedge of high pressure 1020 hPa that extended 
northward from the high now 1030 hPa centeres midway between Newfoundland and the 
Azores. The low, now of 1000 hPa moved to the south of Greenland on July 13 while 
moderate winds from easterly directions veering to westerlies later were 
experienced by METEOR returning from the vicinity of Southwestern Greenland by 
then. In the meantime, an area of low pressure west of Hudson Bay had elongated to 
the Gulf of St. Lawrence and had formed a low of 1000 hPa over the Strait of Belle 
Isle. Upon reaching open waters this low intensified to a complex gale 990 hPa east 
of Belle Isle and southeast of Cape Race. The METEOR approached her stopover 
destination St. Anthony from the north to northeast, thereby experiencing strong 
northeasterly winds but avoiding gales. During stopover time the following wedge of 
high pressure closed in to eliminate what little amount of clouds had been left 
over St. Anthony by the passage of the gale center. When METEOR put out to the 
Labrador Sea again another gale center had developed west of Hudson Bay and had 
moved to North Quebec, minimum central pressure being 990 hPa on July 17. Whereas 
central pressure filled somewhat, the area of strong southeasterlies extended out 
to the ships working area, easterly and southeasterly winds of 6 and 7 Bft being 
observed from July 18 to 20. Cyclonic activity on Canada's Eastern Seaboard did not 
cease after that date, but the ship was lucky to be in the center of the low of 
1000 hPa during July 21 to 22 when the low eventually filled and moved away 
northeastward. Light northwesterly winds gave way to light and variable conditions, 
and when METEOR visited Cape Farvel on July 25, it was calm for a few hours. The 
research vessel then headed south while a developing gale center made its way from 
the Grand Banks to the Irminger Sea, intensifying to 990 hPa while on its way. 
Another gale center was following closely, reaching a central pressure of unter 990 
hPa on July 28, too, on a position midway between Iceland and the Azores. METEOR 
was influenced only by moderate to strong northwesterly winds up to July 28. The 
gale center south of Iceland further developed into a storm center 975 hPa on July 
29, the ship benefiting but shortly from the area of high pressure building to the 
southwest of the storm center which slowly filled thereafter. The research ship was 
influenced by a gale center that had developed over the region of the Great Lakes 
during July 26, being hardly discernible by that date but having reached a central 
pressure of under 990 hPa over North Quebec by July 28. The gale center then moved 
on to Southwestern Greenland, making its landfall with a central pressure of 980 
hPa on July 30 just when METEOR visited the northern part of Flemish Cap. 
Southwesterly gales of 8 Bft were observed for several hours. These abated to 
moderate Southwesterlies when the ship headed east to reach 35 West by August 2. 
Another gale center 995 hPa had reached the Labrador coast and had moved quickly to 
southeastern Greenland, meanwhile further deepening by 5 hPa. The METEOR then 
headed north, Southwesterlies becoming strong almost immediately, lows crossing the 
North Atlantic quickly, developing into strong gale centers by the time they 
reached the vicinity of either Greenland or Iceland. After all, the Greenlandic 
Inland Ice Sheet and the East Greenland Current are a principal source of cold air 
masses in summer. West of Baffin Bay, a gale center 990 with a large diameter had 
developed. While it deepened further to 985 hPa, a secondary gale center 995 hPa 
developed over the northern part of Hudson Bay. This gale center, having 
intensified to 985 hPa, passed Hudson Strait during August 7 and moved east to 
southeast later to be centered west of Ireland when METEOR finished her cruise. The 
ship had made her way to Southeastern Greenland through strong westerlies caused by 
a low 1000 hPa there during August 6 and 7, then winds were light while they backed 
to east during the afternoon of August 8, and during the last days of her cruise 
the ship had to make her way to Reykjavik against strong easterlies.

6.5	Meteorological conditions during leg M39/5 (G. Kahl)

When METEOR left Reykjavik on schedule in the morning of 14.08.97, there were light 
southeasterly winds accompanying her out to sea. These resulted from a central low 
1000 centered at 56 North 28 West. The Azores High 1027 was to be found just east 
of that archipelago. A secondary low 1005 which had originated somewhere along the 
U.S. east coast a few days earlier had made its way to the region east of Cape 
Race. However, winds backed to the northeast and were up to 6 Bft by 16.08. because 
the secondary low had become the major low of the northeastern North Atlantic by 
intensifying to 990 and moving up to the south coast of Iceland, the former central 
low now being relegated to a mere extension of the new gale center. A new low 1005 
had passed Cape Race to lie northwest of the Azores, and another development was 
taking place over Nova Scotia.

Still another development had taken place during these few days. A low at the 
Labrador coast had moved up to the central part of the west Greenland coast and 
then it had been veering at the Polar Cirkel, eventually going southeast over the 
ice clad interior. A secondary low 1000 formed over The Irminger Sea, and this kept 
the METEOR from experiencing more than 5 Bft up to the 20.08. By then, the gale 
center south of Iceland had moved on to the Norwegian Sea and eventually to the 
Fram Strait, and the next low waiting in line had moved up from Newfoundland to 60 
North 25 West, thereby deepening to 985.

Conditions deteriorated somewhat on 21.08. when central pressure in the gale center 
fell below 980 before it crossed Iceland on its way northward and began to fill. 
Northwesterly winds of 7 Bft were experienced for a few hours now but when the 
vessel approached the Greenland coast winds abated again to light northerly winds. 
For some time even the state of "light and variable" was reached, this being 
appreciated by scientific as well as ship's crew. At nightfall on 25.08. when 
Greenland was left behind winds were still light and visibility was of an order 
that is seldom observed in more southerly latitudes.

While the research vessel was on her way to the southeast, one of the lows 
migrating over the Atlantic at 40 to 45 North had slowed and intensified to a gale 
center 975 at northwestern Ireland on 27.08. This, too, moved on the Norwegian Sea 
and the Fram Strait so that METEOR was not bothered, the observed winds being 
northwesterlies about 4. During 31.08. a flat low that had moved from Labrador to 
our working area had seen some intensification to a central pressure of 1000 
because of the cold air flowing out of the gale center passing Jan Mayen by then 
passed north of our position so that westerly winds of 6 Bft were observed, veering 
northwest and abating 4 Bft by the next day. Winds were up West 7 Bft by 03.09. to 
04.09. because of a cold front originating from the last mentioned low having 
deepened to a gale center of 980.

On the whole, the General Circulation over the North Atlantic was weak as it should 
be according to the time of year, but some prominent features of the synoptic 
charts may be figured out:

1. Lows moving along the U.S. coast, passing the Azores and then going up to the 
   Norwegian Sea,
2. Lows originating west of Hudson Bay, intensifying over North-Quebec to gale 
   center strength and then moving east,
3. A few special developments like the low going up the western Greenland coast and 
   then not continuing to Baffin Bay but choosing to go over the Inland Ice,
4. A quasi-permanent high over the region of the Great Lakes and Hudson Bay, and
5. The Azores High becoming a major feature of the synoptic Chart only during the 
   latter part of the voyage.

Intensity of all Developments has risen during the time the voyage took. During the 
03.09. the Azores High once again introduced itself to the synoptic chart at 48 
North 40 West with a strength of 1025. By 07.09. this was up to 1040 at 50 North 22 
West. Thereafter, it weakened but slowly and moved northeast, swinging east by 
10.09. and visiting Germany one day later. The METEOR was near the core of the 
anticyclone, so that winds were light and variable during the last few days of 
probing the ocean. In other regions, however, intense gale centers reigned, the 
Norwegian Sea being especially hard hit by a low that became almost a storm center 
975 during 09.09., our research vessel being lucky to be left unmolested at least 
as far as the English Channel. Hamburg was reached by 14.09.1997. Some weather 
statistics of this leg are shown in Fig. 60.

Fig. 60:Weather statistics during M39/5 for a) Wave statistics in meter steps and 
	b) Wind statistics in Beauford scale.

7	LISTS
7.1	Leg M39/1
7.1.1	Locations for sediment and plankton/water samples

GEOMAR	  METEOR  DATE		DEVICE	TIME	LATITUDE   LONGITUDE	WATER	RECOVERY   REMARKS
NO.	  NO.				(UTC)	(N)	   (W)		DEPTH(m)   (m)
M39001-1  121	  20.04.1997	ROS/CTD	16:17	36ƒ02.608  7ƒ45.572	1145		   Pinger at 30m,12/12 1156,1119,988,946,921,845, 797,677,576, 345,147,10
M39001-2  121	  20.04.1997	GoFlo	18:53	36ƒ02.491  7ƒ45.606	1132		   Water samples at:607,710,830,878,954,974,1022, 1052,1089, a test
M39001-3  121	  20.04.1997	PN	18:30				1131
M39001-4  121	  20.04.1997	CTD	19:53	36ƒ02.3	   7ƒ45.7	1131		   CTD-Test
M39002-1  122	  21.04.1997	BC	07:15	36ƒ01.7	   7ƒ46.6	1208		   Box washed out
M39002-2  122	  21.04.1997	BC	08:12	36ƒ01.7	   7ƒ46.5	1209	0.49
M39002-3  122	  21.04.1997	MUC	09:28	36ƒ1.6	   7ƒ46.5	1205	0.38	   1 tube empty
M39002-4  122	  21.04.1997	PN	09:22
M39002-5  122	  21.04.1997	GC6	12:42	36ƒ1.7	   7ƒ46.4	1205	4.7
M39002-6  122	  21.04.1997	GC12	12:05	36ƒ1.6	   7ƒ46.4	1212	5.82
M39002-7  122	  21.04.1997	GoFlo	12:52	36ƒ01.712  7ƒ47.086	1214		   Water samples at:231,452,500/F(S),601,774,811(S)
M39003-1  123	  22.04.1997	BC	17:01	36ƒ06.7	   7ƒ13.4	802	0.42
M39003-2  123	  22.04.1997	MUC	17:48	36ƒ6.6	   7ƒ13.4	801	0.36-0.40
M39003-3  123	  22.04.1997	GC6	18:33	36ƒ6.7	   7ƒ13.3	800	3.52
M39003-4  123	  22.04.1997	PN	17:15
M39003-5  123	  22.04.1997	GC12	19:26	36ƒ6.6	   7ƒ13.3	798	0	   Core bent
M39003-6  123	  22.04.1997	ROS/CTD	20:41	36ƒ6.8	   7ƒ14.1	803		   Pinger at 30m,12/12 804,777,6,642,502, 401,5,303,1, 277,7,211,154,103,5,53,6,12,3
M39003-7  123	  22.04.1997	GoFlo	22:26	36ƒ6.6	   7ƒ14.0	824		   Water samples at:79,181,330,429,524,664,784 (S)
M39004-1  124	  23.04.1997	BC	21:01	36ƒ14.2	   7ƒ43.9	966	0.46
M39004-2  124	  23.04.1997	MUC	21:53	36ƒ14.2	   7ƒ43.8	968	0.40-0.44
M39004-3  124	  23.04.1997	GC6	22:49	36ƒ14.3	   7ƒ43.8	968	5.75
M39004-4  124	  23.04.1997	GC12	23:52	36ƒ14.2	   7ƒ43.9	968	0	   Tube lost
M39004-5  124	  24.04.1997	GC12	01:22	36ƒ14.2	   7ƒ43.8	968	6.17
M39005-1  125	  24.04.1997	Grab	07:55	36ƒ32.0	   6ƒ44.0	119	0.2-0.3	   dark, olive-greyish silty fine sand
M39005-2  125	  24.04.1997	BC	08:33	36ƒ32.1	   6ƒ44.1	118.3	0	   not triggered
M39005-3  125	  24.04.1997	BC	08:48	36ƒ32.2	   6ƒ44.1	118	0.34
M39006-1  126	  24.04.1997	BC	09:45	36ƒ30.7	   6ƒ46.4	214	0.34
M39006-2  126	  24.04.1997	PN	09:40
M39007-1  127	  24.04.1997	Grab	11:17	36ƒ37.2	   6ƒ54.8	467		   Fine sand with abundant quartz and carbonate
M39007-2  128	  24.04.1997	Grab	13:02	36ƒ22.9	   7ƒ04.5	578		   Clayish Silt with planktic Foraminifera
M39007-3  128	  24.04.1997	GC6	13:33	36ƒ23.0	   7ƒ04.4	579
M39007-4  128	  24.04.1997	GC8.5	14:30	36ƒ22.8	   7ƒ04.3	577	5.77
M39007-5  128	  24.04.1997	BC	15:27	36ƒ22.7	   7ƒ04.2	577	0.32
M39008-5  129	  24.04.1997	PN
M39009-1  130	  24.04.1997	BC	16:42	36ƒ21.0	   7ƒ08.5	681	0.36	   BC
M39010-1  130	  24.04.1997	Grab	18:05	36ƒ19.3	   7ƒ12.4	878		   Sandstone with attached Hydrozoeas,Ascidiae, Bryozoas,Poriferas,Serpulidae,juvenile Pectinidae
M39010-2  131	  24.04.1997	Grab	18:48	36ƒ19.3	   7ƒ12.4	882		   coarse sand with biogenic debris
M39011-1  132	  24.04.1997	Grab	20:05	36ƒ19.3	   7ƒ12.9	846		   coarse sand w/ lithoclastic & biogenic material
M39012-1  133	  24.04.1997	Grab	21:13	36ƒ14.7	   7ƒ13.1	873		   coarse sand w/ lithoclastic & biogenic material
M39013-1  134	  24.04.1997	Dredge	22:28-	36ƒ19.2-   7ƒ12.4-	871		   boulder with sessile epifauna,seaurchin
					22:59	36ƒ19.2	   7ƒ12.7
M39014-1  134	  25.04.1997	Dredge	0:21-	36ƒ16.3-   7ƒ12.9-	850		   boulder with sessile epifauna,seaurchin
					0:50	36ƒ16.5	   7ƒ13.4
M39014-2  134	  25.04.1997	Dredge	1:52-	36ƒ16.2-   7ƒ12.8-	847		   sandstone pebbles,corals,compacted sand with biogenics
					2:25	36ƒ16.3	   7ƒ13.3
M39015-1  135	  25.04.1997	ROS/CTD	05:14	36ƒ14.240  7ƒ43.832	970		   Pinger at 30m,12/12 373,856,792,704,622.3, 532,448.5,374,203,117,64.3,10.6
M39015-2  135	  25.04.1997	GoFlo	07:22	36ƒ14.2	   7ƒ43.8	967		   Water samples at: 64,374,622,702,792,856, 938(S)
M39015-3  135	  25.04.1997	GC12	09:59	36ƒ14.2	   7ƒ43.8	967	3.37
M39016-1  136	  26.04.1997	BC	14:54	36ƒ46.7	   7ƒ42.2	581	0.33
M39016-2  136	  26.04.1997	MUC	15:37	36ƒ46.7	   7ƒ42.1	581	0.20-0.22  4 empty liners
M39016-3  136	  26.04.1997	GC6	16:08	36ƒ46.7	   7ƒ42.2	581	2.44
M39017-1  137	  26.04.1997	ROS/CTD	20:54	36ƒ39.0	   7ƒ24.7	527		   Pinger at 30m,12/12 529,511,487.5,462,410,380.6, 302,202,138.6,100.7,60.6,10.6
M39017-2  137	  26.04.1997	GoFlo	22:18	36ƒ39.0	   7ƒ24.5	533		   Water samples at:204,304,383,412,464,490,507
M39017-3  137	  26.04.1997	GC6	23:00	36ƒ39.0	   7ƒ24.5	533	4.1
M39017-4  137	  26.04.1997	MUC	23:42	36ƒ38.9	   7ƒ24.6	532	0.18-0.21  5 empty liners
M39017-5  137	  26.04.1997	BC	00:24	36ƒ39.0	   7ƒ24.6	533	0.27
M39017-6  137	  26.04.1997	PN	23:32
M39018-1  138	  27.04.1997	BC	02:06	36ƒ45.2	   7ƒ15.1	496	0.32
M39018-2  138	  27.04.1997	GC6	02:41	36ƒ45.2	   7ƒ15.1	496	2.88
M39019-1  139	  27.04.1997	Grab	13:46	36ƒ44.9	   8ƒ06.2	729
M39019-2  139	  27.04.1997	BC	14:22	36ƒ44.9	   8ƒ06.1	730	0.16
M39020-1  140	  27.04.1997	BC	15:16	36ƒ44.3	   8ƒ06.3	726	0.32
M39020-2  140	  27.04.1997	GC6	16:06	36ƒ44.4	   8ƒ6.2	728	2	   Core bent
M39020-3  140	  27.04.1997	PN	15:33-15:50
M39021-1  141	  28.04.1997	ROS/CTD	12:26	36ƒ36.5	   8ƒ15.4	900		   12/12 901,861,821,790,758,664,526,497,392,101, 50/52,10/11
M39021-2  141	  28.04.1997	GoFlo	13:44	36ƒ36.5	   8ƒ15.3	900		   Water samples at:860,875(S)
M39021-3  141	  28.04.1997	Grab	14:44	36ƒ36.5	   8ƒ15.4	903		   middle sand, clay
M39021-4  141	  28.04.1997	PN	14:25
M39021-5  141	  28.04.1997	BC	15:30	36ƒ36.5	   8ƒ15.3	901	0.36
M39022-1  142	  28.04.1997	BC	17:02	36ƒ42.7	   8ƒ15.6	668	0.36
M39022-2  142	  28.04.1997	PN	16:54
M39022-3  142	  28.04.1997	MUC	17:40	36ƒ42.7	   8ƒ15.6	668	0.24-0.27  4 Tubes empty, not triggered
M39022-4  142	  28.04.1997	GC6	18:20	36ƒ42.7	   8ƒ15.6	668	2.66
M39023-1  143	  28.04.1997	Grab	19:41	36ƒ44.1	   8ƒ15.3	728	full	   silty middle sand, corals, brachiopods
M39023-2  143	  28.04.1997	PN	19:23
M39023-3  143	  28.04.1997	BC	20:20	36ƒ44.1	   8ƒ15.3	730	0.34
M39024-1  144	  29.04.1997	Grab	10:20	36ƒ53.1	   8ƒ18.8	103		   not closed
M39024-2  144	  29.04.1997	Grab	10:31	36ƒ52.9	   8ƒ18.8	106	full	   clayish silt with endobenthic bivalves
M39024-3  144	  29.04.1997	PN	10:20
M39025-1  145	  29.04.1997	Grab	11:26	36ƒ48.2	   8ƒ18.7	272	full	   clayish silt with endobenthic bivalves (Nucula)
M39025-2  145	  29.04.1997	PN	11:22
M39026-1  146	  29.04.1997	Grab	12:09	36ƒ47.7	   8ƒ19.1	308	full	   clayish silt with Nucula
M39026-2  146	  29.04.1997	PN
M39027-1  147	  29.04.1997	Grab	12:52	36ƒ46.9	   8ƒ19.0	396		   silty fine sand
M39027-2  147	  29.04.1997	PN	12:41
M39028-1  148	  29.04.1997	Grab	13:37	36ƒ46.2	   8ƒ18.9	545	not closed
M39028-2  148	  29.04.1997	PN	13:22
M39028-3  148	  29.04.1997	Grab	14:08	36ƒ46.1	   8ƒ18.9	550	full	   silty fine to middle sand, with Bivalves and Coralls
M39029-1  149	  30.04.1997	CTD/ROS	12:53	36ƒ2.6	   8ƒ13.8	1915		   pinger at 30m,12/12 1933,1710,1503,1326,1207,896, 696,543,301,102,51,12
M39029-2  149	  30.04.1997	GoFlo	15:36	36ƒ2.7	   8ƒ14.0	1914		   Water samples at:540,1320,1700,1890 (S)
M39029-3  149	  30.04.1997	BC	17:27	36ƒ02.5	   8ƒ14.0	1917	0.36
M39029-4  149	  30.04.1997	GC6	18:39	36ƒ2.5	   8ƒ14.0	1918	3.055	   russian core device
M39029-5  149	  30.04.1997	PN	19:00				1917
M39029-6  149	  30.04.1997	MUC	19:50	36ƒ2.5	   8ƒ14.0	1919	0.31-0.45
M39029-7  149	  30.04.1997	GC6	21:05	36ƒ2.5	   8ƒ13.8	1917	5.02	   kiel core device
M39029-8  149	  30.04.1997	GC9	22:54	36ƒ2.5	   8ƒ13.8	1916	5.21	   kiel core device
M39030-1  150	  01.05.1997	Grab	09:08	37ƒ13.5	   9ƒ12.7	159.8		   carbonate fine sand to coarse sand
M39031-1  150*	  01.05.1997	Grab	09:35	37ƒ13.4	   9ƒ12.9	146.6	   empty
M39032-1  151	  01.05.1997	Grab	10:08	37ƒ12.9	   9ƒ13.5	310	not closed
M39032-2  151	  01.05.1997	Grab	10:24	37ƒ13.0	   9ƒ13.5	193	not closed
M39032-3  151	  01.05.1997	Grab	10:43	37ƒ12.9	   9ƒ13.5	322		   silty middle to coarse sand
M39033-1  152	  01.05.1997	Grab	11:57	37ƒ10.5	   9ƒ17.9	319	not closed
M39033-2  152	  01.05.1997	Grab	12:13	37ƒ10.5	   9ƒ17.8	319	full	   silty, carbonate sand
M39034-1  153	  01.05.1997	Grab	12:56	37ƒ10.9	   9ƒ17.4	197		   carbonate sand
M39034-2  153	  01.05.1997	Dredge	13:40	37ƒ10.9-   9ƒ17.5-	186		   stones, sponge, echinodemes
						37ƒ10.9	   9ƒ17.4
M39034-3  153	  01.05.1997	Drege	14:14	37ƒ10.9-   9ƒ17.5-	184		   seaurchins
						37ƒ10.9	   9ƒ17.4
M39035-1  154	  02.05.1997	CTD/ROS	09:17	37ƒ49.3	   9ƒ30.2	1086		   pinger at 30m,12/12 1094,1005.6,928.7,856.6,679, 633.3,605,354,201.6101.6,52.1,10.7
M39035-2  154	  02.05.1997	GoFlo	10:52	37ƒ49.3	   9ƒ30.2	1084		   water samples at:352,601,630,675,923,1059(S)
M39035-3  154	  02.05.1997	MUC	12:00	37ƒ49.350  9ƒ30.1	1085	0.18-0.44
M39035-4  154	  02.05.1997	PN	11:36
M39036-1  155	  02.05.1997	BC	14:07	37ƒ48.3	   9ƒ41.0	1747	0.46
M39036-2  155	  02.05.1997	GC6	15:20	37ƒ48.3	   9ƒ40.8	1746	5.71
M39036-3  155	  02.05.1997	PN	14:20
M39036-4  155	  02.05.1997	GC12	16:46	37ƒ48.3	   9ƒ40.8	1745	7.17
M39037-1  156	  02.05.1997	GC12	20:18	37ƒ48.5	   9ƒ59.77	2533	7
M39037-2  156	  02.05.1997	PN	19:51
M39037-3  156	  02.05.1997	BC	21:55	37ƒ48.5	   9ƒ59.6	2532	0.29
M39038-1  157	  03.05.1997	Grab	03:37	37ƒ44.7	   9ƒ28.1	508.8		   silty carbonate middle to coarse sand
M39039-1  158	  03.05.1997	Grab	05:16	37ƒ44.3	   9ƒ30.8	1014	full	   silty clay
M39040-1  159	  03.05.1997	Grab	06:19	37ƒ44.1	   9ƒ30.2	800		   clayish silt
M39041-1  160	  03.05.1997	Grab	07:18	37ƒ43.9	   9ƒ29.6	660		   silty carbonate sand
M39042-1  161	  03.05.1997	Grab	08:06	37ƒ43.7	   9ƒ29.2	568		   middle sand
M39043-1  162	  03.05.1997	Grab	08:54	37ƒ43.4	   9ƒ28.5	424		   mudpebbles,pebble with sessile organisms, ophiorae (Starfish)
M39043-2  162	  03.05.1997	Grab	09:13	37ƒ43.5	   9ƒ28.5	401
M39044-1  163	  03.05.1997	Grab	09:47	37ƒ43.5	   9ƒ28.5	398		   fine to middle sand with ophiorae
M39045-1  164	  03.05.1997	Grab	10:33	37ƒ43.7	   9ƒ27.6	470	not closed
M39045-2  	  03.05.1997	Grab	10:54	37ƒ43.7	   9ƒ27.6	470
M39046-1  165	  03.05.1997	Grab	11:50	37ƒ44.1	   9ƒ26.3	740	not closed
M39046-2  165	  03.05.1997	Grab	12:25	37ƒ44.0	   9ƒ26.3	716
M39047-1  166	  03.05.1997	Grab	14:39	37ƒ33.8	   9ƒ11.1	451		   glauconitic sand with benthic forams and bivalves
M39047-2  166	  03.05.1997	PN	14:30
M39048-1  167	  03.05.1997	Grab	16:08	37ƒ37.3	   9ƒ02.8	253		   carbonate sand
M39048-2  167	  03.05.1997	PN	16:03
M39049-1  168	  03.05.1997	Grab	18:48	37ƒ42.9	   8ƒ50.5	51	not closed
M39049-2  168	  03.05.1997	PN	18:46
M39049-3  168	  03.05.1997	Grab	18:53	37ƒ42.9	   8ƒ50.5	55	empty
M39049-4  168	  03.05.1997	Grab	19:02	37ƒ42.9	   8ƒ50.6	55		   carbonate coarse sand with bivalves;pebbles with sessile epifauna
M39050-1  169	  03.05.1997	Grab	19:38	37ƒ42.1	   8ƒ52.5	93	empty
M39050-2  169	  03.05.1997	PN	19:34
M39050-3  169	  03.05.1997	Grab	19:49	37ƒ42.1	   8ƒ52.6	93		   carbonate coarse sand, pebbles with sessile epifauna
M39051-1  170	  03.05.1997	Grab	20:30	37ƒ40.7	   8ƒ55.1	127		   middle sand with glauconitic
M39051-2  170	  03.05.1997	PN	20:28
M39052-1  171	  03.05.1997	Grab	21:15	37ƒ39.6	   8ƒ57.7	145.3		   glauconitic middle to coarse sand
M39052-2  171	  03.05.1997	PN	21:10
M39053-1  172	  03.05.1997	Grab	21:56	37ƒ38.8	   8ƒ59.5	164		   glauconitic middle to coarse sand
M39053-2  172	  03.05.1997	PN	21:51
M39054-1  173	  03.05.1997	Grab	22:36	37ƒ38.1	   9ƒ00.8	200		   glauconitic middle to coarse sand
M39054-2  173	  03.05.1997	PN	22:31
M39055-1  174	  04.05.1997	Grab	07:22	38ƒ49.9	   10ƒ02.1	180		   carbonate sand
M39056-1  175	  04.05.1997	Grab	07:48	38ƒ49.9	   10ƒ01.8	119		   sponge
M39057-1  176	  04.05.1997	Dredge	10:45-	39ƒ05.0	   10ƒ10.1	150(190)	   boulders, pebbles with sessile epifauna, crinoids
					11:19
M39058-1  177	  04.05.1997	BC	16:50	39ƒ02.4	   10ƒ40.8	1975	0.29
M39058-2  177	  04.05.1997	GC6	18:14	39ƒ2.4	   10ƒ40.8	1974	3.2
M39058-3  177	  04.05.1997	PN	18:05
M39059-1  178	  04.05.1997	GC6	20:04	39ƒ04.0	   10ƒ32.1	1605	0.95
M39059-2  178	  04.05.1997	BC	20:45	39ƒ4.1	   10ƒ32.2	1605	0.18
M39060-1  179	  05.05.1997	BC	12:15	40ƒ06.3	   09ƒ51.3	1166	0.3
M39061-1  180	  05.05.1997	BC	14:10	40ƒ06.5	   09ƒ41.8	544	0.3

7.1.2	Water sampling sites for plankton assemblage studies

FILTER	DATE	 METEOR	GEOMAR	   LATITUDE	LONGITUDE WATER		WATER TEMP.	SALINITY	WATER
NR.		 STA.	NUMBER	   N		W	  DEPTH[m]	[ƒC]				FILTERED [l]
1	20/04/97 # 121	M39001-1   36ƒ02,6	011ƒ45,6  10		17.92		36.41		1
2							  147		14.61		36.02		1.5
3							  345		12.52		35.68		2
4							  797		10.44		35.70		1.5
5							  946		10.35		35.91		1.5
6		 Sea floor at:				  1156		11.19		36.24		2
		 1176 m
7	22/04/97 # 123	M39003-6   36ƒ06,9	007ƒ14,0  10		18		36.50		1.5
8							  50		17		36.40		2
9							  100		15.7		36.20		2
10							  211		14.5		36.00		2
11							  502		11.3		35.60		2
12		 Sea floor at:				  804		11.15		36.06		2
		 810 m
13	24/04/97 # 135	M39015-1   36ƒ14,2	007ƒ43,8  10		17.9		36.40		2
14							  64		17.2		36.40		2
15							  117		15.8		36.20		2
16							  203		14.1		35.90		2
17							  622		11.2		35.60		2
18		 Sea floor at:				  937		12.3		36.50		2
		 945 m
19	26/04/97 # 137	M39017-1   36ƒ38,9	007ƒ24,5  10		18.2		36.40		2
20							  60		17.3		36.40		2
21							  100		16.2		36.30		2
22							  202		14.2		36.00		2
23							  410		12.4		35.70		2
24		 Sea floor at:				  529		12.3		36.10		2
		 535 m
25	28/04/97 # 141	M39021-1   36ƒ36,500	008ƒ15,300 10		18.16		36.34		2
26							  50		17.61		36.45		2
27							  100		16.24		36.31		2
28							  390		12.36		35.70		2
29							  525		11.32		35.64		2
30		 Sea floor at:				  860		12.51		36.51		2
		 892 m
31	30/04/97 # 149	M39029-1   36ƒ02,568	008ƒ13,752 10		18.9		36.50		2
32							  50		17.8		36.50		2
33							  100		15.8		36.20		2
34							  544		10.8		35.60		2
35							  897		9.6		35.60		2
36		 Sea floor at:				  1503		8		35.70		2
		 1950 m

37	02/05/97 # 154	M39035-1   37ƒ49,360	009ƒ30,226 10		18.3		36.20		2
38							  50		16.6		36.20		2
39							  100		15.1		36.10		2
40							  354		12.6		35.70		2
41							  680		12.6		36.20		2
42		 Sea floor at:				  1005		12.6		36.30		2
		 1088 m
43	06/05/97 # 184	M39065-1   40ƒ34,768	010ƒ20,962 10		16.83		35.98		2
44							  50		14.57		35.91		2
45							  100		13.85		35.85		2
46							  400		11.47		35.58		2
47							  793		12.1		36.16		2
48		 Sea floor at:				  1186		11.33		36.20		2
		 3350 m
49	09/05/97 # 193	M39073-1   43ƒ51,600	009ƒ50,089 10		14		35.70		1.5
50							  50		14		35.70		1.5
51							  100		12.8		35.70		2
52							  457		11.2		35.50		2
53							  993		10.9		36.02		2
54		 Sea floor at:				  2041		3.79		34.97		2
		 3200 m

7.1.3	Phyto- and zooplankton species found in M39/1 sampling sites*

*Please see pdf file for this table.

7.2	Leg M39/2
7.2.1	CTD Inventory

STAT	PROF	DATE		HOUR	LATITUDE	LONGITUDE	DEPTH	PMAX
		YYYY  MM DD		N		E		m	dbar
199	 1	1997  5  16	 9.000	50.6133		 -9.0631	127	104
200	 2	1997  5  17	 9.000	54.6656		-10.5825	342	324
201	 3	1997  5  17	10.000	54.7373		-10.7316	1646	1662
201	 4	1997  5  17	13.000	54.7372		-10.7184	1540	1554
202	 5	1997  5  17	15.000	54.7998		-10.8638	1922	1942
203	 6	1997  5  17	19.000	54.9009		-11.0960	2630	2632
204	 7	1997  5  18	 0.000	55.1429		-11.6393	2630	2796
205	 8	1997  5  18	 6.000	55.5772		-12.6013	2829	2838
206	 9	1997  5  18	12.000	55.9998		-13.5626	2829	2552
207	10	1997  5  18	15.000	56.1419		-13.8858	2196	2192
208	11	1997  5  18	19.000	56.2832		-14.2142	1118	1106
209	12	1997  5  18	23.000	56.5619		-14.8277	200	174
210	13	1997  5  19	 4.000	56.9964		-15.9990	1075	1056
211	14	1997  5  19	 8.000	57.2823		-16.8920	1302	1276
212	15	1997  5  19	13.000	57.6181		-17.6186	1244	1228
213	16	1997  5  19	17.000	57.9157		-18.5818	849	856
214	17	1997  5  19	22.000	58.2678		-19.5044	9999	1586
215	18	1997  5  20	 4.000	58.6668		-20.6338	2909	2916
216	19	1997  5  20	11.000	59.0868		-21.8491	2408	2878
217	20	1997  5  20	17.000	59.4084		-22.8425	2516	2508
218	21	1997  5  20	22.000	59.7442		-23.8193	2636	2354
219	22	1997  5  21	 4.000	60.0704		-24.7252	2287	2278
220	23	1997  5  21	13.000	60.3772		-25.6542	2287	2126
221	24	1997  5  21	16.000	60.5694		-26.2344	1927	1920
222	25	1997  5  21	20.000	60.7676		-26.8329	9999	1548
223	26	1997  5  22	 0.000	60.9534		-27.3308	1364	1786
224	27	1997  5  22	 3.000	61.1661		-27.9373	976	944
225	28	1997  5  22	14.000	59.6670		-29.8243	1088	1080
226	29	1997  5  22	20.000	59.2089		-28.5529	2054	2016
227	30	1997  5  23	 2.000	58.7604		-27.2662	2054	2200
228	31	1997  5  23	 9.000	58.2659		-26.0048	2569	2562
229	32	1997  5  23	16.000	57.7941		-24.7145	2812	2810
230	33	1997  5  23	23.000	57.3007		-23.4189	3052	3058
231	34	1997  5  24	 6.000	56.8255		-22.1344	2295	2284
232	35	1997  5  24	14.000	56.2951		-20.8421	1563	1560
233	36	1997  5  25	 0.000	56.0012		-23.3165	2345	2344
234	37	1997  5  25	11.000	55.6912		-25.7763	3311	3322
235	38	1997  5  25	21.000	55.4001		-27.9416	2804	2806
236	39	1997  5  26	 6.000	55.1273		-30.2160	2804	2996
237	40	1997  5  26	14.000	54.9152		-31.6450	2617	2618
238	41	1997  5  26	19.000	54.7844		-32.5150	2632	2622
239	42	1997  5  27	 0.000	54.6750		-33.3384	2458	2442
240	43	1997  5  27	 6.000	54.5770		-34.1944	1749	1714
241	44	1997  5  27	 9.000	54.5072		-34.7265	1499	1412
242	45	1997  5  27	19.000	54.2773		-32.8919	2707	2700
243	46	1997  5  28	 0.000	54.3644		-33.5911	2647	2714
244	47	1997  5  28	 7.000	54.0568		-32.3555	2831	2798
245	48	1997  5  28	16.000	53.5449		-31.0454	3174	3162
245	49	1997  5  28	19.000	53.5356		-31.0461	3178	3158
245	50	1997  5  28	21.000	53.5309		-31.0331	3175	3156
246	51	1997  5  29	 3.000	53.2521		-30.3054	3066	3054
247	52	1997  5  29	12.000	52.9652		-29.5679	3389	3402
248	53	1997  5  29	20.000	52.4885		-28.4173	3779	3792
249	54	1997  5  31	 4.000	53.8349		-31.7787	2848	2862
250	55	1997  5  31	22.000	53.2172		-35.1645	2749	2734
251	56	1997  6  1	 2.000	52.8671		-34.9184	3335	3310
252	57	1997  6  1	 6.000	52.7510		-35.0010	3152	3174
253	58	1997  6  1	 9.000	52.6503		-34.9970	3412	3420
254	59	1997  6  1	14.000	52.3477		-35.0022	3856	3876
255	60	1997  6  1	18.000	52.0989		-35.0016	3324	3366
256	61	1997  6  2	 1.000	51.3488		-34.9972	3300	3312
257	62	1997  6  2	 8.000	51.4490		-33.4906	3868	3898
258	63	1997  6  2	16.000	51.6081		-32.0429	2981	3046
259	64	1997  6  3	 1.000	51.7665		-30.3364	2300	2274
260	65	1997  6  3	 5.000	51.7508		-30.0036	3238	3242
261	66	1997  6  3	 9.000	51.8290		-29.5218	2243	2398
261	67	1997  6  3	11.000	51.8315		-29.5219	2358	2416
261	68	1997  6  3	13.000	51.8370		-29.5223	2358	2474
262	69	1997  6  3	18.000	52.0003		-28.9596	3755	3792
263	70	1997  6  4	 0.000	52.3165		-28.1166	3770	3804
264	71	1997  6  4	 9.000	52.9329		-26.5365	3704	3736
265	72	1997  6  4	20.000	51.7607		-24.7344	3929	3962
266	73	1997  6  5	14.000	51.0518		-20.5638	4307	4366
267	74	1997  6  5	23.000	50.7333		-18.6706	4723	4806
268	75	1997  6  5	10.000	50.4215		-16.7619	4745	4836
269	76	1997  6  5	18.000	50.5274		-15.5674	4264	4324
270	77	1997  6  6	23.000	50.6337		-14.8419	3221	3264
271	78	1997  6  7	 4.000	50.7176		-14.2003	1010	1002
272	79	1997  6  7	13.000	50.9880		-12.0890	1800	1812

7.2.2	Mooring Activities

STA.	INT.	IFM	DATE 1997	LATITUDE	LONGITUDE	DEPTH	INSTR.	REMARKS INCL.
NO.	NO.	NO.			NORTH		WEST		(m)	TYPE	NOMINAL INSTR. DEPTH
CURRENT METER MOORINGS
246	IM3	V388	29 May		53ƒ14.6'N	030ƒ16.0'W	3087	SoSo	No.23,Win.01:30Z
											@1407m
										ACM	No.10078@1357m
										ACM	No. 8412@2207m
										ACM	No. 9819@2507m
										ACM	No. 6159@2757m
										ACM	No. 8575@3037m
242		V386	27 May		54ƒ17.1'N	032ƒ57.0'W	2723	ACM	No.12051@1213m
										ACM	No. 9812@2063m
										ACM	No. 7929@2363m
										ACM	No. 7927@2673m
249		V387	31 May		53ƒ50.2'N	031ƒ43.6'W	2858	ACM	No.10074@1310m
										ACM	No. 9311@2258m
										ACM	No. 4570@2558m
										ACM	No. 4563@2808m
SOUND SOURCE MOORINGS
219	IM1	V384	21 May		60ƒ04.3'N	024ƒ43.5'W	2281	SoSo	No. 24, Win 01:00Z
											@1381m
										ACM	No. 9346@1331m
										Wdog	ARGOS 2263
231	IM2	V385	24 May		56ƒ48.7'N	022ƒ08.0'W	2307	SoSo	No22, Win 00:30Z
											@1447m
			(see Fig. B3)							no ac. release
										Wdog	ARGOSS 2264
	IM3		    -- see above --

SoSo	Sound source
Win	window
ACM	Aanderaa Current Meter
Wdog	Watch Dog buoy

7.2.3	List of RAFOS Float Launches

STA.	IFM	DATE	TIME	LATITUDE	LONGITUDE	ARGOS	MISSION	REMARKS
NO.	NO.	1997	Z	NORTH	WEST	(DEC)	(MONTHS)
RAFOS FLOATS
203	403	17/5	22:05	54ƒ53.9'N	011ƒ05.8'W	12611	12	Eastern boundary
								Rockall Tr.
207	408	18/5	18:05	56ƒ08.6'N	013ƒ53.8'W	12617	18	Western boundary
215	405	20/5	07:07	58ƒ40.4'N	020ƒ38.4'W	12613	15	Maury Channel North
217	411	20/5	19:17	59ƒ24.6'N	022ƒ49.3'W	12620	24	Central Iceland Basin
220	407	21/5	14:56	60ƒ22.8'N	025ƒ39.4'W	12616	18	Reykjanes Ridge North
227	406	23/5	04:44	58ƒ45.7'N	027ƒ13.8'W	12614	15	Reykjanes Ridge South
229	404	23/5	18:32	57ƒ47.7'N	024ƒ42.4'W	12612	12	Central Iceland Basin
231	409	24/5	09:47	56ƒ48.4'N	022ƒ08.3'W	12618	21	Rockall Platateau West
234	410	25/5	13:39	55ƒ41.5'N	025ƒ45.8'W	12619	21	Maury Channel
245	401	29/5	00:46	53ƒ31.9'N	031ƒ01.6'W	4374	14	1st float park (North)
261	402B	3/6	15:41	51ƒ50.7'N	029ƒ32.0'W	4375	24	2nd float park (South)
DUAL RELEASE RAFOS FLOATS deployed by CTD probe ('Ofenrohr') (see Fig. B4)
245	412	28/5	18:07	53ƒ32.3'N	031ƒ02.6'W	4376	2+12	1st float park (North)
245	413	28/5	20:38	53ƒ31.9'N	031ƒ02.2'W	4377	4+10	1st float park (North)
245	414	28/5	23:14	53ƒ32.0'N	031ƒ01.9'W	12615	6+8	1st float park (North)
261	415	3/6	10:28	51ƒ50.1'N	029ƒ31.4'W	5487	3+21	2nd float park (South)
261	416	3/6	12:31	51ƒ50.2'N	029ƒ31.4'W	12610	6+18	2nd float park (South)
261	417	3/6	14:31	51ƒ50.3'N	029ƒ31.6'W	12621	9+15	2nd float park (South)

7.3	Leg M39/3
7.3.1	Station list of cruise M39/3

A2 R/V METEOR CURISE 039 leg 3	Version 1.1 February 1998; 03.03.98 Update
SHIP/CRS	WOCE			CAST		UTC		        POSITION			UNC  HT ABOVE	WIRE	MAX	NO. OF
EXPOCODE	SECT	STNBR	CASTNO	TYPE	DATE	TIME	CODE	LATITUDE	LONGITUDE	NAV	DEPTH	BOTTOM	OUT	PRESS	BOTTLES	COMMENTS
06MT039/3	A2	274	01	ROS	061397	0929	BE	48 55.3 N	13 16.3 W	GPS	3719
06MT039/3	A2	274	01	ROS	061397	1044	BO	48 55.6 N	13 16.8 W	GPS	3719	09	3731	3500	22
06MT039/3	A2	274	01	ROS	061397	1207	EN	48 55.6 N	13 17.3 W	GPS	3719
06MT039/3	A2	275	02	ROS	061397	1416	BE	49 00.1 N	13 02.5 W	GPS	3124
06MT039/3	A2	275	02	ROS	061397	1513	BO	49 00.2 N	13 02.5 W	GPS	3124	10	3107	3149	22
06MT039/3	A2	275	02	ROS	061397	1627	EN	49 00.3 N	13 02.5 W	GPS	3124
06MT039/3	A2	276	01	ROS	061397	1753	BE	49 00.0 N	12 58.9 W	GPS	2570
06MT039/3	A2	276	01	ROS	061397	1843	BO	49 00.1 N	12 58.9 W	GPS	2570	07	2565	2598	22
06MT039/3	A2	276	01	ROS	061397	1952	EN	49 00.0 N	12 59.4 W	GPS	2570
06MT039/3	A2	277	01	ROS	061397	2149	BE	49 00.9 N	12 51.4 W	GPS	2019
06MT039/3	A2	277	01	ROS	061397	2231	BO	49 00.9 N	12 51.6 W	GPS	2019	09	2004	2020	21
06MT039/3	A2	277	01	ROS	061397	2337	EN	49 01.1 N	12 52.2 W	GPS	2019
06MT039/3	A2	278	01	ROS	061497	0111	BE	49 03.1 N	12 41.5 W	GPS	1509
06MT039/3	A2	278	01	ROS	061497	0142	BO	49 03.1 N	12 41.7 W	GPS	1509	11	1489	1450	17
06MT039/3	A2	278	01	ROS	061497	0228	EN	49 03.1 N	12 41.9 W	GPS	1509
06MT039/3	A2	279	01	ROS	061497	0436	BE	49 06.6 N	12 12.0 W	GPS	1013
06MT039/3	A2	279	01	ROS	061497	0502	BO	49 06.6 N	12 12.1 W	GPS	1013	10	1004	0999	13
06MT039/3	A2	279	01	ROS	061497	0536	EN	49 06.7 N	12 12.5 W	GPS	1013
06MT039/3	A2	280	01	ROS	061497	0847	BE	49 11.0 N	11 26.2 W	GPS	495
06MT039/3	A2	280	01	ROS	061497	0900	BO	49 11.2 N	11 26.2 W	GPS	495	10	482	0469	8
06MT039/3	A2	280	01	ROS	061497	0923	EN	49 11.2 N	11 26.3 W	GPS	495
06MT039/3	A2	281	01	ROS	061497	1036	BE	49 11.9 N	11 11.0 W	GPS	200
06MT039/3	A2	281	01	ROS	061497	1046	BO	49 11.9 N	11 10.9 W	GPS	200	09	185	0177	5
06MT039/3	A2	281	01	ROS	061497	1104	EN	49 12.1 N	11 10.8 W	GPS	200
06MT039/3	A2	282	01	ROS	061497	1329	BE	49 13.9 N	10 38.9 W	GPS	160
06MT039/3	A2	282	01	ROS	061497	1338	BO	49 13.9 N	10 38.9 W	GPS	160	09	147	0150	7
06MT039/3	A2	282	01	ROS	061497	1354	EN	49 13.9 N	10 38.8 W	GPS	160
06MT039/3	A2	283	01	ROS	061597	2315	BE	48 55.3 N	13 16.4 W	GPS	3729
06MT039/3	A2	283	01	ROS	061697	0020	BO	48 55.5 N	13 16.2 W	GPS	3729	09	3735	3770	22
06MT039/3	A2	283	01	ROS	061697	0151	EN	48 55.9 N	13 15.9 W	GPS	3729
06MT039/3	A2	283	02	ROS	061597	0219	BE	48 55.9 N	13 15.9 W	GPS	3723
06MT039/3	A2	283	02	ROS	061597	0319	BO	48 55.8 N	13 15.9 W	GPS	3723	09	3564	3499	36
06MT039/3	A2	283	02	ROS	061597	0551	EN	48 55.9 N	13 15.2 W	GPS	3723
06MT039/3	A2	284	01	ROS	061597	0734	BE	48 51.4 N	13 48.2 W	GPS	4515
06MT039/3	A2	284	01	ROS	061597	0856	BO	48 51.5 N	13 47.9 W	GPS	4515	10	4527	4601	22
06MT039/3	A2	284	01	ROS	061597	1052	EN	48 51.8 N	13 47.7 W	GPS	4515
06MT039/3	A2	285	01	ROS	061597	1428	BE	48 44.5 N	14 44.1 W	GPS	4717
06MT039/3	A2	285	01	ROS	061597	1601	BO	48 44.4 N	14 44.0 W	GPS	4717	20	4730	4784	21
06MT039/3	A2	285	01	ROS	061597	1750	EN	48 44.4 N	14 43.7 W	GPS	4717
06MT039/3	A2	286	01	ROS	061597	2059	BE	48 36.4 N	15 28.7 W	GPS	4802
06MT039/3	A2	286	01	ROS	061597	2229	BO	48 36.4 N	15 29.1 W	GPS	4802	17	4814	4858	21
06MT039/3	A2	286	01	ROS	061597	0031	EN	48 36.8 N	15 29.6 W	GPS	4802
06MT039/3	A2	287	01	ROS	061697	0445	BE	48 27.1 N	16 34.9 W	GPS	4818
06MT039/3	A2	287	01	ROS	061697	0618	BO	48 27.0 N	16 34.8 W	GPS	4818		4842	4894	22
06MT039/3	A2	287	01	ROS	061697	0810	EN	48 26.8 N	16 34.9 W	GPS	4818
06MT039/3	A2	288	01	ROS	061697	1616	BE	48 18.0 N	17 40.9 W	GPS	4016
06MT039/3	A2	288	01	ROS	061697	1727	BO	48 18.2 N	17 41.3 W	GPS	4016		4016	4043	19
06MT039/3	A2	288	01	ROS	061697	1858	EN	48 18.3 N	17 41.7 W	GPS	4016
06MT039/3	A2	289	02	ROS	061797	0221	BE	48 09.8 N	18 40.1 W	GPS	4395
06MT039/3	A2	289	02	ROS	061797	0342	BO	48 09.8 N	18 40.3 W	GPS	4395		4419	4470	20
06MT039/3	A2	289	02	ROS	061797	0525	EN	48 09.8 N	18 40.6 W	GPS	4395
06MT039/3	A2	290	01	ROS	061797	0956	BE	48 01.8 N	19 39.4 W	GPS	4471
06MT039/3	A2	290	01	ROS	061797	1121	BO	48 01.8 N	19 36.7 W	GPS	4471	20	4476	4513	21
06MT039/3	A2	290	01	ROS	061797	1310	EN	48 01.8 N	19 40.0 W	GPS	4471
06MT039/3	A2	291	01	ROS	061797	1837	BE	47 53.6 N	20 39.2 W	GPS	4343
06MT039/3	A2	291	01	ROS	061797	1956	BO	47 53.6 N	20 39.7 W	GPS	4343	09	4362	4417	35
06MT039/3	A2	291	01	ROS	061797	2142	EN	47 53.2 N	20 40.0 W	GPS	4343
06MT039/3	A2	291	02	ROS	061797	2223	BE	47 53.1 N	20 39.7 W	GPS	4333
06MT039/3	A2	291	02	ROS	061797	2242	BO	47 53.0 N	20 39.7 W	GPS	4333	09	993	0899	12
06MT039/3	A2	291	02	ROS	061797	2312	EN	47 53.0 N	20 40.0 W	GPS	4333
06MT039/3	A2	292	02	ROS	061897	0639	BE	47 45.9 N	21 37.8 W	GPS	4114
06MT039/3	A2	292	02	ROS	061897	0752	BO	47 45.9 N	21 38.1 W	GPS	4114		4122	4159	22
06MT039/3	A2	292	02	ROS	061897	0924	EN	47 45.7 N	21 37.9 W	GPS	4114
06MT039/3	A2	293	02	ROS	061897	1342	BE	47 37.6 N	22 36.0 W	GPS	4070
06MT039/3	A2	293	02	ROS	061897	1459	BO	47 37.6 N	22 36.3 W	GPS	4070		4075	4110	22
06MT039/3	A2	293	02	ROS	061897	1638	EN	47 37.6 N	22 36.3 W	GPS	4070
06MT039/3	A2	293	03	ROS	061897	1642	BE	47 37.4 N	22 36.3 W	GPS	4011
06MT039/3	A2	293	03	ROS	061897	1659	BO	47 37.4 N	22 36.3 W	GPS	4011		995	0900	12
06MT039/3	A2	293	03	ROS	061897	1727	EN	47 37.2 N	22 36.4 W	GPS	4011
06MT039/3	A2	294	02	ROS	061897	1956	BE	47 33.8 N	23 05.3 W	GPS	4224
06MT039/3	A2	294	02	ROS	061897	2110	BO	47 33.7 N	23 05.4 W	GPS	4224		4220	4266	22
06MT039/3	A2	294	02	ROS	061897	2255	EN	47 37.6 N	23 05.5 W	GPS	4224
06MT039/3	A2	294	03	ROS	061897	2304	BE	47 33.7 N	23 05.4 W	GPS	4234
06MT039/3	A2	294	03	ROS	061897	2326	BO	47 33.7 N	23 05.5 W	GPS	4234		994	0874	12
06MT039/3	A2	294	03	ROS	061897	2355	EN	47 33.6 N	23 05.5 W	GPS	4234
06MT039/3	A2	295	01	ROS	061997	0217	BE	47 29.6 N	23 33.5 W	GPS	3988
06MT039/3	A2	295	01	ROS	061997	0329	BO	47 29.4 N	23 33.0 W	GPS	3988		3987	4019	22
06MT039/3	A2	295	01	ROS	061997	0508	EN	47 29.4 N	23 34.5 W	GPS	3988
06MT039/3	A2	296	01	ROS	061997	0837	BE	47 23.0 N	24 15.9 W	GPS	3327
06MT039/3	A2	296	01	ROS	061997	0939	BO	47 22.9 N	24 16.0 W	GPS	3327	20	3312	3320	21
06MT039/3	A2	296	01	ROS	061997	1107	EN	47 22.9 N	24 16.1 W	GPS	3327
06MT039/3	A2	297	01	ROS	061997	1516	BE	47 16.9 N	25 00.6 W	GPS	3040
06MT039/3	A2	297	01	ROS	061997	1613	BO	47 16.8 N	25 00.6 W	GPS	3040		3045	3046	22
06MT039/3	A2	297	01	ROS	061997	1732	EN	47 16.1 N	25 02.1 W	GPS	3040
06MT039/3	A2	298	01	ROS	061997	2125	BE	47 10.7 N	25 43.2 W	GPS	2977
06MT039/3	A2	298	01	ROS	061997	2225	BO	47 10.6 N	25 43.4 W	GPS	2977		3013	2972	22
06MT039/3	A2	298	01	ROS	061997	2345	EN	47 10.5 N	25 43.8 W	GPS	2977
06MT039/3	A2	298	05	ROS	062097	0020	BE	47 10.5 N	25 43.6 W	GPS	3058
06MT039/3	A2	298	05	ROS	062097	0117	BO	47 10.4 N	25 44.2 W	GPS	3058	13	3041	3066	24
06MT039/3	A2	298	05	ROS	062097	0233	EN	47 10.2 N	25 45.2 W	GPS	3058
06MT039/3	A2	299	01	ROS	062097	0533	BE	47 06.4 N	26 17.1 W	GPS	2519
06MT039/3	A2	299	01	ROS	062097	0621	BO	47 06.3 N	26 17.4 W	GPS	2519		2410	2404	22
06MT039/3	A2	299	01	ROS	062097	0729	EN	47 06.2 N	26 17.9 W	GPS	2519
06MT039/3	A2	300	01	ROS	062097	0941	BE	47 03.2 N	26 39.6 W	GPS	2802
06MT039/3	A2	300	01	ROS	062097	1035	BO	47 03.0 N	26 39.9 W	GPS	2802	20	2782	2800	22
06MT039/3	A2	300	01	ROS	062097	1150	EN	47 02.9 N	26 40.4 W	GPS	2802
06MT039/3	A2	301	01	ROS	062097	1329	BE	46 59.0 N	26 59.5 W	GPS	2178
06MT039/3	A2	301	01	ROS	062097	1412	BO	46 58.9 N	26 59.6 W	GPS	2178		2162	2170	22
06MT039/3	A2	301	01	ROS	062097	1519	EN	46 59.0 N	26 59.9 W	GPS	2178
06MT039/3	A2	302	01	ROS	062097	1658	BE	46 54.7 N	27 18.3 W	GPS	3487
06MT039/3	A2	302	01	ROS	062097	1801	BO	46 54.8 N	27 18.3 W	GPS	3487		3517	3541	22
06MT039/3	A2	302	01	ROS	062097	1926	EN	46 54.7 N	27 18.3 W	GPS	3487
06MT039/3	A2	302	02	FLT	062097	2042	EN	46 54.4 N	27 18.3 W	GPS	3487		ALACE   719   FLOAT
06MT039/3	A2	302	02	ROS	062097	1923	BE	46 54.7 N	27 18.3 W	GPS	3501
06MT039/3	A2	302	02	ROS	062097	1952	BO	46 54.7 N	27 18.4 W	GPS	3501		1011	0999	12
06MT039/3	A2	302	02	ROS	062097	2023	EN	46 54.7 N	27 18.4 W	GPS	3501
06MT039/3	A2	303	01	ROS	062197	0109	BE	46 43.5 N	28 15.9 W	GPS	3398
06MT039/3	A2	303	01	ROS	062197	0218	BO	46 43.6 N	28 15.8 W	GPS	3398		3381	3407	22
06MT039/3	A2	303	01	ROS	062197	0346	EN	46 43.6 N	28 15.8 W	GPS	3398
06MT039/3	A2	304	01	ROS	062197	0812	BE	46 32.5 N	29 08.8 W	GPS	2995
06MT039/3	A2	304	01	ROS	062197	0910	BO	46 32.6 N	29 08.7 W	GPS	2995	20	2953	2969	22
06MT039/3	A2	304	01	ROS	062197	1029	EN	46 32.4 N	29 08.5 W	GPS	2995
06MT039/3	A2	304	02	FLT	062197	1039	EN	46 32.4 N	29 08.4 W	GPS	2995		ALACE   720   FLOAT
06MT039/3	A2	305	00	MOR	062297	1426	BE	46 19.8 N	29 55.3 W	GPS	3308		Recovery of MOORING K1/96
06MT039/3	A2	305	00	MOR	062297	2235	EN	46 21.3 N	29 55.9 W	GPS	3308		New MOORING K1/97
06MT039/3	A2	305	01	ROS	062297	2310	BE	46 19.9 N	29 55.8 W	GPS	3296
06MT039/3	A2	305	01	ROS	062397	0011	BO	46 19.8 N	29 55.8 W	GPS	3296	19	3268	3305	21
06MT039/3	A2	305	01	ROS	062397	0128	EN	46 19.7 N	29 55.8 W	GPS	3296
06MT039/3	A2	306	01	ROS	062297	0528	BE	46 05.0 N	30 46.4 W	GPS	3277
06MT039/3	A2	306	01	ROS	062297	0624	BO	46 04.9 N	30 46.5 W	GPS	3277	09	3266	3300	22
06MT039/3	A2	306	01	ROS	062297	0742	EN	46 04.9 N	30 46.7 W	GPS	3277
06MT039/3	A2	307	01	ROS	062297	1134	BE	45 50.1 N	31 36.8 W	GPS	3651
06MT039/3	A2	307	01	ROS	062297	1245	BO	45 50.1 N	31 36.8 W	GPS	3651	19	3637	3682	22
06MT039/3	A2	307	01	ROS	062297	1410	EN	45 49.8 N	31 36.6 W	GPS	3651
06MT039/3	A2	307	02	FLT	062297	1414	EN	45 49.5 N	31 37.7 W	GPS	3651		ALACE   718   FLOAT
06MT039/3	A2	308	01	ROS	062297	1802	BE	45 35.3 N	31 26.7 W	GPS	3772
06MT039/3	A2	308	01	ROS	062297	1908	BO	45 35.0 N	31 26.6 W	GPS	3772	09	3782	3800	21
06MT039/3	A2	308	01	ROS	062297	2033	EN	45 34.4 N	31 26.2 W	GPS	3772
06MT039/3	A2	309	01	ROS	062397	0015	BE	45 19.2 N	33 12.7 W	GPS	3653
06MT039/3	A2	309	01	ROS	062397	0121	BO	45 18.9 N	33 12.2 W	GPS	3653	11	3663	3704	22
06MT039/3	A2	309	01	ROS	062397	0245	EN	45 18.7 N	33 11.9 W	GPS	3653
06MT039/3	A2	309	02	MOR	062397	0621	BE	45 19.8 N	33 12.6 W	GPS	3653		Recovery of MOORING K3/96
06MT039/3	A2	309	02	MOR	062397	1434	EN	45 19.3 N	33 09.1 W	GPS	3567		New MOORING K3/97
06MT039/3	A2	310	01	ROS	062397	1935	BE	45 07.2 N	34 04.8 W	GPS	3619
06MT039/3	A2	310	01	ROS	062397	2040	BO	45 07.1 N	34 04.8 W	GPS	3619	09	3625	3669	21
06MT039/3	A2	310	01	ROS	062397	2206	EN	45 07.2 N	34 04.4 W	GPS	3619
06MT039/3	A2	311	01	ROS	062497	0153	BE	44 55.6 N	34 45.7 W	GPS	4068
06MT039/3	A2	311	01	ROS	062497	0308	BO	44 55.4 N	34 45.4 W	GPS	4068	11	4080	4132	22
06MT039/3	A2	311	01	ROS	062497	0437	EN	44 55.2 N	34 45.3 W	GPS	4068
06MT039/3	A2	312	01	ROS	062497	0759	BE	44 45.1 N	35 24.6 W	GPS	3953
06MT039/3	A2	312	01	ROS	062497	0911	BO	44 45.1 N	35 24.6 W	GPS	3953	10	3965	4014	22
06MT039/3	A2	312	01	ROS	062497	1046	EN	44 44.9 N	35 24.7 W	GPS	3953
06MT039/3	A2	313	01	ROS	062497	1403	BE	44 34.0 N	36 05.0 W	GPS	4078
06MT039/3	A2	313	01	ROS	062497	1518	BO	44 33.7 N	36 05.2 W	GPS	4078	09	4110	4158	22
06MT039/3	A2	313	01	ROS	062497	1648	EN	44 33.6 N	36 05.1 W	GPS	4078
06MT039/3	A2	314	01	ROS	062497	2043	BE	44 20.0 N	36 54.5 W	GPS	4233
06MT039/3	A2	314	01	ROS	062497	2200	BO	44 19.9 N	36 54.5 W	GPS	4233	09	4255	4312	22
06MT039/3	A2	314	01	ROS	062497	2339	EN	44 19.9 N	36 54.5 W	GPS	4233
06MT039/3	A2	315	01	ROS	062597	0337	BE	44 05.8 N	37 43.6 W	GPS	4140
06MT039/3	A2	315	01	ROS	062597	0450	BO	44 05.6 N	37 43.6 W	GPS	4140	11	4136	4190	22
06MT039/3	A2	315	01	ROS	062597	0618	EN	44 05.3 N	37 43.7 W	GPS	4140
06MT039/3	A2	316	01	ROS	062597	1034	BE	43 52.0 N	38 32.8 W	GPS	4044
06MT039/3	A2	316	01	ROS	062597	1150	BO	43 51.9 N	38 32.6 W	GPS	4044	11	4048	4082	22
06MT039/3	A2	316	01	ROS	062597	1327	EN	43 51.6 N	38 32.5 W	GPS	4044
06MT039/3	A2	316	02	ROS	062597	1342	BE	43 51.7 N	38 32.5 W	GPS	4036
06MT039/3	A2	316	02	ROS	062597	1416	BO	43 51.6 N	38 32.4 W	GPS	4036		1991	1999	10
06MT039/3	A2	316	02	ROS	062597	1506	EN	43 51.8 N	38 32.3 W	GPS	4036
06MT039/3	A2	317	01	ROS	062597	2001	BE	43 38.1 N	39 21.6 W	GPS	4658
06MT039/3	A2	317	01	ROS	062597	2024	BO	43 37.9 N	39 21.3 W	GPS	4658		1188	1200	12
06MT039/3	A2	317	01	ROS	062597	2102	EN	43 37.6 N	39 20.8 W	GPS	4658
06MT039/3	A2	317	02	ROS	062597	2106	BE	43 37.4 N	39 20.6 W	GPS	4602
06MT039/3	A2	317	02	ROS	062597	2238	BO	43 36.2 N	39 19.8 W	GPS	4602	08	4816	4726	22
06MT039/3	A2	317	02	ROS	062697	0024	EN	43 35.0 N	39 19.6 W	GPS	4602
06MT039/3	A2	318	01	ROS	062697	0431	BE	43 24.2 N	40 10.2 W	GPS	4780
06MT039/3	A2	318	01	ROS	062697	0453	BO	43 24.3 N	40 10.7 W	GPS	4780	10	1188	1199	12
06MT039/3	A2	318	01	ROS	062697	0530	EN	43 24.5 N	40 10.9 W	GPS	4780
06MT039/3	A2	318	02	ROS	062697	0536	BE	43 24.5 N	40 10.9 W	GPS	4779
06MT039/3	A2	318	02	ROS	062697	0638	BO	43 24.7 N	40 10.5 W	GPS	4779	08	4829	4887	22
06MT039/3	A2	318	02	ROS	062697	0828	EN	43 24.7 N	40 11.9 W	GPS	4779
06MT039/3	A2	319	01	ROS	062697	1209	BE	43 10.4 N	40 59.4 W	GPS	4798
06MT039/3	A2	319	01	ROS	062697	1338	BO	43 10.5 N	41 00.1 W	GPS	4798	10	4832	4883	21
06MT039/3	A2	319	01	ROS	062697	1519	EN	43 10.5 N	41 00.9 W	GPS	4798
06MT039/3	A2	320	01	ROS	062697	1839	BE	42 56.3 N	41 47.3 W	GPS	4809
06MT039/3	A2	320	01	ROS	062697	1900	BO	42 56.0 N	41 47.6 W	GPS	4809		1194	1200	12
06MT039/3	A2	320	01	ROS	062697	1937	EN	42 55.8 N	41 48.7 W	GPS	4809
06MT039/3	A2	320	02	ROS	062697	1943	BE	42 55.2 N	41 49.0 W	GPS	4809
06MT039/3	A2	320	02	ROS	062697	2108	BO	42 55.2 N	41 40.0 W	GPS	4809	09	4850	4921	22
06MT039/3	A2	320	02	ROS	062697	2252	EN	42 54.3 N	41 49.9 W	GPS	4809
06MT039/3	A2	320	04	ROS	062797	0133	BE	42 52.3 N	41 52.4 W	GPS	4880
06MT039/3	A2	320	04	ROS	062797	0236	BO	42 51.4 N	41 53.2 W	GPS	4880		3720	3755	20
06MT039/3	A2	320	04	ROS	062797	0350	EN	42 50.7 N	41 54.1 W	GPS	4880
06MT039/3	A2	321	01	ROS	062797	0715	BE	42 24.7 N	42 35.9 W	GPS	4837
06MT039/3	A2	321	01	ROS	062797	0842	BO	42 41.8 N	42 36.5 W	GPS	4837	08	4903	4955	20
06MT039/3	A2	321	01	ROS	062797	1027	EN	42 41.0 N	42 37.8 W	GPS	4837
06MT039/3	A2	322	01	ROS	062797	1345	BE	42 28.1 N	43 30.0 W	GPS	4832
06MT039/3	A2	322	01	ROS	062797	1423	BO	42 28.4 N	43 24.4 W	GPS	4832		1395	1301	12
06MT039/3	A2	322	01	ROS	062797	1505	EN	42 28.0 N	42 24.7 W	GPS	4832
06MT039/3	A2	322	02	ROS	062797	1523	BE	42 27.9 N	43 25.0 W	GPS	4831
06MT039/3	A2	322	02	ROS	062797	1651	BO	42 27.3 N	43 25.6 W	GPS	4831	13	4887	4955	21
06MT039/3	A2	322	02	ROS	062797	1822	EN	42 27.9 N	43 26.7 W	GPS	4831
06MT039/3	A2	323	01	ROS	062797	2157	BE	42 15.2 N	44 12.2 W	GPS	4865
06MT039/3	A2	323	01	ROS	062797	2231	BO	42 15.6 N	44 12.6 W	GPS	4865		1191	1200	12
06MT039/3	A2	323	01	ROS	062797	2309	EN	42 16.0 N	44 13.3 W	GPS	4865
06MT039/3	A2	323	02	ROS	062897	2319	BE	42 16.0 N	44 13.4 W	GPS	4863
06MT039/3	A2	323	02	ROS	062997	0049	BO	42 16.6 N	44 14.5 W	GPS	4863	10	4915	4983	21
06MT039/3	A2	323	02	ROS	062997	0232	EN	42 17.2 N	44 15.9 W	GPS	4863
06MT039/3	A2	324	01	ROS	062897	0636	BE	42 00.9 N	44 59.9 W	GPS	4814
06MT039/3	A2	324	01	ROS	062897	0702	BO	42 01.6 N	45 00.9 W	GPS	4814		1228	1203	10
06MT039/3	A2	324	01	ROS	062897	0740	EN	42 20.4 N	45 01.4 W	GPS	4814
06MT039/3	A2	324	02	ROS	062897	0755	BE	42 02.2 N	45 01.5 W	GPS	4801
06MT039/3	A2	324	02	ROS	062897	0928	BO	42 04.4 N	45 03.2 W	GPS	4801	09	4937	4914	22
06MT039/3	A2	324	02	ROS	062897	1118	EN	42 05.8 N	45 05.1 W	GPS	4801
06MT039/3	A2	325	01	ROS	062897	1350	BE	42 11.5 N	45 38.4 W	GPS	4720
06MT039/3	A2	325	01	ROS	062897	1413	BO	42 12.2 N	45 38.8 W	GPS	4720		1278	1101	11
06MT039/3	A2	325	01	ROS	062897	1453	EN	42 13.1 N	45 39.3 W	GPS	4720
06MT039/3	A2	325	02	ROS	062897	1454	BE	42 13.3 N	45 39.4 W	GPS	4714
06MT039/3	A2	325	02	ROS	062897	1619	BO	42 14.8 N	45 40.6 W	GPS	4714	09	4835	4802	22
06MT039/3	A2	325	02	ROS	062897	1804	EN	42 17.1 N	45 40.9 W	GPS	4714
06MT039/3	A2	326	01	ROS	062897	2045	BE	42 22.4 N	46 17.6 W	GPS	4660
06MT039/3	A2	326	01	ROS	062897	2140	BO	42 22.3 N	46 17.5 W	GPS	4660		3029	2298	24
06MT039/3	A2	326	01	ROS	062897	2300	EN	42 22.3 N	46 17.4 W	GPS	4660
06MT039/3	A2	326	02	ROS	062897	2333	BE	42 22.3 N	46 17.5 W	GPS	4660
06MT039/3	A2	326	02	ROS	062997	0056	BO	42 22.4 N	46 17.7 W	GPS	4660	12	4742	4733	21
06MT039/3	A2	326	02	ROS	062997	0241	EN	42 22.5 N	46 17.4 W	GPS	4660
06MT039/3	A2	327	01	ROS	062997	0516	BE	42 44.3 N	46 17.5 W	GPS	4660
06MT039/3	A2	327	01	ROS	062997	0630	BO	42 22.4 N	46 17.7 W	GPS	4660	12	4298	4332	22
06MT039/3	A2	327	01	ROS	062997	0753	EN	42 22.5 N	46 17.4 W	GPS	4660
06MT039/3	A2	328	01	ROS	062997	0940	BE	42 36.5 N	47 07.3 W	GPS	4045
06MT039/3	A2	328	01	ROS	062997	1102	BO	42 35.6 N	47 08.1 W	GPS	4045	11	4070	4077	21
06MT039/3	A2	328	01	ROS	062997	1232	EN	42 34.6 N	47 09.0 W	GPS	4045
06MT039/3	A2	329	01	ROS	062997	1452	BE	42 34.7 N	47 26.7 W	GPS	3825
06MT039/3	A2	329	01	ROS	062997	1600	BO	42 44.0 N	47 27.3 W	GPS	3825	10	3846	3879	22
06MT039/3	A2	329	01	ROS	062997	1723	EN	42 43.8 N	47 27.1 W	GPS	3825
06MT039/3	A2	330	01	ROS	062997	1934	BE	42 49.2 N	47 44.1 W	GPS	3741
06MT039/3	A2	330	01	ROS	062997	2036	BO	42 49.4 N	47 43.9 W	GPS	3741	09	3742	3786	22
06MT039/3	A2	330	01	ROS	062997	2206	EN	42 49.8 N	47 43.8 W	GPS	3741
06MT039/3	A2	331	01	ROS	062997	2358	BE	42 54.8 N	48 01.7 W	GPS	3486
06MT039/3	A2	331	01	ROS	063097	0103	BO	42 55.0 N	48 01.7 W	GPS	3486	10	3465	3505	22
06MT039/3	A2	331	01	ROS	063097	0223	EN	42 55.0 N	48 01.2 W	GPS	3486
06MT039/3	A2	332	01	ROS	063097	0506	BE	43 03.1 N	48 37.5 W	GPS	2510
06MT039/3	A2	332	01	ROS	063097	0549	BO	43 03.0 N	48 37.6 W	GPS	2510	10	2473	2494	22
06MT039/3	A2	332	01	ROS	063097	0651	EN	43 03.1 N	48 37.6 W	GPS	2510
06MT039/3	A2	333	01	ROS	063097	0836	BE	43 05.5 N	48 50.5 W	GPS	2072
06MT039/3	A2	333	01	ROS	063097	0913	BO	43 05.3 N	48 50.8 W	GPS	2072	10	2043	2050	22
06MT039/3	A2	333	01	ROS	063097	1014	EN	43 04.9 N	48 51.4 W	GPS	2072
06MT039/3	A2	334	01	ROS	063097	1206	BE	43 08.3 N	48 59.8 W	GPS	1588
06MT039/3	A2	334	01	ROS	063097	1248	BO	43 08.4 N	48 59.7 W	GPS	1588	09	1554	1564	22
06MT039/3	A2	334	01	ROS	063097	1340	EN	43 08.4 N	48 59.4 W	GPS	1588
06MT039/3	A2	335	01	ROS	063097	1518	BE	43 11.7 N	49 09.3 W	GPS	1049
06MT039/3	A2	335	01	ROS	063097	1547	BO	43 11.6 N	49 09.2 W	GPS	1049	09	1022	1029	10
06MT039/3	A2	335	01	ROS	063097	1621	EN	43 11.6 N	49 09.2 W	GPS	1049
06MT039/3	A2	336	01	ROS	063097	1803	BE	43 15.2 N	49 22.2 W	GPS	0570	05	557	560	10
06MT039/3	A2	336	01	ROS	063097	1840	EN	43 15.2 N	49 22.2 W	GPS	0570
06MT039/3	A2	337	01	ROS	063097	1953	BE	43 20.1 N	49 34.9 W	GPS	0097
06MT039/3	A2	337	01	ROS	063097	2000	BO	43 20.1 N	49 34.9 W	GPS	0097		77	0080	7
06MT039/3	A2	337	01	ROS	063097	2009	EN	43 20.1 N	49 34.9 W	GPS	0097
06MT039/3	A2	338	01	ROS	063097	2223	BE	43 30.2 N	50 00.3 W	GPS	0068
06MT039/3	A2	338	01	ROS	063097	2227	BO	43 20.2 N	50 00.3 W	GPS	0068	09	55	0057	5
06MT039/3	A2	338	01	ROS	063097	2235	EN	43 30.3 N	50 00.4 W	GPS	0068

7.4	Leg M39/4
7.4.1	CTD-profile station list and water samples taken from the bottles

CTD-	STATION	DATE		TIME	LATITUDE	LONGITUDE	WATER	PROFILE	COMMENT	CH4-	He,3H,18O  PLANKTON NET	18O FOR
PROFILE	NO.								DEPTH	DEPTH		SAMPLES	SAMPLES	   DEPTH/	LAMONT US
										DBAR				   COMMENT	ENGLAND GB
1	339	1997/07/07	23:03	52ƒ57.22'N	51ƒ21.08'W	2200	2111				   200m
														   culturing
2	341	1997/07/08	23:03	55ƒ19.54'N	53ƒ53.55'W	2405	2398	K2,K6		He(12) 3H(12)		US(4)
											retrieved	18O(5)			GB(20)
3	342	1997/07/09	03:30	55ƒ00.72'N	54ƒ12.57'W	514	482			He(6) 3H(6) 500m	US(4)
													18O(6)	   conservation	GB(5)
4	343	1997/07/09	06:30	55ƒ09.11'N	54ƒ03.86'W	1270	1236			He(7) 3H(7)		US(5)
													18O(6)			GB(10)
	344	1997/07/09	08:35	55ƒ15.96'N	53ƒ57.03'W						   500m
														   conservation
5	346	1997/07/09	12:09	55ƒ33.52'N	53ƒ40.02'W	2898	2887			18O(6)			US(4)
																GB(22)
6	347	1997/07/09	17:06	55ƒ58.01'N	53ƒ15.96'W	3230	3233			He(12) 3H(12)		US(4)
													18O(6)			GB(22)
7	348	1997/07/10	04:02	57ƒ22.74'N	51ƒ47.36'W	3552	3569			He(12) 3H(12)		US(4)
													18O(6)			GB(22)
8	349	1997/07/10	23:30	58ƒ29.63'N	50ƒ33.49'W	3552	3569	K4 retrieved	He(13) 3H(14)		US(4)
													18O(6)			GB(22)
9	350	1997/07/11	13:07	57ƒ44.89'N	49ƒ56.87'W	3595	3611	no LADCP	18O(6)
10	351	1997/07/11		57ƒ00.03'N	49ƒ19.05'W	3644	3651			He(12) 3H(12)
													18O(4)
11	352	1997/07/12	04:18	56ƒ16.48'N	48ƒ41.95'W	3716	3733	K3 retrieved		   500m
														   conservation
12	353	1997/07/12	18:26	55ƒ22.99'N	48ƒ47.86'W	3780	3808			He(12) 3H(12)
													18O(5)
13	354	1997/07/13	03:00	54ƒ32.11'N	49ƒ06.88'W	3746	3766	no LADCP
14	355	1997/07/13	13:43	53ƒ41.13'N	49ƒ26.64'W	3716	3741	K16 deployed,	He(13) 3H(13)		US(4)
											no LADCP	18O(6)
15	357	1997/07/14	01:21	53ƒ26.08'N	50ƒ04.04'W	3533	3565	K10 deployed,	18O(6)	   500m		US(4)
											no LADCP		   conservation
16	358	1997/07/14	06:54	53ƒ16.06'N	50ƒ33.11'W	3189	3192			He(12) 3H(12)		US(4)
													18O(5)
17	359	1997/07/14	14:56	53ƒ07.99'N	50ƒ53.68'W	2903	2902	K9 deployed	18O(7)			US(4)
18	361	1997/07/14	23:18	52ƒ52.44'N	51ƒ30.77'W	1691	1665	K7 deployed	He(9) 3H(9) 500m	US(4)
													18O(7)	   conservation
19	362	1997/07/15	03:37	53ƒ02.50'N	51ƒ05.89'W	2601	2577			He(10)3H(10) 500m	US(4)
													18O(6)	   conservation
20	363	1997/07/15	07:56	52ƒ58.02'N	51ƒ18.00'W	2284	2261	K8 deployed	18O(6)	   500m		US(4)
														   culturing
21	364	1997/07/15	17:02	52ƒ47.93'N	51ƒ45.05'W	550	520			He(5) 3H(5) 500m	US(3)
													18O(6)	   conservation
22	366	1997/07/19	04:02	57ƒ40.13'N	56ƒ32.03'W	3019	3018		   22		   500m		US(4)
														   conservation
23	367	1997/07/20	01:30	57ƒ06.51'N	54ƒ36.11'W	3260	3262	K15+K17	   22		   500m		US(4)
											deployed		   conservation
24	370	1997/07/21	12:54	55ƒ08.92'N	54ƒ04.21'W	1243	1234		    8
25	372	1997/07/21	23:18	55ƒ22.02'N	53ƒ49.10'W	2581	2558	K12	   17
26	373	1997/07/22	03:37	55ƒ42.09'N	53ƒ31.88'W	3020	3009	deployed   22
27	374	1997/07/22	12:03	56ƒ34.07'N	52ƒ39.93'W	3509	3520	K11	   21	He(12)3H(12) 500m	GB(22)
											deployed		   conservation
28	375	1997/07/23	11:26	57ƒ56.12'N	51ƒ10.26'W	3588	3602		   22	He(9) 3H(8)		GB(19)
													SF6(8)
29	376	1997/07/23	19:15	58ƒ27.49'N	50ƒ29.94'W	3552	505	K14	    -		   500m
											deployed		   conservation
30	377	1997/07/24	05:18	59ƒ27.87'N	49ƒ29.79'W	3413	3425		   21				US(4)
																GB(22)
31	378	1997/07/24	10:54	59ƒ53.97'N	49ƒ00.02'W	3110	3113		   21	He(12)3H(12)		US(4)
													18O(4)			GB(22)
32	379	1997/07/24	16:02	60ƒ07.77'N	48ƒ45.76'W	2918	2917		    -	He(10)3H(10) 500m	US(5)
													18O(4)	   conservation	GB(17)
33	380	1997/07/24	20:56	60ƒ18.46'N	48ƒ34.20'W	2747	2741		   21	He(10)3H(10) 500m	US(5)
													18O(4)	   conservation	GB(17)
34	381	1997/07/25	20:45	59ƒ03.07'N	43ƒ30.05'W	1707	1692		   13	He(8)3H(8) 500m		US(5)
													18O(3)	   conservation
35	382	1997/07/26	01:33	58ƒ40.08'N	43ƒ30.03'W	1975	1946		   -	He(8)3H(8)		US(4)
													18O(3)
36	383	1997/07/26	05:55	58ƒ26.27'N	43ƒ30.31'W	2439	2425		   22	He(9)3H(9) 500m		US(3)
													18O(4)	   conservation
37	384	1997/07/26	09:31	58ƒ11.98'N	43ƒ30.02'W	2942	2942		   -				US(4)
38	385	1997/07/26	14:20	57ƒ58.10'N	43ƒ30.14'W	3248	3252		   22	He(11)3H(11) 500m	US(4)
														   conservation
39	386	1997/07/26	18:44	57ƒ37.87'N	43ƒ29.95'W	3417	3426		   20	He(5) 3H(5)
40	387	1997/07/26	23:48	57ƒ10.04'N	43ƒ30.09'W	3449	3478		   -
41	388	1997/07/27	05:15	56ƒ39.91'N	43ƒ29.91'W	3502	3515		   21
42	389	1997/07/27	12:07	55ƒ57.93'N	43ƒ29.94'W	3348	3360		   22	He(3) 3H(3)
43	390	1997/07/27	18:37	55ƒ15.88'N	43ƒ30.02'W	3329	3338		   22	He(8) 3H(8)
44	391	1997/07/28	00:48	54ƒ33.99'N	43ƒ30.00'W	3410	3414		   -
45	392	1997/07/28	07:09	53ƒ51.92'N	43ƒ29.76'W	3625	3668		   21
46	393	1997/07/28	13:41	53ƒ09.96'N	43ƒ30.05'W	3661	3686		   21
47	394	1997/07/28	20:11	52ƒ27.97'N	43ƒ29.87'W	4190	4237		   21	He(9) 3H(9)
48	395	1997/07/29	01:45	51ƒ59.84'N	43ƒ30.00'W	4176	4218		   -
49	396	1997/07/29	07:29	51ƒ30.07'N	43ƒ30.02'W	4234	4289		   22
50	397	1997/07/29	14:07	50ƒ59.92'N	43ƒ29.98'W	4205	4259		   22
51	398	1997/07/29	22:22	50ƒ30.03'N	43ƒ29.99'W	4267	4305		   -
52	399	1997/07/30	05:00	49ƒ59.99'N	43ƒ30.00'W	4259	4310		   21				US(5)
53	400	1997/07/30	10:58	49ƒ40.04'N	43ƒ49.97'W	4070	4111		   22	He(10)3H(10)		US(4)
54	401	1997/07/30	16:52	49ƒ15.65'N	44ƒ14.86'W	3106	3113		   21	He(9)3H(9)		US(4)
													18O(5)
55	402	1997/07/30	22:15	48ƒ15.41'N	44ƒ38.72'W	1573	1548		   19	He(9)3H(7) 500m	US(5)
													18O(6)	   conservation
56	403	1997/07/31	02:29	49ƒ04.30'N	44ƒ25.89'W	2550	2538		   -	He(10)3H(10)
													18O(4)
57	404	1997/07/31	07:49	49ƒ27.79'N	44ƒ03.01'W	3845	3906		   22	He(11)3H(11) 500m
													18O(3)	   conservation
58	405	1997/07/31	18:18	50ƒ12.05'N	41ƒ59.78'W	4349	4412		   21
59	406	1997/08/01	02:00	50ƒ23.97'N	40ƒ29.68'W	4341	4407		   22	He(9)3H(9)
60	407	1997/08/01	10:16	50ƒ35.97'N	39ƒ00.12'W	4136	4192		   21
61	408	1997/08/01	18:11	50ƒ48.01'N	37ƒ29.86'W	4242	4308		   21	He(10)3H(10)
62	409	1997/08/02	02:00	50ƒ59.94'N	35ƒ59.91'W	4328	4380		   -
63	410	1997/08/02	08:54	51ƒ20.11'N	34ƒ59.97'W	3307	3316		   21	He(10)3H(10)
64	411	1997/08/02	13:11	51ƒ40.12'N	35ƒ00.04'W	3828	3859		   -
65	412	1997/08/02	17:30	51ƒ55.02'N	34ƒ59.94'W	3235	3223		   -
66	413	1997/08/02	20:36	52ƒ06.11'N	34ƒ59.92'W	3321	3343		   20	He(8)3H(8)
67	414	1997/08/03	00:13	52ƒ15.17'N	34ƒ59.88'W	3779	3849		   -
68	415	1997/08/07	03:30	52ƒ22.62'N	35ƒ00.02'W	3774	3744		   21	He(9)3H(9)
69	416	1997/08/07	07:18	52ƒ28.03'N	34ƒ59.88'W	2821	2774		   -
70	417	1997/08/07	09:54	52ƒ34.04'N	35ƒ00.22'W	2784	2752		   -	He(6) 3H(6)
71	418	1997/08/07	12:35	52ƒ38.54'N	35ƒ01.18'W	3332	3369		   21	He(9) 3H(9)
72	419	1997/08/07	19:41	53ƒ01.99'N	35ƒ06.84'W	3136	3270		   21	He(6) 3H(6)
73	420	1997/08/07	23:18	53ƒ02.05'N	35ƒ18.94'W	2419	2421		   -
74	421	1997/08/07	01:40	53ƒ02.06'N	35ƒ12.35'W	3109	3108		   -
75	422	1997/08/07	05:11	52ƒ56.67'N	34ƒ58.45'W	3083	3110		   -
76	423	1997/08/07	08:31	52ƒ47.56'N	34ƒ58.11'W	3281	3214		   -
77	424	1997/08/07	11:16	52ƒ43.11'N	34ƒ59.61'W	3531	3537		   -
78	425	1997/08/07	14:37	52ƒ51.97'N	34ƒ57.45'W	3482	3510		   22	He(7) 3H(7)
79	426	1997/08/07	19:33	53ƒ11.62'N	34ƒ51.47'W	2795	2750		   -
80	427	1997/08/07	22:30	53ƒ15.09'N	34ƒ51.76'W	2613	2616		   -	He(8) 3H(8)
81	428	1997/08/07	03:38	53ƒ44.07'N	35ƒ15.08'W	2480	2467		   -	He(4) 3H(4)
82	429	1997/08/07	08:37	54ƒ13.99'N	35ƒ08.96'W	2900	2893		   20	He(7) 3H(7)
83	430	1997/08/07	13:41	54ƒ42.41'N	35ƒ09.77'W	2001	1964		   -
84	431	1997/08/07	17:41	54ƒ59.08'N	34ƒ49.99'W	2460	2434		   -
85	432	1997/08/07	20:18	55ƒ03.44'N	34ƒ49.95'W	2568	2559		   14	He(6) 3H(6)
86	433	1997/08/07	01:15	55ƒ34.03'N	35ƒ06.89'W	2047	2027		   -
87	434	1997/08/07	06:01	56ƒ03.02'N	35ƒ24.80'W	2042	2022		   19
88	435	1997/08/07	10:39	56ƒ31.10'N	35ƒ42.16'W	2270	2246		   -
89	436	1997/08/07	14:09	56ƒ41.12'N	36ƒ02.05'W	2421	2416		   22
90	437	1997/08/07	17:33	56ƒ50.96'N	36ƒ21.90'W	2620	2629		   -
91	438	1997/08/07	21:07	57ƒ02.02'N	36ƒ42.98'W	2422	2423		   22
92	439	1997/08/07	00:35	57ƒ12.01'N	37ƒ03.09'W	2743	2734		   -
93	440	1997/08/07	04:17	57ƒ23.03'N	37ƒ24.04'W	3250	3263		   -
94	441	1997/08/07	08:07	57ƒ32.99'N	37ƒ44.90'W	3222	3216		   22
95	442	1997/08/07	13:58	57ƒ54.00'N	38ƒ26.01'W	3249	3262		   21	He(15) 3H(15)
96	443	1997/08/07	20:18	58ƒ14.00'N	39ƒ05.88'W	3324	3334		   -
97	444	1997/08/08	02:45	58ƒ34.04'N	39ƒ44.76'W	3139	3134		   22
98	445	1997/08/08	07:59	58ƒ48.96'N	40ƒ14.84'W	3088	3091		   -				US(4)
																GB(20)
99	446	1997/08/08	13:22	59ƒ01.93'N	40ƒ39.07'W	2948	2944		   21		   200m		US(4)
														   culturing	GB(18)
100	447	1997/08/08	17:11	59ƒ13.03'N	41ƒ02.90'W	2716	2709		   19				US(4)
																GB(20)
101	448	1997/08/08	20:45	59ƒ23.97'N	41ƒ26.00'W	2359	2342		   6				US(4)
																GB(20)
102	449	1997/08/09	00:03	59ƒ35.08'N	41ƒ50.03'W	1942	1922		   14				US(4)
																GB(18)
103	450	1997/08/09	02:45	59ƒ42.47'N	42ƒ06.94'W	1755	1730		   -				GB(4)

7.5	Leg M39/5
7.5.1	Station Listing

EXPO-	  Section	Stat	Cast	Cast	Date	Time		        Position			Bottom	Meter	Max.	Bottom	No. of	Para	Comments
CODE	  NAME		No.	No.	Type		UTC	Code	Latitude	Longitude	Code	Depth	Wheel	Pres.	Dist.	Btles	meters
06MT39/5  VEINS-6	451	01	ROS/A	081497	2110	BE	64 45.0N	26 39.7W	GPS	 250
06MT39/5  VEINS-6	451	01	ROS/A	081497	2110	BO	64 45.0N	26 39.9W	GPS	 250		 243		10	1-8, 23	Test station
06MT39/5  VEINS-6	451	01	ROS/A	081497	2148	EN	64 45.0N	26 40.0W	GPS	 250
06MT39/5  VEINS-6	451	02	ROS/A	081497	2345	BE	64 45.0N	26 40.0W	GPS	 253
06MT39/5  VEINS-6	451	02	ROS/A	081497	2356	BO	64 45.0N	26 40.1W	GPS	 250		 239		10	1-8,20
06MT39/5  VEINS-6	451	02	ROS/A	081597	0014	EN	64 45.1N	26 40.2W	GPS	 250
06MT39/5  VEINS-6	452	01	ROS/A	081597	0149	BE	64 45.1N	27 14.9W	GPS	 495
06MT39/5  VEINS-6	452	01	ROS/A	081597	0206	BO	64 45.2N	27 14.8W	GPS	 494		 482		 8	1-8,20,23
06MT39/5  VEINS-6	452	01	ROS/A	081597	0226	EN	64 45.2N	27 14.8W	GPS	 492
06MT39/5  VEINS-6	453	01	ROS/A	081597	0406	BE	64 45.3N	27 50.2W	GPS	 902
06MT39/5  VEINS-6	453	01	ROS/A	081597	0431	BO	64 45.4N	27 50.0W	GPS	 893		 902	 9	11	1-8,20,23
06MT39/5  VEINS-6	453	01	ROS/A	081597	0503	EN	64 45.5N	27 49.8W	GPS	 882
06MT39/5  VEINS-6	454	01	ROS/A	081597	0637	BE	64 45.1N	28 25.1W	GPS	1171
06MT39/5  VEINS-6	454	01	ROS/A	081597	0703	BO	64 45.1N	28 24.9W	GPS	1168		1162	11	13	1-8,20
06MT39/5  VEINS-6	454	01	ROS/A	081597	0740	EN	64 45.9N	28 24.9W	GPS	1164
06MT39/5  VEINS-6	455	01	ROS/A	081597	0920	BE	64 45.2N	29 04.9W	GPS	1070
06MT39/5  VEINS-6	455	01	ROS/A	081597	0947	BO	64 45.2N	29 04.8W	GPS	1070	1044	1058	16	13	1-8,20
06MT39/5  VEINS-6	455	01	ROS/A	081597	1028	EN	64 45.0N	29 05.0W	GPS	1071
06MT39/5  VEINS-6	456	01	ROS/A	081597	1209	BE	64 45.1N	29 45.1W	GPS	2139
06MT39/5  VEINS-6	456	01	ROS/A	081597	1251	BO	64 45.2N	29 45.2W	GPS	2139		2141		22	1-10,20
06MT39/5  VEINS-6	456	01	ROS/A	081597	1349	EN	64 45.2N	29 45.4W	GPS	2155
06MT39/5  VEINS-6	457	01	ROS/A	081597	1533	BE	64 45.1N	30 25.2W	GPS	2236
06MT39/5  VEINS-6	457	01	ROS/A	081597	1616	BO	64 45.2N	30 25.1W	GPS	2235		2237	12	22	1-10,20,23,26
06MT39/5  VEINS-6	457	01	ROS/A	081597	1719	EN	64 45.4N	30 24.9W	GPS	2230
06MT39/5  VEINS-6	458	01	ROS/A	081597	1901	BE	65 00.2N	30 42.2W	GPS	1888
06MT39/5  VEINS-6	458	01	ROS/A	081597	1943	BO	65 00.3N	30 42.5W	GPS	1887		1887	12	22	1-10,20
06MT39/5  VEINS-6	458	01	ROS/A	081597	2045	EN	65 00.4N	30 42.9W	GPS	1868
06MT39/5  VEINS-6	459	01	ROS/A	081597	2257	BE	65 16.2N	31 00.0W	GPS	1192
06MT39/5  VEINS-6	459	01	ROS/A	081597	2325	BO	65 16.2N	31 00.2W	GPS	1187		1171	20	14	1-8,20,23,26
06MT39/5  VEINS-6	459	01	ROS/A	081697	0009	EN	65 16.5N	31 01.3W	GPS	1178
06MT39/5  VEINS-6	460	01	ROS/A	081697	0149	BE	65 31.2N	31 15.9W	GPS	 364
06MT39/5  VEINS-6	460	01	ROS/A	081697	0202	BO	65 31.1N	31 16.0W	GPS	 364		 353	10	 8	1-6,20
06MT39/5  VEINS-6	460	01	ROS/A	081697	0223	EN	65 31.1N	31 16.4W	GPS	 364
06MT39/5  VEINS-5	461	01	ROS/A	081697	0937	BE	65 05.1N	34 28.0W	GPS	 316
06MT39/5  VEINS-5	461	01	ROS/A	081697	0949	BO	65 05.1N	34 28.0W	GPS	 316	 296	 302	12	 6	1-10
06MT39/5  VEINS-5	461	01	ROS/A	081697	1007	EN	65 05.1N	34 28.1W	GPS	 316
06MT39/5  VEINS-5	462	01	ROS/A	081697	1203	BE	64 48.9N	34 07.9W	GPS	1028
06MT39/5  VEINS-5	462	01	ROS/A	081697	1224	BO	64 48.8N	34 08.4W	GPS	1029		1009	 8	12	1-8,23,26
06MT39/5  VEINS-5	462	01	ROS/A	081697	1258	EN	64 48.8N	34 09.2W	GPS	1026
06MT39/5  VEINS-5	463	01	MOR	081697	1500	BE	64 30.4N	33 49.9W	GPS	1608					Recovery of mooring "9602"
06MT39/5  VEINS-5	463	01	MOR	081697	1538	EN	64 30.4N	33 50.5W	GPS						(failed)
06MT39/5  VEINS-5	464	01	MOR	081697	1654	BE	64 19.8N	33 39.5W	GPS	1946					Recovery of mooring "9601"
06MT39/5  VEINS-5	464	01	MOR	081697	1705	EN	64 19.8N	33 39.5W	GPS						(failed)
06MT39/5  VEINS-5	464	02	ROS/A	081697	1719	BE	64 19.7N	33 39.5W	GPS	1946
06MT39/5  VEINS-5	464	02	ROS/A	081697	1758	BO	64 19.8N	33 39.6W	GPS	1946	1957	1935	20	22	1-10,23,26
06MT39/5  VEINS-5	464	02	ROS/A	081697	1906	EN	64 19.8N	33 39.3W	GPS	1948
06MT39/5  VEINS-5	463	02	ROS/A	081697	2307	BE	64 30.6N	33 50.7W	GPS	1613
06MT39/5  VEINS-5	463	02	ROS/A	081697	2339	BO	64 30.6N	33 50.9W	GPS	1612	1601	1601	14	18	1-10
06MT39/5  VEINS-5	463	02	ROS/A	081797	0035	EN	64 30.6N	33 51.6W	GPS	1609
06MT39/5  VEINS-5	465	01	ROS/A	081797	0612	BE	64 09.5N	33 25.5W	GPS	2239
06MT39/5  VEINS-5	465	01	ROS/A	081797	0338	BO	64 09.6N	33 26.0W	GPS	2234		2233	10	21	1-10,23,26
06MT39/5  VEINS-5	465	01	ROS/A	081797	0441	EN	64 09.8N	33 26.5W	GPS	2229
06MT39/5  VEINS-5	464	03	MOR	081797	0615	BE	64 20.7N	33 39.0W	GPS	1920					Dredging of mooring "9601"
06MT39/5  VEINS-5	464	03	MOR	081797	1453	EN	64 19.0N	33 40.8W	GPS						(failed)
06MT39/5  VEINS-5	463	03	MOR	081797	1612	BE	64 30.4N	33 50.1W	GPS	1633					Dredging of mooring "9602"
06MT39/5  VEINS-5	463	03	MOR	081797	2329	EN	64 30.2N	33 51.1W	GPS						(failed)
06MT39/5  VEINS-5	466	01	MOR	081897	0734	BE	63 16.8N	35 52.4W	GPS	2200					Recovery of mooring "9604"
06MT39/5  VEINS-5	466	01	MOR	081897	0912	EN	63 16.2N	35 52.8W	GPS
06MT39/5  VEINS-5	467	01	MOR	081897	1008	BE	63 22.4N	36 04.6W	GPS	2200					Recovery of IES
06MT39/5  VEINS-5	467	01	MOR	081897	1117	EN	63 22.0N	36 04.6W	GPS
06MT39/5  VEINS-5	468	01	MOR	081897	1209	BE	63 29.6N	36 16.3W	GPS	2151					Recovery of mooring "9603"
06MT39/5  VEINS-5	468	01	MOR	081897	1321	EN	63 29.4N	36 17.0W	GPS
06MT39/5  VEINS-5	469	01	MOR	081897	1336	BE	63 29.6N	36 18.4W	GPS	1970					Dredging of mooring "9504"
06MT39/5  VEINS-5	469	01	MOR	081897	2153	EN	63 27.9N	36 18.7W	GPS						(failed)
06MT39/5  VEINS-4	470	01	ROS/A	081897	2237	BE	63 34.1N	36 27.2W	GPS	1803
06MT39/5  VEINS-4	470	01	ROS/A	081897	2314	BO	63 34.4N	36 27.5W	GPS	1780	1795	1783	20	 9	1-8,23,26
06MT39/5  VEINS-4	470	01	ROS/A	081897	2359	EN	63 34.4N	36 27.4W	GPS
06MT39/5  VEINS-4	471	01	ROS/A	081997	0114	BE	63 43.0N	36 44.2W	GPS	1632
06MT39/5  VEINS-4	471	01	ROS/A	081997	0147	BO	63 42.9N	36 44.6W	GPS	1633	1612	1628	20	 7	1-8
06MT39/5  VEINS-4	471	01	ROS/A	081997	0223	EN	63 42.8N	36 44.9W	GPS	1644
06MT39/5  VEINS-4	472	01	ROS/A	081997	0324	BE	63 50.0N	36 57.9W	GPS	 358
06MT39/5  VEINS-4	472	01	ROS/A	081997	0336	BO	63 50.0N	36 57.8W	GPS	 355	 336	 346	 9	 5	1-6
06MT39/5  VEINS-4	472	01	ROS/A	081997	0350	EN	63 50.0N	36 57.7W	GPS	 356
06MT39/5  VEINS-4	473	01	MOR	081997	0609	BE	63 38.4N	36 47.4W	GPS	1614					Deployment of mooring "F1"
06MT39/5  VEINS-4	473	01	MOR	081997	0631	EN	63 38.2N	36 47.4W	GPS
06MT39/5  VEINS-4	474	01	MOR	081997	0748	BE	63 33.4N	36 30.3W	GPS	1784					Deployment of mooring "F2"
06MT39/5  VEINS-4	474	01	MOR	081997	0812	EN	63 33.2N	36 30.1W	GPS
06MT39/5  VEINS-4	475	01	MOR	081997	0906	BE	63 28.8N	36 18.0W	GPS	1993					Deployment of mooring "UK1"
06MT39/5  VEINS-4	475	01	MOR	081997	1012	EN	63 28.9N	36 18.1W	GPS						and of IES1
06MT39/5  VEINS-4	476	01	MOR	081997	1117	BE	63 22.0N	36 03.8W	GPS	1993					Deployment of mooring "G1"
06MT39/5  VEINS-4	476	01	MOR	081997	1218	EN	63 22.0N	36 03.9W	GPS						and of IES2
06MT39/5  VEINS-4	477	01	MOR	081997	1330	BE	63 16.8N	35 51.2W	GPS	2364					Deployment of mooring "UK2"
06MT39/5  VEINS-4	477	01	MOR	081997	1344	EN	63 16.6N	35 51.5W	GPS
06MT39/5  VEINS-4	478	01	MOR	081997	1503	BE	63 07.2N	35 32.2W	GPS	2589					Deployment of mooring "G2"
06MT39/5  VEINS-4	478	01	MOR	081997	1518	EN	63 07.0N	35 32.3W	GPS
06MT39/5  VEINS-4	479	01	ROS/A	081997	1648	BE	63 18.1N	35 57.1W	GPS	2313
06MT39/5  VEINS-4	479	01	ROS/A	081997	1732	BO	63 17.9N	35 57.0W	GPS	2313		2317	8	22	1-10,23,26
06MT39/5  VEINS-4	479	01	ROS/A	081997	1847	EN	63 17.9N	35 57.1W	GPS	2314
06MT39/5  VEINS-4	480	01	ROS/A	081997	2048	BE	63 02.0N	35 27.4W	GPS	2658
06MT39/5  VEINS-4	480	01	ROS/A	081997	2138	BO	63 02.1N	35 27.4W	GPS	2656	2663	2661	14	22	1-10
06MT39/5  VEINS-4	480	01	ROS/A	081997	2257	EN	63 02.1N	35 27.3W	GPS	2654
06MT39/5  VEINS-4	481	01	ROS/A	082097	0105	BE	62 45.9N	34 57.1W	GPS	2780
06MT39/5  VEINS-4	481	01	ROS/A	082097	0158	BO	62 46.1N	34 57.6W	GPS	2774	2742	2781	12	21	1-10
06MT39/5  VEINS-4	481	01	ROS/A	082097	0312	EN	62 46.2N	34 57.9W	GPS
06MT39/5  VEINS-4	482	01	ROS/A	082097	0524	BE	62 30.0N	34 27.9W	GPS	2845
06MT39/5  VEINS-4	482	01	ROS/A	082097	0619	BO	62 30.1N	34 28.0W	GPS	2845	2815	2852	14	22	1-10,23,26
06MT39/5  VEINS-4	482	01	ROS/A	082097	0738	EN	62 30.1N	34 28.0W	GPS	2846
06MT39/5		483	01	ROS/A	082097	1105	BE	61 58.0N	35 07.8W	GPS	2901
06MT39/5		483	01	ROS/A	082097	1156	BO	61 58.1N	35 07.8W	GPS	2899	2848	2905	20	22	1-8,23,26	Ros. quality test #1
06MT39/5		483	01	ROS/A	082097	1306	EN	61 58.2N	35 07.8W	GPS	2898
06MT39/5  VEINS-3	484	01	ROS/A	082097	1632	BE	61 26.1N	35 44.1W	GPS	2915
06MT39/5  VEINS-3	484	01	ROS/A	082097	1720	BO	61 26.0N	35 43.9W	GPS	2917		2926	14	22	1-10,20
06MT39/5  VEINS-3	484	01	ROS/A	082097	1855	EN	61 26.0N	35 44.2W	GPS	2917
06MT39/5  VEINS-3	485	01	ROS/A	082097	2120	BE	61 37.8N	36 18.2W	GPS	2804
06MT39/5  VEINS-3	485	01	ROS/A	082097	2214	BO	61 37.9N	36 18.2W	GPS	2800	2775	2806	15	22	1-10,20
06MT39/5  VEINS-3	485	01	ROS/A	082097	2333	EN	61 38.0N	36 18.0W	GPS	2800
06MT39/5  VEINS-3	486	01	ROS/A	082197	0201	BE	61 48.9N	36 53.0W	GPS	2685
06MT39/5  VEINS-3	486	01	ROS/A	082197	0250	BO	61 48.9N	36 53.2W	GPS	2684	2648	2685	19	21	1-10,20
06MT39/5  VEINS-3	486	01	ROS/A	082197	0413	EN	61 49.1N	36 53.6W	GPS	2685
06MT39/5  VEINS-3	487	01	ROS/A	082197	0640	BE	62 01.0N	37 28.3W	GPS	2563
06MT39/5  VEINS-3	487	01	ROS/A	082197	0731	BO	62 01.0N	37 28.3W	GPS	2565	2525	2572	10	22	1-10,20,23
06MT39/5  VEINS-3	487	01	ROS/A	082197	0849	EN	62 01.0N	37 28.3W	GPS	2564
06MT39/5  VEINS-3	488	01	ROS/A	082197	1058	BE	62 11.9N	38 03.1W	GPS	2492
06MT39/5  VEINS-3	488	01	ROS/A	082197	1142	BO	62 12.0N	38 03.0W	GPS	2492	2470	2491	13	22	1-10,20
06MT39/5  VEINS-3	488	01	ROS/A	082197	1251	EN	62 11.9N	38 03.1W	GPS	2491
06MT39/5  VEINS-3	489	01	ROS/A	082197	1459	BE	62 24.0N	38 38.3W	GPS	2267
06MT39/5  VEINS-3	489	01	ROS/A	082197	1543	BO	62 24.2N	38 38.5W	GPS	2270	2201	2256	20	22	1-10,20
06MT39/5  VEINS-3	489	01	ROS/A	082197	1655	EN	62 24.3N	38 38.9W	GPS	2272
06MT39/5  VEINS-3	490	01	ROS/A	082197	1856	BE	62 35.1N	39 13.2W	GPS	2030
06MT39/5  VEINS-3	490	01	ROS/A	082197	1943	BO	62 35.1N	39 13.3W	GPS	2026	2004	2027	 9	20	1-10,20,23,26
06MT39/5  VEINS-3	490	01	ROS/A	082197	2046	EN	62 35.2N	39 13.3W	GPS	2028
06MT39/5  VEINS-3	491	01	ROS/A	082197	2245	BE	62 47.0N	39 49.3W	GPS	1931
06MT39/5  VEINS-3	491	01	ROS/A	082197	2325	BO	62 46.8N	39 49.3W	GPS	1939	1963	1924	30	20	1-10,20
06MT39/5  VEINS-3	491	01	ROS/A	082297	0026	EN	62 46.0N	39 51.2W	GPS	1939
06MT39/5  VEINS-3	492	01	ROS/A	082297	0207	BE	62 51.8N	40 06.7W	GPS	1706
06MT39/5  VEINS-3	492	01	ROS/A	082297	0243	BO	62 51.4N	40 07.0W	GPS	1690	1672	1694	32	18	1-8,20
06MT39/5  VEINS-3	492	01	ROS/A	082297	0337	EN	62 51.1N	40 07.4W	GPS	1666
06MT39/5  VEINS-3	493	01	ROS/A	082297	0514	BE	62 58.0N	40 25.0W	GPS	 218
06MT39/5  VEINS-3	493	01	ROS/A	082297	0525	BO	62 58.0N	40 25.2W	GPS	 232	 212	 215	10	 4	1-10,20
06MT39/5  VEINS-3	493	01	ROS/A	082297	0543	EN	62 57.9N	40 25.4W	GPS	 241
06MT39/5		494	01	ROS	082297	1123	BE	62 08.6N	41 19.2W	GPS	 415
06MT39/5		494	01	ROS	082297	1135	BO	62 08.4N	41 19.1W	GPS	 421		 406		24	1,23	Test CTD "DHI-2"
06MT39/5		494	01	ROS	082297	1200	EN	62 08.2N	41 19.2W	GPS	 433
06MT39/5  VEINS-2	495	01	ROS/A	082297	1817	BE	61 17.7N	41 29.5W	GPS	 445
06MT39/5  VEINS-2	495	01	ROS/A	082297	1831	BO	61 17.7N	41 29.5W	GPS	 456	 465	 458	 9	 6	1-6,9,20
06MT39/5  VEINS-2	495	01	ROS/A	082297	1852	EN	61 17.7N	41 29.5W	GPS	 462
06MT39/5  VEINS-2	496	01	ROS/A	082297	2007	BE	61 14.9N	41 05.2W	GPS	1761
06MT39/5  VEINS-2	496	01	ROS/A	082297	2043	BO	61 14.7N	41 05.6W	GPS	1763	1726	1752	24	16	1-8,20
06MT39/5  VEINS-2	496	01	ROS/A	082297	2133	EN	61 14.5N	41 06.2W	GPS	1760
06MT39/5  VEINS-2	497	01	ROS/A	082397	2316	BE	61 11.1N	40 39.1W	GPS	1892
06MT39/5  VEINS-2	497	01	ROS/A	082497	0001	BO	61 10.9N	40 39.3W	GPS	1897	1827	1878	50	20	1-10,20,23
06MT39/5  VEINS-2	497	01	ROS/A	082497	0059	EN	61 10.5N	40 39.6W	GPS	1818
06MT39/5  VEINS-2	498	01	ROS/A	082397	0306	BE	61 04.0N	40 07.7W	GPS	2193
06MT39/5  VEINS-2	498	01	ROS/A	082397	0349	BO	61 03.9N	40 07.5W	GPS	2196	2160	2185	19	21	1-8,20
06MT39/5  VEINS-2	498	01	ROS/A	082397	0501	EN	61 03.7N	40 07.8W	GPS	2197
06MT39/5  VEINS-2	499	01	ROS/A	082397	0701	BE	60 56.9N	39 27.1W	GPS	2580
06MT39/5  VEINS-2	499	01	ROS/A	082397	0749	BO	60 57.1N	39 27.2W	GPS	2579	2550	2583	 9	20	1-10,20
06MT39/5  VEINS-2	499	01	ROS/A	082397	0904	EN	60 57.2N	39 27.3W	GPS	2578
06MT39/5  VEINS-2	500	01	ROS/A	082397	1110	BE	60 50.1N	38 46.9W	GPS	2816
06MT39/5  VEINS-2	500	01	ROS/A	082397	1201	BO	60 49.9N	38 47.3W	GPS	2814	2765	2820	24	22	1-10,20,23
06MT39/5  VEINS-2	500	01	ROS/A	082397	1315	EN	60 49.7N	38 47.0W	GPS	2813
06MT39/5  VEINS-2	501	01	ROS	082397	1532	BE	60 44.1N	38 06.0W	GPS	2906
06MT39/5  VEINS-2	501	01	ROS	082397	1624	BO	60 43.9N	38 06.0W	GPS	2905		2914	04	23	1-2,20	Test CTD "DHI-2"
06MT39/5  VEINS-2	501	01	ROS	082397	1748	EN	60 43.9N	38 06.2W	GPS	2906
06MT39/5  VEINS-2	501	03	ROS/A	082397	1858	BE	60 43.9N	38 05.8W	GPS	2906
06MT39/5  VEINS-2	501	03	ROS/A	082397	1954	BO	60 43.9N	38 05.8W	GPS	2906	2874	2911	18	21	1-8,23	Ros. quality test #2
06MT39/5  VEINS-2	501	03	ROS/A	082397	2102	EN	60 44.0N	38 06.3W	GPS	2907
06MT39/5		502	01	ROS/A	082497	0023	BE	60 13.9N	38 50.0W	GPS	2877
06MT39/5		502	01	ROS/A	082497	0116	BO	60 13.7N	38 49.6W	GPS	2879	2847	2883	18	26	1-10,20,23
06MT39/5		502	01	ROS/A	082497	0229	EN	60 13.5N	38 49.4W	GPS	2879
06MT39/5		503	01	MOR	082497	0911	BE	59 25.4N	40 35.7W	GPS						Rec. of mooring
06MT39/5		503	01	MOR	082497	1014	EN	59 25.5N	40 35.5W	GPS						"VEINS21"
06MT39/5		504	01	MOR	082497	1042	BE	59 23.0N	40 38.0W	GPS						Rec. of mooring "VEINS2"
06MT39/5		504	01	MOR	082497	1050	EN	59 23.0N	40 38.0W	GPS						(failed)
06MT39/5		505	01	MOR	082497	1342	BE	59 41.3N	41 26.5W	GPS						Rec. and dredging of mooring
06MT39/5		505	01	MOR	082497	2332	EN	59 41.8N	41 26.2W	GPS						"VEINS11" (failed)
																			CTD-Tests:"DHI-1","DHI-2", "NB-3"

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

EXPO-	WOCE	Stat	Cast	Cast	Date	Time		Position				Bottom	Meter	Bottom 	Max.	No. of	Parameters	Comments
CODE	WHP-ID	No.	No.	Type		UTC	Code	Latitude	Longitude	Code	Depth	Wheel	Dist.	Pres.	Btles
06Me039	A1/E	506	01	ROS/A	082597	0709	BE	59ƒ59.8N	42ƒ30.0W	GPS	 193
06Me039	A1/E	506	01	ROS/A	082597	0720	BO	59ƒ59.8N	42ƒ30.1W	GPS	 193	 173	10	 179	 4	1-6,10,20,23,26
06Me039	A1/E	506	01	ROS/A	082597	0735	EN	59ƒ59.8N	42ƒ30.1W	GPS	 193
06Me039	A1/E	507	01	ROS/A	082597	0859	BE	59ƒ58.0N	42ƒ10.4W	GPS	 497
06Me039	A1/E	507	01	ROS/A	082597	0911	BO	59ƒ58.9N	42ƒ10.6W	GPS	 497	 480	 9	 478	 8	1-8,10,20,23,26
06Me039	A1/E	507	01	ROS/A	082597	0933	EN	59ƒ58.0N	42ƒ10.7W	GPS	 497
06Me039	A1/E	508	01	ROS/A	082597	1059	BE	59ƒ55.9N	41ƒ51.0W	GPS	1829
06Me039	A1/E	508	01	ROS/A	082597	1131	BO	59ƒ55.8N	41ƒ51.1W	GPS	1829	1806	11	1821	20	1-10,20
06Me039	A1/E	508	01	ROS/A	082597	1229	EN	59ƒ55.5N	41ƒ51.7W	GPS	1829
06Me039	A1/E	509	01	ROS/A	082597	1406	BE	59ƒ54.1N	41ƒ30.7W	GPS	1902
06Me039	A1/E	509	01	ROS/A	082597	1445	BO	59ƒ53.9N	41ƒ30.8W	GPS	1902	1864	22	1895	21	1-6,20,23,26
06Me039	A1/E	509	01	ROS/A	082597	1540	EN	59ƒ53.6N	41ƒ31.3W	GPS	1902
06Me039	A1/E	510	01	ROS/A	082597	1701	BE	59ƒ52.0N	41ƒ12.0W	GPS	2040
06Me039	A1/E	510	01	ROS/A	082597	1741	BO	59ƒ52.0N	41ƒ12.0W	GPS	2040	2023	10	2038	22	1-10,23
06Me039	A1/E	510	01	ROS/A	082597	1848	EN	59ƒ51.9N	41ƒ12.0W	GPS	2040
06Me039	A1/E	511	01	ROS/A	082597	2041	BE	59ƒ49.1N	40ƒ45.1W	GPS	2598
06Me039	A1/E	511	01	ROS/A	082597	2131	BO	59ƒ49.0N	40ƒ45.6W	GPS	2598	2576	10	2608	21	1-10,23
06Me039	A1/E	511	01	ROS/A	082597	2246	EN	59ƒ49.0N	40ƒ45.9W	GPS	2598
06Me039	A1/E	512	02	ROS/A	082697	0108	BE	59ƒ45.9N	40ƒ13.2W	GPS	2646
06Me039	A1/E	512	02	ROS/A	082697	0211	BO	59ƒ46.0N	40ƒ12.9W	GPS	2646	2612	16	2597	22	1-8,23
06Me039	A1/E	512	02	ROS/A	082697	0317	EN	59ƒ45.9N	40ƒ12.8W	GPS	2646
06Me039	A1/E	513	01	ROS/A	082697	0546	BE	59ƒ40.0N	39ƒ23.8W	GPS	2854
06Me039	A1/E	513	01	ROS/A	082697	0640	BO	59ƒ40.9N	39ƒ23.8W	GPS	2854	2829	 9	2865	22	1-10,23,26
06Me039	A1/E	513	01	ROS/A	082697	0806	EN	59ƒ40.8N	39ƒ23.7W	GPS	2854
06Me039	A1/E	514	01	ROS/A	082697	1032	BE	59ƒ36.0N	38ƒ35.8W	GPS	3012
06Me039	A1/E	514	01	ROS/A	082697	1132	BO	59ƒ36.1N	38ƒ35.9W	GPS	3012	3993	 9	3029	22	1-10,20,23,26
06Me039	A1/E	514	01	ROS/A	082697	1250	EN	59ƒ35.9N	38ƒ35.8W	GPS	3012
06Me039	A1/E	514	02	ROS	082697	1302	BE	59ƒ35.9N	38ƒ35.8W	GPS	3013			3010	15	1-2	CTD "NB-3"
06Me039	A1/E	514	02	ROS	082697	1356	BO	59ƒ35.9N	38ƒ35.9W	GPS	3013
06Me039	A1/E	515	01	ROS/A	082697	1817	BE	59ƒ30.9N	37ƒ37.1W	GPS	3126
06Me039	A1/E	515	01	ROS/A	082697	1920	BO	59ƒ31.0N	37ƒ37.3W	GPS	3126	3106	11	3147	22	1-10,23,26
06Me039	A1/E	515	01	ROS/A	082697	2043	EN	59ƒ31.0N	37ƒ37.4W	GPS	3126
06Me039	A1/E	516	01	ROS/A	082697	2349	BE	59ƒ25.0N	36ƒ39.1W	GPS	3124
06Me039	A1/E	516	01	ROS/A	082797	0045	BO	59ƒ25.1N	36ƒ39.1W	GPS	3124	3059	10	3145	22	1-8,23,26
06Me039	A1/E	516	01	ROS/A	082797	0202	EN	59ƒ25.1N	36ƒ39.1W	GPS	3124
06Me039	A1/E	517	01	ROS/A	082797	0507	BE	59ƒ20.1N	35ƒ40.8W	GPS	3124
06Me039	A1/E	517	01	ROS/A	082797	0606	BO	59ƒ20.0N	35ƒ40.8W	GPS	3124	3102	11	3143	22	1-8,23
06Me039	A1/E	517	01	ROS/A	082797	0730	EN	59ƒ20.0N	35ƒ41.1W	GPS	3124
06Me039	A1/E	518	01	ROS/A	082797	1028	BE	59ƒ14.0N	34ƒ44.0W	GPS	2592
06Me039	A1/E	518	01	ROS/A	082797	1118	BO	59ƒ13.9N	34ƒ44.0W	GPS	2592	2568	 8	2595	22	1-8,23
06Me039	A1/E	518	01	ROS/A	082797	1227	EN	59ƒ13.7N	34ƒ44.1W	GPS	2592
06Me039	A1/E	519	01	ROS/A	082797	1530	BE	59ƒ08.0N	33ƒ45.8W	GPS	2411
06Me039	A1/E	519	01	ROS/A	082797	1615	BO	59ƒ07.9N	33ƒ46.0W	GPS	2411	2399	 9	2421	22	1-10,23,26
06Me039	A1/E	519	01	ROS/A	082797	1729	EN	59ƒ08.0N	33ƒ45.9W	GPS	2411
06Me039	A1/E	520	01	ROS/A	082797	2031	BE	59ƒ02.0N	32ƒ49.2W	GPS	2209
06Me039	A1/E	520	01	ROS/A	082797	2116	BO	59ƒ02.0N	32ƒ48.9W	GPS	2209	2189	11	2214	21	1-8,23
06Me039	A1/E	520	01	ROS/A	082797	2222	EN	59ƒ02.0N	32ƒ48.8W	GPS	2209
06Me039	A1/E	521	01	ROS/A	082897	0037	BE	58ƒ58.1N	32ƒ08.9W	GPS	1609
06Me039	A1/E	521	01	ROS/A	082897	0110	BO	58ƒ58.1N	32ƒ08.9W	GPS	1609	1578	22	1608	16	1-10,23,26
06Me039	A1/E	521	01	ROS/A	082897	0205	EN	58ƒ58.0N	32ƒ08.9W	GPS	1609
06Me039	A1/E	522	01	ROS/A	082897	0429	BE	58ƒ53.9N	31ƒ29.0W	GPS	1558
06Me039	A1/E	522	01	ROS/A	082897	0501	BO	58ƒ54.0N	31ƒ28.9W	GPS	1558	1536	10	1553	17	1-10,23
06Me039	A1/E	522	01	ROS/A	082897	0555	EN	58ƒ53.9N	31ƒ28.9W	GPS	1558
06Me039	A1/E	523	01	ROS/A	082897	0807	BE	58ƒ50.0N	30ƒ50.0W	GPS	1467
06Me039	A1/E	523	01	ROS/A	082897	0838	BO	58ƒ49.9N	30ƒ49.2W	GPS	1467	1457	16	1479	17	1-8,23,26
06Me039	A1/E	523	01	ROS/A	082897	0927	EN	58ƒ49.7N	30ƒ49.2W	GPS	1467
06Me039	A1/E	524	01	ROS/A	082897	1132	BE	58ƒ35.9N	30ƒ22.1W	GPS	1513
06Me039	A1/E	524	01	ROS/A	082897	1204	BO	58ƒ35.9N	30ƒ22.1W	GPS	1513	1498	18	1581	15	1-10,23
06Me039	A1/E	524	01	ROS/A	082897	1251	EN	58ƒ36.0N	30ƒ22.0W	GPS	1513
06Me039	A1/E	525	01	ROS/A	082897	1503	BE	58ƒ21.1N	29ƒ55.9W	GPS	2384
06Me039	A1/E	525	01	ROS/A	082897	1547	BO	58ƒ21.0N	29ƒ56.2W	GPS	2384	2346	27	2390	22	1-10,23,26
06Me039	A1/E	525	01	ROS/A	082897	1659	EN	58ƒ21.2N	29ƒ56.4W	GPS	2384
06Me039	A1/E	526	01	ROS/A	082897	1904	BE	58ƒ06.9N	29ƒ29.0W	GPS	2316
06Me039	A1/E	526	01	ROS/A	082897	1955	BO	58ƒ06.9N	29ƒ28.9W	GPS	2316	2215	19	2304	21	1-10,23
06Me039	A1/E	526	01	ROS/A	082897	2106	EN	58ƒ06.9N	29ƒ28.9W	GPS	2316
06Me039	A1/E	527	01	ROS/A	082897	2322	BE	57ƒ52.0N	28ƒ59.9W	GPS	2374
06Me039	A1/E	527	01	ROS/A	082997	0009	BO	57ƒ52.0N	29ƒ00.0W	GPS	2374	2354	17	2383	18	1-10,23
06Me039	A1/E	527	01	ROS/A	082997	0115	EN	57ƒ51.9N	29ƒ00.0W	GPS	2374
06Me039	A1/E	528	01	ROS/A	082997	0318	BE	57ƒ38.1N	28ƒ37.0W	GPS	2477
06Me039	A1/E	528	01	ROS/A	082997	0407	BO	57ƒ38.0N	28ƒ37.1W	GPS	2477	2461	13	2487	20	1-8,23,26
06Me039	A1/E	528	01	ROS/A	082997	0518	EN	57ƒ37.9N	28ƒ37.0W	GPS	2477
06Me039	A1/E	529	01	ROS/A	082997	0719	BE	57ƒ22.9N	28ƒ10.9W	GPS	2615
06Me039	A1/E	529	01	ROS/A	082997	0810	BO	57ƒ22.9N	28ƒ10.9W	GPS	2615	2615	14	2625	21	1-8,23
06Me039	A1/E	529	01	ROS/A	082997	0929	EN	57ƒ22.9N	28ƒ11.0W	GPS	2615
06Me039	A1/E	530	01	ROS/A	082997	1205	BE	56ƒ59.0N	27ƒ51.9W	GPS	2801
06Me039	A1/E	530	01	ROS/A	082997	1257	BO	56ƒ59.0N	27ƒ52.1W	GPS	2801	2775	17	2819	20	1-8,23
06Me039	A1/E	530	01	ROS/A	082997	1418	EN	56ƒ59.0N	27ƒ52.4W	GPS	2801
06Me039	A1/E	531	01	ROS/A	082997	1658	BE	56ƒ35.2N	27ƒ34.4W	GPS	2758
06Me039	A1/E	531	01	ROS/A	082997	1749	BO	56ƒ35.3N	37ƒ34.8W	GPS	2758	2725	19	2757	22	1-10,23,26
06Me039	A1/E	531	01	ROS/A	082997	1905	EN	56ƒ35.4N	37ƒ35.3W	GPS	2758
06Me039	A1/E	532	01	ROS/A	082997	2146	BE	56ƒ11.0N	27ƒ15.1W	GPS	2779
06Me039	A1/E	532	01	ROS/A	082997	2241	BO	56ƒ11.0N	27ƒ15.0W	GPS	2779	2758	15	2793	22	1-8,23
06Me039	A1/E	532	01	ROS/A	083097	0004	EN	56ƒ11.1N	27ƒ15.1W	GPS	2779
06Me039	A1/E	533	01	ROS/A	083097	0249	BE	55ƒ46.9N	26ƒ56.9W	GPS	2966
06Me039	A1/E	533	01	ROS/A	083097	0344	BO	55ƒ46.9N	26ƒ56.7W	GPS	2966	2959	13	2987	22	1-8,23,26
06Me039	A1/E	533	01	ROS/A	083097	0504	EN	55ƒ47.1N	26ƒ56.6W	GPS	2966
06Me039	A1/E	534	01	ROS/A	083097	0755	BE	55ƒ23.0N	29ƒ38.9W	GPS	3347
06Me039	A1/E	534	01	ROS/A	083097	0858	BO	55ƒ23.0N	29ƒ38.8W	GPS	3347	3333	16	3379	22	1-8,23	Ros. quality
06Me039	A1/E	534	01	ROS/A	083097	1028	EN	55ƒ23.0N	29ƒ38.8W	GPS	3347						test # 3
06Me039	A1/E	534	02	ROS	083097	1203	BE	55ƒ23.0N	26ƒ39.0W	GPS	3340
06Me039	A1/E	534	02	ROS	083097	1238	BO	55ƒ23.1N	26ƒ38.9W	GPS	3340	1760		1782	22	1-6,23
06Me039	A1/E	534	02	ROS	083097	1322	EN	55ƒ23.0N	26ƒ38.9W	GPS	3340
06Me039	A1/E	535	01	ROS/A	083097	1629	BE	55ƒ00.2N	26ƒ21.5W	GPS	3362
06Me039	A1/E	535	01	ROS/A	083097	1733	BO	55ƒ00.1N	26ƒ21.5W	GPS	3362	3351	21		21	1-10,23,26
06Me039	A1/E	535	01	ROS/A	083097	1904	EN	55ƒ00.2N	26ƒ21.4W	GPS	3362
06Me039	A1/E	536	01	ROS/A	083097	2152	BE	54ƒ36.1N	26ƒ03.7W	GPS	3409
06Me039	A1/E	536	01	ROS/A	083097	2257	BO	54ƒ36.0N	26ƒ03.7W	GPS	3409	3394	14	3441	22	1-8,23
06Me039	A1/E	536	01	ROS/A	083197	0022	EN	54ƒ35.9N	26ƒ03.6W	GPS	3409
06Me039		537	01	ROS/A	083197	0205	BE	54ƒ34.0N	25ƒ36.9W	GPS	2421
06Me039		537	01	ROS/A	083197	0247	BO	54ƒ33.9N	25ƒ36.9W	GPS	2421	2388	16	2412	20	1-6,23	Eriador-Hecate
06Me039		537	01	ROS/A	083197	0358	EN	54ƒ33.7N	25ƒ37.3W	GPS	2421						--Section
06Me039	A1/E	538	01	ROS/A	083197	0556	BE	54ƒ18.9N	25ƒ51.8W	GPS	3050
06Me039	A1/E	538	01	ROS/A	083197	0657	BO	54ƒ18.9N	25ƒ52.1W	GPS	3050	3065	10	3097	21	1-8,23
06Me039	A1/E	538	01	ROS/A	083197	0820	EN	54ƒ19.0N	25ƒ52.2W	GPS	3050
06Me039		539	01	ROS/A	083197	1052	BE	54ƒ04.0N	26ƒ13.8W	GPS	3400
06Me039		539	01	ROS/A	083197	1155	BO	54ƒ03.8N	26ƒ13.7W	GPS	3400	3448	12	3431	21	1-8,23,26
06Me039		539	01	ROS/A	083197	1318	EN	54ƒ03.5N	26ƒ13.5W	GPS	3400
06Me039		540	01	ROS/A	083197	1826	BE	53ƒ33.1N	26ƒ56.9W	GPS	2666
06Me039		540	01	ROS/A	083197	1919	BO	53ƒ33.4N	26ƒ57.2W	GPS	2666	2651	11	2681	22	1-8,23
06Me039		540	01	ROS/A	083197	2030	EN	53ƒ33.4N	26ƒ57.7W	GPS	2666
06Me039		541	01	ROS/A	090197	0136	BE	53ƒ01.9N	27ƒ39.8W	GPS	3632
06Me039		541	01	ROS/A	090197	0245	BO	53ƒ01.8N	27ƒ39.9W	GPS	3632	3590	41	3645	21	1-8,23,26
06Me039		541	01	ROS/A	090197	0426	EN	53ƒ01.8N	27ƒ39.9W	GPS	3632
06Me039		542	01	ROS/A	090197	0836	BE	52ƒ32.0N	28ƒ22.7W	GPS	3683
06Me039		542	01	ROS/A	090197	0944	BO	52ƒ32.1N	28ƒ22.4W	GPS	3683	3680	12	3731	22	1-10,23
06Me039		542	01	ROS/A	090197	1120	EN	52ƒ32.0N	28ƒ22.3W	GPS	3683
06Me039		543	01	ROS/A	090197	1527	BE	52ƒ00.9N	29ƒ05.0W	GPS	3793
06Me039		543	01	ROS/A	090197	1636	BO	52ƒ00.9N	29ƒ05.0W	GPS	3793	3790	 9	3846	22	1-8,23
06Me039		543	01	ROS/A	090197	1813	EN	52ƒ01.1N	29ƒ05.0W	GPS	3793
06Me039		544	01	ROS/A	090197	2053	BE	51ƒ42.9N	29ƒ30.2W	GPS	1839
06Me039		544	01	ROS/A	090197	2127	BO	51ƒ42.9N	29ƒ30.1W	GPS	1839	1739	17	1756	17	1-6,20,23
06Me039		544	01	ROS/A	090197	2221	EN	51ƒ42.9N	29ƒ30.3W	GPS	1839
06Me039		545	01	ROS/A	090297	0014	BE	51ƒ51.9N	29ƒ15.9W	GPS	3198
06Me039		545	01	ROS/A	090297	0110	BO	51ƒ52.0N	29ƒ15.7W	GPS	3198	3170	20	3211	20	1-8,23
06Me039		545	01	ROS/A	090297	0232	EN	51ƒ51.8N	29ƒ15.5W	GPS	3198
06Me039		546	01	ROS/A	090297	0544	BE	52ƒ17.0N	28ƒ42.0W	GPS	3121
06Me039		546	01	ROS/A	090297	0652	BO	52ƒ17.0N	28ƒ42.1W	GPS	3121	3159	 9	3196	21	1-8,23
06Me039		546	01	ROS/A	090297	0818	EN	52ƒ17.1N	28ƒ41.9W	GPS	3121
06Me039		547	01	ROS/A	090297	1156	BE	52ƒ46.9N	28ƒ01.8W	GPS	3464
06Me039		547	01	ROS/A	090297	1301	BO	52ƒ47.0N	28ƒ01.9W	GPS	3464	3454	18	3498	22	1-8,23
06Me039		547	01	ROS/A	090297	1427	EN	52ƒ47.0N	28ƒ01.8W	GPS	3464
06Me039		548	01	ROS/A	090297	1837	BE	53ƒ18.0N	27ƒ19.0W	GPS	3618
06Me039		548	01	ROS/A	090297	1947	BO	53ƒ18.0N	27ƒ19.1W	GPS	3618	3610	 8	3664	22	1-8,23
06Me039		548	01	ROS/A	090297	2118	EN	53ƒ18.0N	27ƒ19.3W	GPS	3618
06Me039		549	01	ROS/A	090397	0132	BE	53ƒ47.9N	26ƒ34.9W	GPS	3713
06Me039		549	01	ROS/A	090397	0235	BO	53ƒ47.8N	26ƒ35.1W	GPS	3713	3709	20	3754	22	1-8,23
06Me039		549	01	ROS/A	090397	0413	EN	53ƒ47.5N	26ƒ35.6W	GPS	3713
06Me039	A1/E	550	01	ROS/A	090397	0746	BE	53ƒ59.9N	25ƒ37.9W	GPS	3252
06Me039	A1/E	550	01	ROS/A	090397	0848	BO	53ƒ60.0N	25ƒ38.0W	GPS	3252	3229	16	3274	21	1-8,23
06Me039	A1/E	550	01	ROS/A	090397	1009	EN	53ƒ59.9N	25ƒ37.9W	GPS	3252
06Me039	A1/E	551	01	ROS/A	090397	1211	BE	53ƒ41.8N	25ƒ24.7W	GPS	3603
06Me039	A1/E	551	01	ROS/A	090397	1318	BO	53ƒ41.4N	25ƒ24.4W	GPS	3603	3587	22	3638	22	1-10,23
06Me039	A1/E	551	01	ROS/A	090397	1452	EN	53ƒ41.4N	25ƒ24.4W	GPS	3603
06Me039	A1/E	552	01	ROS/A	090397	1717	BE	53ƒ33.0N	24ƒ45.7W	GPS	3621
06Me039	A1/E	552	01	ROS/A	090397	1825	BO	53ƒ32.9N	24ƒ45.7W	GPS	3621	3614	10	3663	20	1-8,23
06Me039	A1/E	552	01	ROS/A	090397	1959	EN	53ƒ32.9N	24ƒ45.9W	GPS	3621
06Me039	A1/E	553	01	ROS/A	090397	2238	BE	53ƒ22.9N	24ƒ06.6W	GPS	3674
06Me039	A1/E	553	01	ROS/A	090397	2347	BO	53ƒ22.7N	24ƒ06.9W	GPS	3674	3663	18	3712	20	1-10
06Me039	A1/E	553	01	ROS/A	090497	0118	EN	53ƒ22.2N	24ƒ08.4W	GPS	3674
06Me039	A1/E	554	01	ROS/A	090497	0402	BE	53ƒ14.0N	23ƒ27.9W	GPS	3725
06Me039	A1/E	554	01	ROS/A	090497	0514	BO	53ƒ13.9N	23ƒ28.3W	GPS	3725	3731	10	3776	22	1-8,23,26
06Me039	A1/E	554	01	ROS/A	090497	0652	EN	53ƒ14.0N	23ƒ28.2W	GPS	3725
06Me039	A1/E	555	01	ROS	090497	1011	BE	53ƒ05.0N	22ƒ49.8W	GPS	4000
06Me039	A1/E	555	01	ROS	090497	1127	BO	53ƒ05.0N	22ƒ49.9W	GPS	4000	4005	16	4064	21	1-8,23,26
06Me039	A1/E	555	01	ROS	090497	1300	EN	53ƒ05.0N	22ƒ49.9W	GPS	4000
06Me039	A1/E	555	02	ROS	090497	1511	BE	53ƒ04.8N	22ƒ50.5W	GPS	3972
06Me039	A1/E	555	02	ROS	090497	1615	BO	53ƒ04.7N	22ƒ50.3W	GPS	3972	3987	15	4047	24	1-6,SF6
06Me039	A1/E	555	02	ROS	090497	1752	EN	53ƒ04.8N	22ƒ50.1W	GPS	3972
06Me039	A1/E	556	01	ROS	090497	2025	BE	52ƒ55.0N	22ƒ11.0W	GPS	4022
06Me039	A1/E	556	01	ROS	090497	2140	BO	52ƒ54.9N	22ƒ11.3W	GPS	4022	4021	18	4080	22	1-10
06Me039	A1/E	556	01	ROS	090497	2314	EN	52ƒ54.8N	22ƒ11.1W	GPS	4022
06Me039	A1/E	557	01	ROS	090597	0143	BE	52ƒ45.9N	21ƒ33.0W	GPS	3877
06Me039	A1/E	557	01	ROS	090597	0300	BO	52ƒ45.7N	21ƒ32.9W	GPS	3877	3818	19	3931	23	1-8,23
06Me039	A1/E	557	01	ROS	090597	0431	EN	52ƒ45.8N	21ƒ32.8W	GPS	3877
06Me039	A1/E	558	01	ROS/A	090597	0728	BE	52ƒ36.8N	20ƒ55.0W	GPS	3709
06Me039	A1/E	558	01	ROS/A	090597	0837	BO	52ƒ36.7N	20ƒ55.4W	GPS	3709	3698	17	3747	22	1-8,23
06Me039	A1/E	558	01	ROS/A	090597	1012	EN	52ƒ36.4N	20ƒ55.5W	GPS	3709
06Me039		559	01	ROS/A	090597	1414	BE	52ƒ01.9N	21ƒ21.1W	GPS	4318
06Me039		559	01	ROS/A	090597	1536	BO	52ƒ01.6N	21ƒ20.9W	GPS	4318	4333	10	4399	22	1-8,10,23 Lorien Bank -- E. Thulean Section
06Me039		559	01	ROS/A	090597	1722	EN	52ƒ01.4N	21ƒ21.3W	GPS	4318
06Me039		560	01	ROS/A	090597	1923	BE	51ƒ42.8N	21ƒ36.1W	GPS	2712
06Me039		560	01	ROS/A	090597	2020	BO	51ƒ42.7N	21ƒ36.3W	GPS	2712	2694	12	2727	21	1-6,23
06Me039		560	01	ROS/A	090597	2145	EN	51ƒ42.4N	21ƒ36.6W	GPS	2712
06Me039		561	01	ROS/A	090697	0206	BE	52ƒ18.9N	21ƒ08.8W	GPS	3774
06Me039		561	01	ROS/A	090697	0314	BO	52ƒ18.4N	21ƒ09.0W	GPS	3774	3769	20	3801	22	1-8,23
06Me039		561	01	ROS/A	090697	0448	EN	52ƒ18.3N	21ƒ09.4W	GPS	3774
06Me039		562	01	ROS/A	090697	0850	BE	52ƒ55.0N	20ƒ41.0W	GPS	2901
06Me039		562	01	ROS/A	090697	0943	BO	52ƒ55.0N	20ƒ41.0W	GPS	2901	2888	10	2925	22	1-8,23
06Me039		562	01	ROS/A	090697	1100	EN	52ƒ55.0N	20ƒ41.0W	GPS	2901
06Me039		563	01	ROS/A	090697	1506	BE	53ƒ31.0N	20ƒ13.0W	GPS	2151
06Me039		563	01	ROS/A	090697	1544	BO	53ƒ30.9N	20ƒ13.2W	GPS	2151	2151	19	2171	22	1-8,23
06Me039		563	01	ROS/A	090697	1655	EN	53ƒ31.0N	20ƒ13.6W	GPS	2151
06Me039	A1/E	564	01	ROS/A	090897	0434	BE	52ƒ24.0N	20ƒ09.8W	GPS	2883
06Me039	A1/E	564	01	ROS/A	090897	0528	BO	52ƒ23.9N	20ƒ09.9W	GPS	2883	2877	11	2916	22	1-10,20,23,26
06Me039	A1/E	564	01	ROS/A	090897	0651	EN	52ƒ24.0N	20ƒ09.9W	GPS	2883
06Me039	A1/E	565	01	ROS/A	090897	0938	BE	52ƒ20.0N	19ƒ19.9W	GPS	3670
06Me039	A1/E	565	01	ROS/A	090897	1045	BO	52ƒ20.1N	19ƒ20.0W	GPS	3670	3666	12	3705	22	1-10,20,23,26
06Me039	A1/E	565	01	ROS/A	090897	1206	EN	52ƒ20.1N	19ƒ20.1W	GPS	3670
06Me039	A1/E	566	01	ROS/A	090897	1455	BE	52ƒ20.0N	18ƒ29.7W	GPS	4309
06Me039	A1/E	566	01	ROS/A	090897	1613	BO	52ƒ20.0N	18ƒ29.8W	GPS	4309	4325	21	4392	21	1-10,20,23
06Me039	A1/E	566	01	ROS/A	090897	1747	EN	52ƒ20.1N	18ƒ30.1W	GPS	4309
06Me039	A1/E	567	01	ROS/A	090897	2040	BE	52ƒ20.0N	17ƒ40.0W	GPS	4217
06Me039	A1/E	567	01	ROS/A	090897	2154	BO	52ƒ20.0N	17ƒ40.0W	GPS	4217	4231	15	4257	22	1-10,20,23,26
06Me039	A1/E	567	01	ROS/A	090897	2326	EN	52ƒ20.0N	17ƒ40.0W	GPS	4217
06Me039	A1/E	568	01	ROS/A	090997	0222	BE	52ƒ20.0N	16ƒ49.7W	GPS	3822
06Me039	A1/E	568	01	ROS/A	090997	0331	BO	52ƒ20.1N	16ƒ49.5W	GPS	3822	3824	21	3882	22	1-10,20,23
06Me039	A1/E	568	01	ROS/A	090997	0502	EN	52ƒ20.2N	16ƒ49.6W	GPS	3822
06Me039	A1/E	569	01	ROS/A	090997	0753	BE	52ƒ19.9N	16ƒ00.1W	GPS	3375
06Me039	A1/E	569	01	ROS/A	090997	0905	BO	52ƒ20.2N	16ƒ00.3W	GPS	3375	3382	13	3423	22	1-10,20,23,26
06Me039	A1/E	569	01	ROS/A	090997	1025	EN	52ƒ20.1N	16ƒ00.6W	GPS	3375
06Me039	A1/E	570	01	ROS/A	090997	1218	BE	52ƒ20.0N	15ƒ30.1W	GPS	2870
06Me039	A1/E	570	01	ROS/A	090997	1310	BO	52ƒ20.0N	15ƒ30.6W	GPS	2870	2848	16	2876	22	1-6,23
06Me039	A1/E	570	01	ROS/A	090997	1412	EN	52ƒ20.0N	15ƒ30.8W	GPS	2870
06Me039	A1/E	571	01	ROS/A	090997	1527	BE	52ƒ20.0N	15ƒ14.8W	GPS	1394
06Me039	A1/E	571	01	ROS/A	090997	1600	BO	52ƒ20.1N	15ƒ15.1W	GPS	1394		20	1388	15	1-8,10,20
06Me039	A1/E	571	01	ROS/A	090997	1642	EN	52ƒ20.0N	15ƒ15.3W	GPS	1394
06Me039	A1/E	572	01	ROS/A	090997	1754	BE	52ƒ19.9N	14ƒ59.8W	GPS	 930
06Me039	A1/E	572	01	ROS/A	090997	1817	BO	52ƒ19.9N	14ƒ59.6W	GPS	 930	 914	10	 922	12	1-6,20
06Me039	A1/E	572	01	ROS/A	090997	1845	EN	52ƒ20.0N	14ƒ59.5W	GPS	 930
06Me039	A1/E	573	01	ROS/A	090997	1952	BE	52ƒ19.9N	14ƒ45.1W	GPS	 462
06Me039	A1/E	573	01	ROS/A	090997	2005	BO	52ƒ20.0N	14ƒ45.1W	GPS	 462	 451	13	 451	 8	1-8,20
06Me039	A1/E	573	01	ROS/A	090997	2024	EN	52ƒ20.1N	14ƒ45.1W	GPS	 462
06Me039	A1/E	574	01	ROS/A	090997	2141	BE	52ƒ20.0N	14ƒ30.0W	GPS	 370
06Me039	A1/E	574	01	ROS/A	090997	2152	BO	52ƒ20.0N	14ƒ29.9W	GPS	 370	 360	11	 360	 6	1-6,20
06Me039	A1/E	574	01	ROS/A	090997	2207	EN	52ƒ20.0N	14ƒ29.9W	GPS	 370



8	CONCLUDING REMARKS AND ACKNOWLEDGEMENTS

The 39th voyage of RV METEOR served a multi-disciplinary group of projects in the 
North Atlantic Ocean. All groups and institution involved helped to support the 
coordination work. Special thanks is expressed to Deutsche Forschungsgemeinschaft 
(DFG) for making available the ship time and funding for cruise M39. Projects of 
the Sonderforschungsbereich 460 were also founded by the DFG.

The principle investigators further acknowledge financial support received from the 
German Ministry of Education and Research (BMBF) through various grants under the 
German WOCE programs for preparation and evaluation of the research carried out on 
cruise M39.

It is our particular pleasure to thank captains and crew of all cruise legs for the 
flexible friendly and very helpful attitude during deployments of the complex 
moored arrays and the various kinds of shipboard measurement programs.



9    CFC REPORTS

9.1  WOCE LINE A02_06MT39_2
     1997.MAY.15 - 1997.JUN.6


CFC PIs: Monika Rhein and Olaf Plähn
         Institut für Meereskunde, 24105 Kiel, Germany
     now at:
         Institut für Ostseeforschung, 18119 Rostock, Germany
         email: monika.rhein@io-warnemuende.de
                oplaehn@ifm.uni-kiel.de

CFC-Lab: Martina Elbrächter and Kristin BahrenfussInstitut für Meereskunde
                24105 Kiel, Germany
         email: melbraechter@ifm.uni-kiel.de

Region:  Subpolar East Atlantic; 51°N - 62°N, 38°W - 12°W


SAMPLE COLLECTION AND TECHNIQUE

The water samples were drawn from pre-cleaned 10 L Niskin bottles with gas tight 
100 mL glass syringes (Becton and Dickinson). CFCs were measured on board with a 
GC-ECD (Electron Capture Detector) technique first described by Bullister and 
Weiss [1988]. About 15-25 mL were   transferred to a purge and trap unit. The 
CFCs were separated on a packed stainless steel column filled with Porasil C and 
detected with an ECD. The carrier gas is ECD pure Nitrogen, which was 
additionally cleaned by molsieves (13X mesh 80/100).

All '0' rings and valves as well as the nylon stopcocks (of the syringes) were 
removed and washed in isopropanol and baked in a vacuum oven for 24 hours prior 
the cruise. The Niskin bottles were cleaned with isopropanol. The rubber bands 
on all bottles were replaced by stainless steel springs. The personnel for all 
water sampling and handling procedures at the bottles wore one-way gloves to 
protect the valves from grease.

A standard gas (ALM 0383034, 120.5 ppt CFC-12, 266.4 ppt CFC-11, kindly provided 
by D. NVallace, IfM Kiel) was used to convert the ECD signal in concentrations. 
The CFC concentrations are reported in pmol kg-I on the S1093 scale (R. Weiss, 
SIO).


Figure 1: Accuracy (%) of the, CFC-12 and CFC-11 replicate samples against 
          Profile number


PERFORMANCE

During leg M39/2, the Kiel CFC system worked continuously and about 1200 water 
samples on 66 stations had been analysed. The survey was dedicated to the 
circulation of the deep water masses. During periods of dense station spacing, 
sampling was focused on the water column below 800 m depth.

Accuracy was checked by analysing about 350 water samples twice. It was found to 
be 0.7%, for CFC-11 and 0.8% for CFC-12 (Figure 1). The system blanks for CFC11 
and CFC-12 were negligible. The blanks were determined by degassing CFC free 
water, produced by purging ECD clean Nitrogen permanently throngh 5 L seawater. 
The blanks were lower than 0.004 pmol kg-1 for both components. As no CFC poor 
water is available in the subpolar North Atlantic, the Niskin bottle blanks 
could not be checked directly. We could only estimate an upper bound of the 
blank by the measurements in the deep Rockall Trough, where CFC-poor water is 
found. On our cruises in the Northern Indian Ocean and the Tropical Atlantic, 
where CFC free deep water is available, the blanks of the pre-cleaned bottles 
were lower than 0.003 pmol kg-1 for both components (CFC-12 and CFC-11).

The temporal evolution of the ECD efficiency is shown in Figure 2. The 
efficiency for the CFC-12 component was very stable. The efficiency of CFC-11 
was more variable, especially between profile 50-60 (stations 245-255). Major 
changes occured, when the drying agent (magnesimperchlorate) in the purge and 
trap unit was exchanged or the molsieves had to be baked and therefore 
exchanged. To correct the temporal drift, a calibration curve with 4-6 different 
standard gas volumes was carried out before and after each station, the change 
between these curves is thought to occur linear with time.


Figure 2: Temporal evolution of the efficiency of the ECD (mVs/mg standard) for 
          the 5 mL sample volume.


CFC concentrations are calculated by using the two neighboured calibration 
points, assuming that the calibration curve is linear between these points.

At first we used sample volumes, precalibrated by the company (Machery and  
Nagel, Germany) for the analysis of standard gas. It turned out that these 
volumes could be off by more than 5%, affecting the precision of the measured 
oceanic CFC concentrations by the same amount. Therefore, in 1998, the volumes 
for the gas standard measurements (nominal 2 mL and 5 mL) were calibrated 
against two 'master' volumes by D. Wallace's group (IfM Kiel), who had done this 
task also for the C02 community. CFC measurements of the air inside the vessel 
and especially in the lab were carried out frequently in order to check for 
contamination. In general, the CFC concentrations in both places were only a few 
percent higher than in clean air. Clean air measurements were carried out 
occasionally by sampling air from the ship's compass bridge or forecastle.


PROBLEMS

At some stations, the CFC-12 peak was disturbed by a high N20 level of the 
samples.


Figure 3: Cruie Meteor 3912, all CFC-11 data [pmol kg-1] versus depth.
Figure 4: All CFC-11/CFC-12 ratios measured during Meteor CFC-11 concentrations 
          larger than, I pmol kg-1 are, marked by circles.
Figure 5: CFC-11 surface saturation relative to the concentration in the 
          Atmosphere (266 pptV), plus: < 95%, circle: 95-100%, cross: 100-105%, 
          dot: > 105%.


COMMENTS

Leg 2 is the first part of the Kiel CFC data set of the Meteor 39 cruise. Along 
the first section (Ireland- Reykjanes- Ridge) the lowest CFC concentrations  - 
less than 1 pmol kg-1 for CFC-11- were measured at the bottom of the Rockall 
Trough (Figure 3). Along the eastern flank of the Reykjanes-Ridge, TSOW spreads 
southward, with a mean CFC-11 signal of 2.5 pmol kg-I at 60oN. Along its pathway 
the concentration decreases, and perpendicular to the flow direction, the 
concentration gradient increase. In the flow through the Charly- Gibbs- Fracture 
Zone (CGFZ), the CFC-11 concentration was 2.3 pmol kg-1 in the core of the TSOW, 
at the northern edge of the fracture zone. The largest CFC signal of the LSW was 
measured southwest of the CGFZ with concentrations of more than 3.2 pmol kg-'. 
Spreading eastwards this strong signal decreases steadily [Sy et al., 1997]. In 
the density range between 27.75 and 27.78, the average CFC-11 concentration was 
less than 2 pmol kg-1 in the Rockall Trough and about 2.7 pmol kg-1 in the 
Iceland Basin. Along the 51oN-section the LSW signal was observed east of 15oW, 
marked by oxygen and CFC-11 maxima. The mean CFC ratio within a depth-range of 
500-2500 m is about 2.1 (Figure 4), which is similar to the observation during 
the other cruises in this region. The accuracy of the ratio is less than 0.1 if 
the CFC-11 concentration is larger than 0.15 pmol kg-1. The scatter increases 
considerably when the CFC concentrations become smaller.

The surface saturation of CFC-11 relative to the atmospheric value of 266 pptV 
varied between 93-107% (Figure 5). The supersaturations in the eastern part of 
the 51oN-section are presumably caused by recent mixing of cold water from the 
north with warmer water from the south, while the air sea gas exchange had not 
enough time to equilibrate with the atmosphere. Similar high saturations were 
found off Newfoundland, where the cold Labrador Current meets the warmer North 
Atlantic Current [Körtzinger et al., 1999].


o Note, that this is not a WOCE cruise, and the data are not in the WOCE format!
o The data are only for personal use. If yon want them for other purposes, you 
  need the consent of Monika Rhein.


REFERENCES

Bullister J. L. and R. F. Weiss (1988). Determination of CCl3F and CCl2F2 in 
     seawater and air. Deep-Sea Res., 35, p. 839-853.
Körtzinger, A., M. Rhein, and L. Mintrop (1999). Anthropogenic C02 and CFCs in 
     the North Atlantic Ocean - A comparison of man-made tracer. Geophys. 
     Res. Left., 26, p. 2065-2068.
Sy, A., M. Rhein, J.R.N. Lazier, K.P. Koltermann, J. Meincke, A. Putzka, and  
     M. Bersch (1997). Surprisingly Rapid Cooling of Newly Formed 
     Intermediate Waters Across the North Atlantic Ocean.  Nature, 386, p. 
     675-679.


Appendix

the station file 'meteor392.sum' includes:
1 station number
2 year
3 month
4 day
5 hour: minutes in decimal system
6 latitude: minutes in decimals
7 longitude: minutes in decimals
8 water depth (m)
9 depth of CTD profile (m)

the bottle file 'meteor392.sea' includes:
1 station number
2 bottle number
3 depth (dbar)
4 in-situ temperature (IC)
5 salinity (psu)
6 CFC-12 (pmol kg-1
7 CFC-11 (pmol kg-1
8 WOCE quality flag for CFC-12 and CFC-11


TECHNICAL  INFORMATION

Gas chromatograph                   Shimadzu GC 14
GC column                           stainless steel, packed with Porasil C
Cooling trap                        with Porapak T and Porasil C
Trap temperatures                   -30-C, 100oC
Column temperature                  70oC, isothermal
ECD temperature                     300oC
Electron Capture Detector           Shimadzu
Software for chromatogram analysis  Shimadzu CLASS LC 10 (1.63)
Standard gas                        ALM 0383034, D. Wallace, PMEL
Precision                           CFC-11: 3%, CFC-12: 3%
Accuracy                            CFC-11: 0.7%, CFC-12: 0.8%
Blanks                              negligible



9.2	WOCE LINE A02_06MT39_3
	1997.JUN.11 - 1997.JUL.03

The data reported here were acquired by Prof. Dr. Roether
         Institut für Umweltphysik
         Tracer Ozeanographie
         University Bremen
         P.O.Box 330 440
         28334 Bremen  GERMANY
         Tel.:  +421 218 3511
         Email: wroether@physik.uni-bremen.de

For questions about the data please contact Uli Fleischmann
         Institut für Umweltphysik
         Tracer Ozeanographie
         University Bremen
         P.O.Box 330 440
         28334 Bremen  GERMANY
         Tel.:  +421 218 4317
         Email: ufleisch@physik.uni-bremen.de

Region:  48°N on the WHP section A2; 42°N - 49°N, 10°W - 50°W


CHLOROFLUOROCARBONS:

CFC11, CFC12, CFC113 and CCL4 have been measured on the cruise. A capillary 
column (DBVRX, ID 0.45mm) was used. A Bremer standard was used that has been 
calibrated against the SIO93 scale using standard gas from Ray Weiss. CFC 
measurements have been assigned individual errors. The overall performance is 
described below:

The CCl4 concentrations had to be corrected. CCl4 concentrations have been 
raised by 3% to account for insufficient extraction from the water sample. 

The ratios of CFC-11/CFC-12 and CFC-113/CFC-12 are rising rapidly and 
consistently on all stations in the deep eastern basin with very low CFCs (283-
295), partially even above the highest values that ever existed. The profiles of 
individual tracers look quite reasonable. CFC-11 and CFC-113 have been flagged 
questionable (3) wherever this occurred.

Flags have generally been assigned by looking at individual profiles together 
with neighbouring profiles. Obvious deviations that did not correspond to any 
hydrographic property change have been flagged out.


FLAGS for the CFCs

                              2      3      4     6     9
                            good   quest   bad   rep   not
                      ------------------------------------
                      F-11   712    37      13    7    781
                      F-12   734    17      10    8    781
                      F-113  715    33      14    7    781
                      CCl4   740     7      14    8    781


REPRODUCIBILITY:

                                  F-11:  0.8 %
                                  F-12:  1.0 %
                                  F-113: 4.0 %
                                  CCl4:  1.6 %


PRECISION:

    F11:   0.002 pmol/kg or a relative error of 0.5% (whichever is greater)
    F12:   0.001 pmol/kg or a relative error of 0.4% (whichever is greater)
    F-113: 0.001 pmol/kg or a relative error of 3.3% (whichever is greater)
    CCl4:  0.005 pmol/kg or a relative error of 0.7% (whichever is greater)


Mean water blank, detection limit:

                           F-11:  0.12 fmol/kg ± 0.56
                           F-12:  0.01 fmol/kg ± 0.23
                           F-113: 2.04 fmol/kg ± 1.96
                           CCl4:  0.11 fmol/kg ± 0.37 

For F-11 a waterblank of 4 fmol/kg has been subtracted. This accounts for 
possible bottle/system contaminations eventually causing the high CFC-11/CFC-12 
ratios wherever the CFCs are very low. But the ratios stayed too high even 
though (see above).


AIR MEASUREMENTS:

Theoretical values for 1997 (northern hemisphere) (SIO-1993 Scale):

                           F-11    F-12    F-113  CCl4
                           263.8   537.5   83.2   99.5

Individual air measurements performed during the cruise (SIO 93 scale):

                   Sta   F12     F11     F113    CCl4    qual
                         pptv    pptv    pptv    pptv
                   ------------------------------------------
                   289   535.2   262.2   84.36   100.8   6666
                   299   537.9   264.94  84.29   100.1   6666
                   309   537.1   263.3   84.05   100.0   6666
                   310   536.6   264.5   83.00   100.9   6666
                   318   536.3   266.7   84.65   101.0   6666
                   329   531.9   264.5   82.93   99.54   6666
                   ------------------------------------------
                   uncertainties of the air measurements
                         0.3 %   0.5 %   0.9 %   2.1 %

Helium and tritium measurements during this cruise have been measured by the 
Institut f¸r Umweltphysik Bremen as well and will be reported later.



9.3	WOCE LINE AR07W_06MT39_4
	1997.JUL.07 - 1997.AUG.08

CFC PIs: Monika Rhein and Olaf Plähn
         Institut für Meereskunde, 24105 Kiel, Germany
     now at:
         Institut für Ostseeforschung, 18119 Rostock, Germany
         email: monika.rhein@io-warnemuende.de
                oplaehn@ifm.uni-kiel.de

CFC-Lab: Martina Elbrächter and Kristin Bahrenfuss Institut für Meereskunde
                24105 Kiel, Germany
         email: melbraechter@ifm.uni-kiel.de

Region:  North Atlantic, Labrador Sea 48°N - 61°N, 58°W - 35°W


SAMPLE COLLECTION AND TECHNIQUE

All samples were collected from 10 L Niskin bottles. The bottles had 
been cleaned prior to the cruise using isopropanol. All 'O' rings, 
valves, and taps were removed, washed in isopropanol and baked in a 
vacuum oven for 24 hours. The rubber bands on all bottles were replaced 
by stainless steel springs. The personnel for all water sampling and 
handling procedures at the bottles wore one-way gloves to protect the 
valves from grease. 

About 100 mL of water were taken from the water bottles with gastight 
glass syringes (Becton and Dickinson). Then 15-25 mL of the samples were 
transferred to a purge and trap unit and analyzed on board following the 
procedures described in Bullister and Weiss [1988]. The CFCs were 
separated on a packed stainless steel column filled with Porasil C and 
detected with an Electron Capture Detector (ECD). The carrier gas was 
ECD pure Nitrogen, which was additionally cleaned by molsieves (13X mesh 
80/100). A standard gas -- kindly provided by D. Wallace, IfM Kiel (ALM 
0383034) -- was used to convert the ECD signal in concentrations. The 
CFC concentrations are reported in pmol kg -1 on the SIO93 scale (R. 
Weiss, SIO). 


Figure 1: Accuracy (%) of the CFC-12 (a) and CFC-11 (b) replicate 
          samples against station number. The line represents the mean 
          accuracy of the CFC-12 and CFC-11 samples, respectively. Note 
          the different scales for (a) and (b).


PERFORMANCE

During the cruise M39/4 the Kiel CFC system worked continuously. Both 
CFC components CFC-11 and CFC-12 had been sampled on 97 CTD stations and 
1850 water samples had been analyzed. The survey was dedicated to the 
circulation of the deep water masses. During periods of dense station 
spacing, sampling was focused on the water column below 800 m depth. 

Accuracy was checked by analyzing 213 water samples twice, and the mean 
rms was 0.7% for CFC-11 and 1.2% for CFC-12. The latter varied owing to 
the intensity of the unknown peak affecting the integration of the CFC-
12 peak (Figure 1). The rms of CFC-11 and CFC-12 at the station 366-367 
(profiles 22-23) were higher than average, caused by frequent 
malfunctions of the caliper used to determine the volume of the water 
sample. After replacement, the accuracy was back to normal. The system 
blanks for CFC-11 and CFC-12 were negligible. The blanks were deter- 
mined by degassing CFC free water, produced by purging ECD clean 
Nitrogen permanently through 5 L seawater. The blanks were lower than 
0.005 pmol kg -1 for both, CFC-11 and CFC-12. 

The Niskin bottle blanks on this cruise could not be determined 
directly, as CFC-free deep water is not present in the western subpolar 
North Atlantic. We assume that the bottle blanks are similar to the 
other cruises. Measurements in the deep Rockall Trough (on leg 5), where 
CFC-poor water was found, showed that the bottle blanks were lower than 
0.01 pmol kg -1 . On our cruises in the Northern Indian Ocean and the 
Tropical Atlantic, where CFC free deep water is available, the blanks of 
the pre-cleaned bottles were lower than 0.003 pmol kg -1 for both 
components. 


Figure 2: Temporal evolution of the efficiency of the ECD (mVs/mg        
          standard) for the 5 mL sample volume.
Figure 3: An example of the calibration curve for CFC-12 and CFC-11       
          before and after the CFC measurements of station 366.


The temporal evolution of the ECD efficiency is shown in Figure 2. 
During the cruise the efficiency decreased about 20%. Major changes 
occurred, when the drying agent (magnesiumperchlorate) in the purge and 
trap unit or the molsieves for purifying the carrier gas were exchanged. 

To correct the temporal drift, a calibration curve with 4-6 different 
standard gas volumes was carried out before and after each station. The 
change between these curves is thought to occur linear with time. As a 
typical example, the two calibration curves for station 366 are 
presented in Figure 3. CFC concentrations were calculated by using the 
two neighboured callibration points, assuming that the calibration curve 
is linear between these points. 

At first we used sample volumes, precalibrated by the company (Machery 
and Nagel, Germany) for the analysis of standard gas. It turned out that 
these volumes could be off by more than 5%, affecting the precision of 
the measured oceanic CFC concentrations by the same amount. Therefore, 
in 1998, the volumes for the gas standard measurements (nominal 2 mL and 
5 mL) were calibrated against two 'master' volumes by D. Wallace's group 
(IfM Kiel), who had done this task also for the CO2 community. CFC 
measurements of the air inside the vessel and especially in the lab were 
carried out frequently in order to check for contamination. In general, 
the CFC concentrations in both places were only a few percent higher 
than in clean air. Clean air measurements were carried out occasionally 
by sampling air from the ship's compass bridge or forecastle. 


PROBLEMS 

CFC-11 analysis was successfully carried out during the cruise, the 
analysis of the CFC-12 concentrations, however, was partly impeded by an 
unknown substance with a similar retention time as CFC-12. In the data-
file, the CFC-12 component got the quality flag'3'. 


COMMENTS 

Leg 4 is part of the 1997 Kiel CFC data set including the M39 legs 2 and 
5 in the subpolar North Atlantic. During the cruise the WHP section AR7 
was repeated. The surface saturation of CFC-11 relative to the 
atmospheric values of 226 ppt varied from 105-117% in the Labrador Sea 
to 98-105% east of 45 Æ W [Körtzinger et al., 1999]. The high 
supersaturations off the shelf in the Labrador Sea (Fig. 4) are 
presumably caused by recent mixing of cold and CFC rich water with 
warmer water from the south, while the air sea gas exchange had not 
enough time to equilibrate with the atmosphere. 


Figure 4: M39/4, CFC-11 surface saturation relative to 266 ppt CFC-11, 
          black dot: 110-117%, star: 110-105%, circle with cross: 105-
          100%, and cross: 100-98%.
Figure 5: Cruise M39/4, all CFC-11 data [pmol kg -1] versus depth.


In Figure 5 all CFC-11 concentrations measured during the cruise Meteor 
39/4 are shown. In the whole water column the concentrations span a 
large range. For example, the CFC-11 concentrations in the Labrador Sea 
Water (LSW) varied along the AR7- section between 4.0 - 4.6 pmol kg -1. 
South of the Gibbs Fracture Zone the values in this water mass did not 
exceed 3.5 pmol kg -1.

o Note, that this is not a WOCE cruise, and the data are not in the
  WOCE format!
o The data are only for personal use. If you want them for other   
  purposes, you need the consent of Monika Rhein.


REFERENCES

Bullister, J.L. and R.F. Weiss (1988). Determination of CCl3F and CCl2F2 
          in seawaterand air. Deep-Sea Res., 35, p. 839{853.
Koortzinger, A., M. Rhein, and L. Mintrop (1999). Anthropogenic CO2 and 
          CFCs in the North Atlantic Ocean -- A comparison of man-made 
          tracer. Geophys. Res. Lett., 26, p. 2065 - 2068.


o the station file 'meteor394.sum' includes:
  1 station number
  2 year
  3 month
  4 day
  5 hour: minutes in decimal system
  6 latitude: minutes in decimals
  7 longitude: minutes in decimals
  8 water depth (m)
  9 depth of CTD profile (m)

o the bottle _le 'meteor394.sea' includes:
  1 station number
  2 bottle number
  3 depth (dbar)
  4 in-situ temperature (ÆC)
  5 salinity (psu)
  6 CFC-12 (pmol kg_ 1)
  7 CFC-11 (pmol kg_ 1)
  8 WOCE quality flag for CFC-12 and CFC-11


TECHNICAL INFORMATION

Gas chromatograph                  Shimadzu GC 14
GC column                          stainless steel packed with Porasil C
Cooling trap                       with Porapak T and Porasil C
Trap temperatures                  -30°C, 100°C
Column temperature                 70°C, isothermal
ECD temperature                    300°C
Electron capture detector          Shimadzu
Software for chromatogram analysis Shimadzu CLASS LC 10 (1.63)
Standard gas                       ALM 0383034, D. Wallace, PMEL
Precision                          CFC-11: 3%, CFC-12: 10%
Accuracy                           CFC-11: 0.7%, CFC-12: 1.2%
Blanks                             negligible



9.4  WOCE LINES AR07E, AR25_06MT39_5
     1997.AUG.14 - 1997.SEP.14
  
CFC PIs: Monika Rhein
         Institut für Meereskunde, 24105 Kiel, Germany
     now at:
         Institut für Ostseeforschung, 18119 Rostock, Germany
         email: monika.rhein@io-warnemuende.de
                oplaehn@ifm.uni-kiel.de

CFC-Lab: Martina Elbrächter and Kristin Bahrenfuss
         Institut für Meereskunde, 24105 Kiel, Germany
         email: melbraechter@ifm.uni-kiel.de

Region:  Subpolar North Atlantic 


SAMPLE COLLECTION AND TECHNIQUE

The water samples were drawn from precleaned 10 L Niskin bottles with gas 
tight 100 mL glass syringes (Becton and Dickinson). CFCs were measured on 
board with a GC-ECD (Electron Capture Detector) technique first described by 
Bullister and Weiss [1988]. About 15-25 mL were transferred to a purge and 
trap unit. The CFCs were separated on a packed stainless steel column filled 
with Porasil C and detected with an ECD. The carrier gas is ECD pure 
Nitrogen, which was additionally cleaned by molsieves (13X mesh 80/100). All 
'O' rings and valves as well as the nylon stopcocks (of the syringes) were 
removed and washed in isopropanol and baked in a vacuum oven for 24 hours 
prior the cruise. The Niskin bottles were cleaned with Isopropanol. The 
rubber bands on all bottles were replaced by stainless steel springs. The 
personnel for all water sampling and handling procedures at the bottles wore 
one-way gloves to protect the valves from grease.

A standard gas (ALM 0383034, 120.5 ppt CFC-12, 266.4 ppt CFC-11 kindly 
provided by D. Wallace, IfM Kiel) was used to convert the ECD signal in 
concentrations. The CFC concentrations are reported in pmol kg-1 on the SIO93 
scale (R. Weiss, SIO).


PERFORMANCE

During leg Meteor 39/5, the Kiel CFC system worked continuously and about 
1550 water samples on 99 stations had been analysed. The survey was dedicated 
to the circulation of the deep water masses. During periods of dense station 
spacing, sampling was focused on the water column below 800 m depth.

Accuracy was checked by analysing about 10% of the water samples twice. The 
result was confirmed by the accuracy obtained at the test stations, where 
several bottles were dripped at the same depths. The accuracy at these test 
stations was better than 0.5% for both substances (Figure 1). The system 
blanks for CFC-11 and CFC-12 were negligible. The blanks were determined by 
degassing CFC free water, produced by purging ECD clean Nitrogen permanently 
through 5 L seawater. The blanks were lower than 0.005 pmol kg-1 for both 
components.

The Niskin bottle blanks on this cruise could not be determined directly, as 
CFC-free deep water is not present in the subpolar North Atlantic. We could 
only estimate an upper bound of the blank by the measurements in the deep 
Rockall Trough, where CFC-poor water is found. CFC-11 concentrations in the 
deep water were similar to the values found at the R/V Meteor cruise 30/3, 
November 1994 (Figure 2). Owing to these measurements the bottle blanks are 
lower than 0.01 pmol kg-1. On our cruises in the Northern Indian Ocean and the 
Tropical Atlantic, where CFC free deep water is available, the blanks of the 
precleaned bottles were lower than 0.003 pmol kg-1 for both components (CFC-12 
and CFC-11).

The temporal evolution of the ECD efficiency is shown in Figure 3. During the 
cruise the efficiency decreased about 25%. Major changes occurred, when the 
drying agent (magnesiumperchlorate) in the purge and trap unit was exchanged. 
To correct the temporal drift of the ECD, a calibration curve with 4-6 
different standard gas volumes was carried out before and after each station. 
The change between these curves is thought to occur linear with time. As a 
typical example, the two calibration curves for station 512 are presented in 
Figure 4. CFC concentrations are calculated by using the two neighboured 
callibration points, assuming that the calibration curve is linear between 
these points.

At first we used sample volumes, precalibrated by the company (Machery and 
Nagel, Germany) for the analysis of standard gas. It turned out that these 
volumes could be off by more than 5%, affecting the precision of the measured 
oceanic CFC concentrations by the same amount. Therefore, in 1998, the 
volumes for the gas standard measurements (nominal 2 mL and 5 mL) were 
calibrated against two 'master' volumes by D. Wallace's group (IfM Kiel), who 
had done this task also for the CO2 community. CFC measurements of the air 
inside the vessel and especially in the lab were carried out frequently in 
order to check for contamination. In general, the CFC concentrations in both 
places were only a few percent higher than in clean air. Clean air 
measurements were carried out occasionally by sampling air from the ship's 
compass bridge or forecastle.


PROBLEMS

CFC-11 analysis was successfully carried out during the cruise. The analysis 
of the CFC-12 peak, however was disturbed by an unknown substance with a 
similar retention time as CFC-12. The unknown peak affected the precision of 
the CFC-12 data, but did not influence the mean accuracy very much (Figure 
1).

During the analysis of the stations 470-483, the efficiency declined rapidly 
(Fig. 3). The CFC-11 measurements during this time had been flagged with '3'. 


COMMENTS 

Leg 5 completed the Kiel CFC data set of the Meteor 39 cruise, covering the 
subpolar East Atlantic (leg 2) and the West Atlantic (leg 4). The second part 
of the cruise was again a repeat of the WHP section A1E/AR7E.

The surface saturation of CFC-11 relative to the atmospheric value of 266 
pptV varied from 104-107% in the northern Irminger Sea to 98-101% in the 
eastern Atlantic (Figure 5). The supersaturations west of Iceland and off the 
shelf in the northern Irminger Sea are presumably caused by recent mixing of 
cold and CFC rich water from the East Greenland Current with warmer water 
from the south, while the air sea gas exchange had not enough time to 
equilibrate with the atmosphere. Similar high saturations were found off 
Newfoundland, where the cold Labrador Current meets the warmer North Atlantic 
Current [Körtzinger et al., 1999].

In Figure 6 all CFC-11 data measured during the cruise are shown. In general, 
the concentrations decrease eastward, as the values are higher in the 
Irminger Sea than east of the Reykjarnes Ridge [Sy et al., 1997]. The high 
concentrations below 2500 m depth characterized the CFC-rich Denmark Strait 
Overflow Water (DSOW), which can be found at Greenland slope. Compared to the 
data collected during the cruise Meteor 30/3 in November 1994 [Sy et al., 
1997], the CFC-11 signal of the Labrador Sea Water (LSW) did not change 
significantly in the Irminger Sea, but increased in the eastern Atlantic.


REFERENCES 

Bullister, J.L. and R.F. Weiss (1988). Determination of CCl3 F and CCl2 F2 in 
          Seawater and Air. Deep-Sea Res., 35, p. 839-853.

Körtzinger, A., M. Rhein, and L. Mintrop (1999). Anthropogenic CO2 and CFCs 
          in the North Atlantic Ocean - A comparison of Man-made Tracer. 
          Geophys. Res. Lett., 26, p. 2065-2068.

Sy, A., M. Rhein, J.R.N. Lazier, K.P. Koltermann, J. Meincke, A. Putzka, and 
          M. Bersch (1997). Surprisingly Rapid Cooling of Newly Formed 
          Intermediate Waters Across the North Atlantic Ocean. Nature, 386, 
          p. 675-679. 


APPENDIX

THE STATION FILE 'METEOR395.SUM' INCLUDES:
1. 1 station number
2. 2 year
3. 3 month
4. 4 day
5. 5 hour: minutes in decimal system
6. 6 latitude: minutes in decimals
7. 7 longitude: minutes in decimals
8. 8 water depth (m)
9. 9 depth of CTD profile (m)

THE BOTTLE FILE 'METEOR395.SEA' INCLUDES:
1. 1 station number
2. 2 bottle number
3. 3 depth (dbar)
4. 4 in-situ temperature (°C)
5. 5 salinity (psu)
6. 6 CFC-12 (pmol kg-1)
7. 7 CFC-11 (pmol kg-1)
8. 8 WOCE quality flag for CFC-12 and CFC-11


TECHNICAL INFORMATION

Gas chromatograph                   Shimadzu GC 14
GC column                           stainless steel, packed with Porasil C
Cooling trap                        with Porapak T and Porasil C
Trap temperatures                   -30°C, 100°C
Electron capture detector           Shimadzu
Column temperature                  70°C, isothermal
ECD temperature                     300°C
Software for chromatogram analysis  Shimadzu CLASS LC 10 (1.63)
Standard gas                        ALM 0383034, D. Wallace, IfM Kiel
Precision                           CFC-11: 3%, CFC-12: 10%
Accuracy                            CFC-11: 0.5% , CFC-12: 1.5%
Blanks                               negligible



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