A.   Cruise Narrative: A01 and A02

A.1. Highlights

                       WHP Cruise Summary Information

      WOCE section designation  A01                    | A02
        Expedition designation  06MT30_3               | 06MT30_2
Chief Scientist(s)/affiliation  Jens Meincke/IfMHH     | Peter Koltermann/BSH
                         Dates  1994.11.15-1994.12.19  | 1994.10.12-1994.11.12
            Number of stations  63                     | 53
  Floats and drifters deployed  6 Floats deployed      | 0 floats deployed
Moorings deployed or recovered  0                      | 0
                          Ship  RV METEOR
                 Ports of call  Hamburg to St. John's to Hamburg

         Geographic boundaries  
                           A01             60°33.90'N
                                54°29.50'W            14°15.40'W
                                           51°35.10'N

                           A02             49°14.10'N 
                                48°45.00'W            10°39.60'W
                                           41°59.60'N

                 Contributing Authors, (as they appear in text)

         W. Balzer        B. Owens      K. Jeskulke        R. Kramer
         O. Pfannkuche    I. Büns       T. Soltwedel       F. Oestereich
         H. Thiel         A. Pfeifer    K.C. Soetje        D.S. Kirkwood
         B.v. Bodungen    A. Deeken     V. Terechtchenkov  E. Gier
         U. Brockmann     H. Dierssen   P. Wöckel          F. Müller
         M. Andreae       S. Otto       M. Stolley         P. Heil
         K.P. Koltermann  H. Wellmann   H. Johannsen       A. Schaub
         J. Duinker       G. Uher       F. Malien          C. Atwood
         L. Mintrop       O. Flöck      A. Putzka          A. Krötzinger
         W. Roether       G. Schebeske  K. Bulsiewicz      S. Schweinsberg
         J. Meincke       V. Ulshöfer   C. Rüth            A.v. Hippel
         R. Bayer         A.N Antia     H. Rose            C. Senet
         A. Sy            W. Erasmi     B. Kromer          H. Thomas
         M. Rhein         R.S. Lampitt  M. Born            R. Prado-Fiedler
         B. Schneider     T. Kumbier    D. Kirkwood          
         G.M. Raisbeck    G. Lehnert    I. Horn
         R. Davis         K. Poremba




                               METEOR CRUISE M30

                 JGOFS, OMEX and WOCE in the North Atlantic 1994

                                  Cruise No 30

                         7 September - 22 December 1994

                   Las Palmas - Hamburg - St John's - Hamburg

TABLE OF CONTENTS

ABSTRACT
ZUSAMMENFASSUNG

1	RESEARCH OBJECTIVES
	Leg M30/1:	Las Palmas - Hamburg
	OMEX	Ocean Margin Exchange
	Legs M30/2-3: Hamburg - St. John's - Hamburg
	WOCE	World Ocean Circulation Experiment
	JGOFS	Joint Global Ocean Flux Study

2	PARTICIPANTS
2.1		Leg M30/1
2.2		Leg M30/2
2.3		Leg M30/3
2.4		Participating Institutions

3	RESEARCH PROGRAMMES
3.1		OMEX Programmes:
	3.1.1	Organic Matter Degradation, Denitrification and Trace Metal Diagenesis
	3.1.2	Carbon Mineralization by the Benthic Community
	3.1.3	Vertical Particle Flux at the Continental Margin
	3.1.4	Phase Transfer of Organic Compounds During Shelf Edge Passage
	3.1.5	Flux of Trace Gases at the Boundary Between Ocean and Atmosphere
3.2		WOCE Programmes:
3.2.1	Determination of the Meridional Transports of Heat, Salt and Freshwater at 
	48°N in the North Atlantic along the WHP section A2
3.2.2	Nutrients Measurements for the Fine Resolution of Oceanic Water Masses on 
	the Meteor Cruise M30/2 (section WHP-A2) in the North Atlantic
3.2.3	CFCs on the section WHP-A2
3.2.4	Mooring Recovery on sections WHP-A2 and WHP-A1
3.2.5	Tritium/Helium and 14C-Sampling along WHP-sections A2 and A1
3.2.6	WOCE North Atlantic Overturning Rate Determination 
       (WOCE-NORD, WHP section A1)
3.2.7	CFCs on the section WHP-A1
3.3		JGOFS - Programmes:
	3.3.1	The Control Function of the Carbonate-System in the Oceanic CO2 uptake, 
		WHP-A2
	3.3.2	The Ocean as a CO2 Sink: Complimentary Studies of the Baltic Sea and 
		the North Atlantic, WHP-A1
3.4		Individual Projects
	3.4.1	129I from Nuclear Fuel Processing as an Oceanographic Tracer
	3.4.2	Profiling ALACE Floats to Determine the Development of the 
		Stratification in the Labrador Sea Over Two Years

4	NARRATIVE OF THE CRUISE
4.1		Leg M30/1	(Chief Scientist-O. Pfannkuche)
4.2		Leg M30/2	(Chief Scientist-K.P. Koltermann)
4.3		Leg M30/3	(Chief Scientist-J. Meincke)


5	OPERATIONAL DETAILS AND PRELIMINARY RESULTS
5.1		OMEX Programmes:
	5.1.1	Biochemistry
-	Phase Transfer of Organic Compounds During Shelf Edge Passage
-	Organic Matter Degradation, Denitrification and Trace Metal Diagenesis
-	Dissolved Organic Carbon
-	Pore Water Chemistry
-	Benthis Denitrification and Bioirrigation
	5.1.2	Air Chemistry
-	Exchange of Reduced Sulphur Compounds Between Ocean and Atmosphere
	5.1.3	Sedimentology
-	Particle Flux and in situ Marine Aggregate Studies at the Continental Margin
-	Particle Flux
-	Marine Snow Studies
-	CTD - work 
	5.1.4	Benthic Biology
-	Benthic Microbiology
-	Carbon Mineralization by the Benthic Community
5.2	WOCE Programmes:
	5.2.1	Physical and Chemical Oceanography on Leg M30/2
-	Determination of the Meridional Transports of Heat, Salt and Freshwater at 
	48°N in the North Atlantic Along the WHP section A2
-	Nutrients Measurements for Fine Resolution of Oceanic Water Masses on the 
	Meteor Cruise M30/2 (section WHP-A2) in the North Atlantic
-	CFCs on the WHP section A2
-	Tritium/Helium and 14C-Sampling Along WHP-sections A2 and A1
	5.2.2	Mooring Recovery on WHP-A2 and WHP-A1
	5.2.3	Physical, Chemical and Tracer Oceanography on Leg M30/3
-	Hydrographic Measurements on WHP-A1
		Nutrients Along WHP-A1
-	Spreading of Newly Formed Labrador Sea Water
-	Thermosalinograph, XBT and XCTD Measurements
			XBT Sections
			XCTD Field Test
-	Sample Oxygen Measurements on WHP-A1
-	Nutrient Measurements on WHP-A1
-	Tracer Studies on WHP-A1
		Tracer Oceanography: Tritium/Helium and Radiocarbon
		Tracer Oceanography: CFCs
5.3		JGOFS Programmes:
	5.3.1	The Control Function of the Carbonate-System in the Oceanic CO2 
		uptake, WHP-A2
	5.3.2	The Ocean as a CO2 Sink: Complimentary Studies of the Baltic Sea and 
		the North Atlantic, WHP-A1
5.4		Individual Programmes:
	5.4.1	129I from Nuclear Fuel Processing as an Oceanographic Tracer
	5.4.2	ALACE Float Deployments


6	SHIP'S METEOROLOGICAL STATION
6.1		Leg M30/1
6.2		Leg M30/2
6.3		Leg M30/3


7	LISTS
7.1		List of Stations
	7.1.1	Lists of Sampling Stations M30/1
	7.1.2	Station List Leg M30/2 Section WHP-A2
-	Summary of Sub-Sampling Schemes, Hydrographic Stations on M30/2
-	Summary of Daily Station Activities M30/2
	7.1.3	Station List Leg M30/3 Section A1W
-	Station List Leg M30/3 Section A1E
7.2		List of Moored Instruments
	7.2.1	Leg M30/1	Sediment Trap Mooring Positions
	7.2.2	Leg M30/2	Current Meter Mooring Positions
	7.2.3	Leg M30/3	Current Meter Mooring Positions
7.3		List of Figures

8	CONCLUDING REMARKS
9	REFERENCES
10	NOTES

ABSTRACT

The Meteor Cruise M30 focused on the North Atlantic components of the global 
research programmes Joint Ocean Flux Study JGOFS, the World Ocean Circulation 
Experiment WOCE and the European programme Ocean Margin EXchange OMEX. 

On the first leg, the exchange processes between the oceanic continental margins 
and the open ocean were addressed. A special emphasis has been put in this 
programme on the interfaces sediment/ocean and ocean/atmosphere. The Celtic 
shelf edge was chosen as the regional focus for this multidisciplinary research 
work. 

The second and third leg used the unique opportunity to determine the 
modification and partitioning of the North Atlantic water masses in a fully 
enclosed region between 48( and 61(N. This programme is part of a longer-lasting 
effort to observe long-term changes of the meridional transports of heat, salt 
and fresh-water on time scales relevant to climate change. The WOCE component of 
ca. 10 weeks field- work will be used to describe in space the quasi-synoptic 
evolution of the hydrographic situation of the "overturning cell" of the global 
thermohaline circulation in the North Atlantic Ocean. Previous assessments as 
part of the WOCE Hydrographic Programme WHP on the section WHP-A1E in 1991 by FS 
Meteor, of AR7E in September 1992 with FS Valdivia (WOCE-NORD) and of WHP-AR19 
in summer 1993 with FS Gauss already showed dramatic changes in water mass 
properties and the depth of individual water mass layers compared to work done 
during the International Geophysical Year IGY in 1957 and other in 1962 and 
1982. These changes in intermediate and deep water masses associate directly 
with the annual winter sections worked in the Labrador Sea by Canadian 
colleagues since 1988 and this new assessment promises to describe in much 
greater details the linkage between local forcing and the large-scale reaction 
of the North Atlantic circulation.

ZUSAMMENFASSUNG

Die Meteor - Reise 30 war den nordatlantischen Komponenten der globalen 
Forschungsprogramme Joint Global Ocean Flux Study JGOFS und World Ocean 
Circulation Experiment WOCE und dem europäischen Programm Ocean Margin EXchange 
OMEX gewidmet.

Im ersten Fahrtabschnitt (M30/1) standen die Austauschprozesse zwischen den 
ozeanischen Kontinentalrändern und dem offenen Ozean im Mittelpunkt. Dabei wurde 
ein besonderes Gewicht auf die Grenzflächen Sediment/Wasser und Ozean/Atmosphäre 
gelegt. Als regionaler Schwerpunkt für diese umfangreichen multidisziplinären 
Untersuchungen wurde der keltische Schelfrand gewählt. 

Der zweite und dritte Fahrtabschnitt (M30/2 und M30/3) boten die erstmalige 
Möglichkeit, die Modifikation der nordatlantischen Wassermassen und ihre daran 
beteiligten jeweiligen Anteile in einem abgeschlossenen Gebiet zwischen 48(N und 
61(N eindeutig zu bestimmen. Diese Arbeiten führen die Beobachtung der 
langzeitigen klimarelevanten Schwankungen von meridionalen Wärme-, Salz- und 
Süßwassertransporten der letzten Jahre fort. Dabei gewährleistete das WOCE- 
Feldprogramm von ca. 10 Wochen erstmalig eine räumlich abgeschlossene quasi- 
synoptische Erfassung des hydrographischen Zustandes der "overturning cell" der 
globalen thermohalinen Zirkulation im Nordatlantik. Die bisherigen Aufnahmen im 
Rahmen des WOCE Hydrographic Programme WHP von WHP-A1E im Jahre 1991 mit FS 
"Meteor" bzw. von AR7E im September 1992 mit FS "Valdivia" (WOCE-NORD) und WHP-
AR19 im Sommer 1993 mit FS "Gauss" haben bereits drastische Veränderungen in den 
Eigenschaften der Wassermassen und der Tiefe der individuellen Schichten der 
Wassermassen im Vergleich zu den früheren Aufnahmen während des Internationalen 
Geophysikalischen Jahr 1957 und in den Jahren 1962 und 1982 ergeben. Die erneute 
Erfassung der intermediären und tiefen Zirkulation insbesondere im Zusammenhang 
mit den jährlichen winterlichen Aufnahmen der Labrador-See durch kanadische 
Kollegen seit 1988 verbessert die Beschreibung der sich abzeichnenden Beziehung 
zwischen dem örtlichen "forcing" und der großräumigen Reaktion des nördlichen 
Atlantiks. 


1  RESEARCH OBJECTIVES

Leg M30/1: Las Palmas - Hamburg
           OMEX Ocean Margin Exchange

On the first leg of METEOR cruise 30 the exchange processes of carbon and "green 
house" gases between the western European shelf edge and the open ocean were 
studied within the frame of an interdisciplinary European Union Programme "Ocean 
Margin Exchange" (OMEX). Station work concentrated on a transect from the outer 
Celtic Sea (Great Sole Bank) across the Goban Spur into the Porcupine Seabight 
covering a depth range from 220 m to 4800 m (Fig. 1). Special emphasis was put 
on the interfaces sediment/ocean and ocean/atmosphere.


Legs M30/2 and M30/3: Hamburg - St. John's - Hamburg WOCE 
                      World Ocean Circulation Experiment

This German contribution to the international WOCE Programme as part of the 
World Climate Research Programme WCRP focused on the Northern North Atlantic in 
late autumn. Here we find significant changes in the water mass characteristics 
such as temperature, salinity and the contents of dissolved oxygen caused by the 
highly variable meteorological forcing on annual and interannual time scales. 
These changes affect the contribution of the North Atlantic to the global 
thermohaline circulation in the form of the North Atlantic Deep Water and its 
signatures. It, in the end, will affect the meridional transports of heat, 
salinity and freshwater.

For a highly resolved description of the water masses that are modified by these 
processes besides measurements of temperature and salinity, the concentrations 
of dissolved oxygen content, nutrients and a sequence of transient tracers such 
as CFCs, carbon 14C, helium 3He and 4He and tritium 3H was analysed from water 
samples. Using the characteristic input functions into the ocean, the relevant 
modification processes and their regions will be better resolved.

Since the scientific programme for both cruise legs M30/2 and M30/3 is 
essentially identical and only most of the participating groups changed, for 
both legs a joint programme description is given below.

The German contributions to WOCE and JGOFS have been funded by the Federal 
Ministry for Research and Technology (BMFT).

JGOFS Joint Global Ocean Flux Study

In co-operation with JGOFS, all WOCE WHP-sections are to be sampled for 
dissolved and particular CO2 to better quantify the ocean's role as a reservoir 
in the global carbon system. Sections A2 at 48(N and A1 at ca. 57(N have been 
sampled in this context. The data are being made available to the appropriate 
data centres. 


2  PARTICIPANTS

2.1  Leg M30/1

NAME			   SPECIALITY		INSTITUTION
Pfannkuche, Olaf, Dr.,	   Benthic Biology	GEOMAR		Chief Scientist 
Antia, Avan, Dr.	   Planktology		IfMK
Balzer, Wolfgang Prof. Dr. Marine Chemistry	UBMCh
Bassek, Dieter		   Weather Technician	DWD/SWA
Behrens, Katrin		   Benthic Biology	IHF
Bosse, Kai		   Benthic Biology	IHF
Büns, Ilse		   Biochemistry		UHIBL
Deeken, Aloys		   Marine Chemistry	UBMCh
Dierßen, Holger		   Marine Chemistry	UBMCh
Dölle, Martina		   Benthic Biology	IHF
Erasmi, Wolfgang	   Hydrography		IfMK
Flöck, Otmar		   Biogeochemistry	MPICh
Götz, Sabine		   Benthic Biology	IHF
Jeskulke, Karen		   Benthic Biology	IfMK
Kahl, G.		   Meteorology 		DWD/SWA
Kumbier, Thomas		   Electronics		IfMK
Lampitt, Richard Dr.	   Planktology		IOSDL
Lehnert, Gerhard	   Planktology		IOW
Nuppenau, Volker	   Electronics		IHF
Otto, Sabine		   Marine Chemistry	UBMCh
Pfeiffer, Alexander	   Biochemistry		UHIBL
Poremba, Knut, Dr.	   Benthic Biology	IfMK
Schebeske, Günther	   Biogeochemistry	MPICh
Soltwedel, Thomas  Dr.	   Benthic Biology	IHF
Uher, Günther		   Biogeochemistry	MPICh
Ulshöver, Veit		   Biogeochemistry	MPICh
Wellmann, Hartwig	   Marine Chemistry	UBMCh
Witte, Ursula  Dr.	   Benthic Biology	IHF


2.2  Leg M30/2

NAME			   SPECIALITY		INSTITUTION
Dr.Koltermann,Klaus Peter, Phys. Oceanography	BSH		Chief Scientist
Wöckel, Peter		   CTD-support		BSH
Soetje, Kai C		   CTD-Computing	BSH
Mauritz, Heiko		   CTD-computing	BSH
Stolley, Martin		   Hydro watch		BSH
Frohse, Alex		   Salinometer		BSH
Berger, Ralf		   CTD-support		IfMK
Dr.Terechtchenkov,Vladimir Hydro watch		BSH/PPS
Hatten, Helge		   Hydro watch		IfMHH
Outzen, Olaf		   Hydro watch		IfMHH
Löwe; Peter		   Hydro watch		BSH
Giese, Holger		   Hydro/moorings	BSH
Dr. Mintrop, Ludger	   Chemistry/CO2	IfMK
Körtzinger, Arne	   Chemistry/CO2	IfMK
Johannsen, Helge	   Chemistry/nutrients	IfMK
Malien, Frank		   Chemistry/nutrients	IfMK
Schweinsberg, Susanne	   Chemistry/CO2	IfMK
Senet, Christian 	   Chemistry/CO2	IfMK
von Hippel, Annette	   Chemistry/CO2	IfMK
Atwood, Chris		   Chemistry/CO2	SIO
Bulsiewicz, Klaus	   CFCs			IUP-B
Rose, Henning		   CFCs			IUP-B
Rüth, Christine		   CFCs			IUP-B
Dr. Bayer, Reinhold	   Tracer		IUP-HD
Dr. Kromer, Bernd	   Tracer		IUP-HD
Dr. Born, Matthias	   Tracer		IUP-HD
Rübel, André		   Tracer		IUP-HD
Kühr,  Sabine		   Tracer		IUP-HD
Dr. Röd, Erhard		   Ship's Meteorologist	SWA
Lambert, Hans-Peter	   Weather Technician	SWA


2.3  Leg M30/3

NAME			   SPECIALITY		INSTITUTION
Dr. Meincke, Jens,	   Phys Oceanography	IfMHH		Chief Scientist
Dr. Sy, Alexander	   Hydrography		BSH
Bersch, Manfred		   Hydro watch		IfMHH
Paul, Uwe		   Hydro watch		BSH
Dr. Lazier, John	   Hydro watch		BIO
Gerdes, Jürgen		   Hydro watch		IfMHH
Haak, Helmuth		   Hydro watch		IfMHH
Bock, Jan		   Hydro watch		IfMHH
Dombrowski, Uwe		   CTD-support		IfMK
Verch, Norbert		   Salinometer		IfMHH
Mauritz, Heiko		   CTD-computing	BSH
Gottschalk, Ilse	   CTD-computing	BSH
Kramer, Rita		   O2			BSH
Horn, Ines		   O2			BSH
Oestereich, Frank	   O2/nutrients		BSH
Kirkland, Donald	   Nutrients		MAFF
Dr. Schneider, Bernd	   CO2			IOW
Thomas, Helmut		   CO2			IOW
Prado-Fiedler, Ronaldo	   CO2			IOW
Dr. Bayer, Reinhold	   Tracer		IUP-HD
Dr. Born, Matthias	   Tracer		IUP-HD
Müller, Franziska	   Tracer		IUP-HD
Gier, Eva-Maria		   Tracer		IUP-HD
Dr. Rhein, Monika	   CFCs			IfMK
Haie, Petra		   CFCs			IfMK
Badewien, Thomas	   CFCs			IfMK
Dr Röd, Erhard		   Ship's Meteorologist	SWA
Lambert, Hans-Peter	   Weather Technician	SWA


2.4  PARTICIPATING INSTITUTIONS

BIO	Bedford Institute of Oceanography, P.O.B. 1006, Dartmouth, N.S., B2Y 4A2, 
	Canada
BSH	Bundesamt für Seeschiffahrt u. Hydrographie, Bernhard-Nocht-Str. 78, 20597 
	Hamburg, Germany
CSNSM	Centre des Spectrométrie Nucléaire et de Spectrométrie de Masse (IN2P3-CRNS), 
	Bâtiment 108, 91405 CAMPUS ORSAY, France
DWD	Deutscher Wetterdienst, Seewetteramt, Bernhard - Nocht - Str. 76, 29359 
	Hamburg, Germany
Geomar	Forschungszentrum für marine Geowissenschaften der Christian-Albrechts-
	Universität zu Kiel, Wischhofstr. 1-3, 24148 Kiel, Germany
IfMHH	Institut für Meereskunde der Universität Hamburg, Troplowitzstr. 7, 22529 
	Hamburg, Germany
IfMK	Institut für Meereskunde an der Universität Kiel, Düsternbrooker Weg 20, 
	24105 Kiel, Germany
IHF	Institut für Hydrobiologie und Fischereiwissenschaft, Universität Hamburg, 
	Zeiseweg 9, 22765 Hamburg, Germany
IOSDL	Institute of Oceanographic Sciences, Deacon Laboratory, Wormley, Godalming, 
	Surrey GU8 5UB, United Kingdom
	now: Southampton Oceanography Centre, Empress Dock, Southampton, Hampshire, 
	SO14 3ZH, United Kingdom
IOW	Institut für Ostseeforschung, Seestr. 15, 18119 Rostock-Warnemünde, Germany
IUP-B	Universität Bremen, Fachbereich 1, Institut für Umweltphysik, Abt. Tracer - 
	Ozeanographie, Bibliotheksstrasse, 28359 Bremen, Germany
IUP-HD	Institut für Umweltphysik der Universität Heidelberg, Im Neuenheimer 
	Feld 366, 69120 Heidelberg, Germany
MAFF	Ministry of Agriculture, Food and Fisheries, Fisheries Laboratory, Lowestoft, 
	Suffolk NR33 0HT, United Kingdom
MPICh	Max-Planck-Institut für Chemie, Abt. Biogeochemie, Postfach 3060, 55020 
	Mainz, Germany
UBMCh	FB-2 Meereschemie, Universität Bremen, Postfach 330440, 28334 Bremen, Germany
UHIBL	Institut für Biochemie, Universität Hamburg, Martin-Luther-King Pl. 6, 20146 
	Hamburg, Germany
IORAS/PPS P.P. Shirshov Institute of Oceanology, 23 Krasikova str., Moscow 
	117851, Russia
SIO	Scripps Institution of Oceanography, University of California, San Diego, La 
	Jolla, CA 92093, USA
WHOI	Woods Hole Oceanographic Institution, Woods Hole, Ma 02543, USA



3  RESEARCH PROGRAMMES

3.1  OMEX PROGRAMMES

The OMEX project is funded by the European Union within the frame-work of MAST 
II ("Targeted Projects").  The various multinational and interdisciplinary 
programmes focus on the exchange processes of carbon and a variety of gases - 
which occur to be relevant to climatic changes - between European shelf areas, 
the adjacent continental margin and open ocean.  Special emphasis is paid on 
exchange processes at the sediment/water and ocean/atmosphere interfaces.  The 
Celtic Margin at the Goban Spur (Fig. 1), where leg M30/1 took place, was chosen 
as a regional focus of the OMEX project for the time span 1993-1995.  The cruise 
M30/1 was part of a series of cruises of various European research vessels 
organized to gain a seasonal coverage of the sampling stations on the Goban Spur 
Transect.  It was intended to investigate a typical autumn situation for the 
different processes.


3.1.1  ORGANIC MATTER DEGRADATION, DENITRIFICATION AND TRACE METAL DIAGENESIS
       (UBMCh, W. Balzer)

For the understanding of the major controls over release fluxes from margin 
sediments a detailed investigation of early diagenetic processes acting within 
the sediments is necessary.  Therefore, extensive work on pore water chemistry 
and on solid sediment phases at transects across the continental margin was 
conducted.  The integrated rate of organic matter remineralization in near-
surface sediments will quantified by modelling the pore water profiles obtained 
during M27.  In dependence on both the diagenetic redox milieu and the input 
terms, the benthic reactions and fluxes of selected trace metals were 
investigated to assess the significance of margin processes for the trace metal 
chemistry of the ocean.  By analysing the trace metal content in trapped 
particles, in suspended material, in sediments and in pore waters we will 
contribute to finding relationships between vertical/lateral sedimentation 
fluxes, benthic release fluxes and burial rates of chemically differing 
elements.  A special study deals with sedimentary denitrification in continental 
margin sediments.


3.1.2  CARBON MINERALIZATION BY THE BENTHIC COMMUNITY
       (GEOMAR, O. Pfannkuche; IHF, H. Thiel)

Rates of remineralization of organic carbon in the benthal are controlled by all 
transport processes in the water column.  Parametrization of benthic processes 
is necessary to determine what portion of the sedimenting carbon is 
remineralized and what portion is accumulating in the sediments.  The 
understanding of the biological, chemical and physical processes involved and 
their quantitative determination is vital for balancing carbon fluxes in the 
sediment.  For the assessment of the role of benthic organisms for carbon 
cycling it is necessary to determine benthic community respiration, biomass 
production and benthic activity.  Present knowledge obtained from deep-sea 
investigations of the temperate Atlantic Ocean suggests that benthic 
respiration, activity and biomass production is subject to strong seasonal 
variations which correlate with carbon input by sedimentation.  The largest part 
of benthic carbon removal is by organism respiration, its seasonal range being 
80-90%.  The determination of in-situ benthic oxygen respiration rates by use of 
"bottom landers" is therefore of central significance for balancing the carbon 
fluxes.  Since most of the biotic oxygen consumption is performed by micro-
organisms, it is necessary to determine the part played by micro-organisms in 
community respiration and biomass production.  The main objective of this 
project is the quantification of biological mediated carbon fluxes through the 
sediment measuring benthic oxygen consumption rates, metabolic activity and 
biomass production on a seasonal scale.


3.1.3  VERTICAL PARTICLE FLUX AT THE CONTINENTAL MARGIN
       (IfMK, B. v. Bodungen)

The overall goal is the investigation of the seasonal pattern of particle 
sedimentation from the epipelagic zone to the sea floor and its dependence on 
the water depth at transects from the shelf edge to the abyssal plain.  It is 
intended to identify the quality and relative significance of the different 
source materials.  Therefore, the particle flux at different water depths were 
determined with high temporal resolution by using sediment traps.  In the 
sedimenting material the following components and parameters have been 
determined: carrier phases, 15N/14N isotopic ratios, pigments, stable carbon 
isotopes, and trace elements.  Light and electron microscopy was used to 
identify individual particles.  In relation to the particulate fluxes of carbon 
and nitrogen as measured with traps, DOC- and DON-measurements of water samples 
serve to assess the significance of dissolved organic components for the cycling 
of carbon and nitrogen.


3.1.4  PHASE TRANSFER OF ORGANIC COMPOUNDS DURING SHELF EDGE PASSAGE
       (UHIBL, Uwe Brockmann)

At the shelf edge, nutrient rich water masses are injected into the euphotic 
zone due to upwelling processes.  Here, inorganic components are rapidly 
transformed into particulate organic material, a part of which sediments to the 
sea floor where it is subject to remineralization.  The spatial distribution of 
these processes depends to a large extent on advective processes at the shelf 
edge.  Provided that currents are directed consistently to the shelf edge, the 
succession of individual processes can be traced by analysing the distribution 
of nutrients as well as the distribution of the dissolved and particulate 
organic components.  Because the different nutrient elements are remineralized 
at different rates, gross inferences on the state of the biological development 
may be drawn from measured element ratios in both the dissolved nutrients and in 
the dissolved/particulate organic substances.  These investigations are closely 
related to hydrographic studies and to an ecosystem analysis at the shelf edge 
of the selected region.


3.1.5  FLUX OF TRACE GASES AT THE BOUNDARY BETWEEN OCEAN AND ATMOSPHERE
       (MPICh, M. Andreae)

In collaboration with other European research groups the biogeochemical 
processes were investigated that are involved in the production and emission of 
trace gases being selected according to their relevance for climate and 
atmospheric chemistry.  In continuation of measurements during the METEOR cruise 
M21/2 the photochemical production of carbonyl sulphide (COS) in the ocean and 
its exchange flux between ocean and atmosphere was determined.  COS is produced 
from certain dissolved organic compounds and may be emitted to the atmosphere.  
Due to its long life time of more than one year, COS may reach the stratosphere 
where it forms the main source of the sulphate layer which influences both the 
ozone layer and the incoming solar radiation.  Of particular significance in 
this context is the seasonal and spatial variability of the ocean as a source of 
COS.  During M27/1 a photochemical/kinetic model was tested and now improved 
that considers light dependent production of COS, hydrolysis of COS and its 
exchange at the ocean/atmosphere interface as well as vertical mixing in the 
ocean.


3.2  WOCE PROGRAMMES:

3.2.1  DETERMINATION OF THE MERIDIONAL TRANSPORTS OF HEAT, SALT AND FRESHWATER 
       AT 48°N IN THE NORTH ATLANTIC ALONG THE WHP SECTION A2
       (BSH, K.P. Koltermann)

The meridional transports of heat, freshwater and salt in the Atlantic Ocean and 
their seasonal and interannual changes are determined for the 90s across the 
latitude of the global maximum freshwater transport at ca. 50°N in the Atlantic 
Ocean.  These results are compared with previous measurements in the 50s and 
80s.  This "time series" is augmented with Russian data along 48°N that have 
been collected at quarterly intervals between 1975 and 1987 down to a depth of 
2000 m.  This will result in a climatology of the changes in the surface and 
intermediate layers and will improve the estimate of the seasonal cycle.  
Comparisons with results from eddy-resolving modelling efforts are separately 
pursued.

These estimates will provide the variance of these integral parameters, and 
finally lead to a history of their development since the IGY in 1957.  This 
section elucidates the interaction of the thermohaline North Atlantic 
circulation with the wind-driven one at intermediate and great depths.  
Furthermore we expect a better formulation of the coupling between these changes 
and the changes in the "forcing fields", particularly the fluxes of latent and 
sensible heat, evaporation and precipitation E-P and wind stress from 
operational atmospheric models (ECMWF, NMC) at the surface.  The WOCE-NORD 
project will in addition document estimates of the temperature distribution and 
heat content at ca. 50°N for the top kilometre on time scales of months from its 
VOS subprogramme to establish their seasonal cycle.  In co-operation, we will 
attempt to complement the circulation estimates of the convective area north of 
48°N with the estimates from this section.

Working this section in the summer of 1993 with FS Gauss has shown the Labrador 
Sea Water temperatures some 0.4°C below its historical characteristic 
temperature, and deeper in the water column by some 700 m.  This fits in with 
observations from the early 90s along 60°N and 24°30'N and indicates a rapid 
reaction of the intermediate circulation of the northern North Atlantic to 
changes in the forcing in the Labrador Sea.  We expect to get some first 
estimates on how changes in the heat, salt and freshwater transports of the 
boundary currents of the North Atlantic continue into the ocean interior, and 
what likely impact this will have on the coupled ocean-atmosphere system.


3.2.2  NUTRIENTS MEASUREMENTS FOR THE FINE RESOLUTION OF OCEANIC WATER MASSES ON 
       THE METEOR CRUISE M30/2 (SECTION WHP-A2) IN THE NORTH ATLANTIC
       (IfMK, J. Duinker, L. Mintrop)
      
The concentrations of nutrients PO4, NO3, NO2, NH4, Si(OH)4 from 1692 samples 
and the content of dissolved oxygen O2 from 1737 water samples have been 
determined on board according to the WHP Standards.  For quality assurance 
purposes additional samples were taken as duplicates or replicates.  All data 
were 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.


3.2.3  CFCS ON THE SECTION WHP-A2
       (IUP-B, W. Roether)

On all stations of the WOCE WHP section A2 water samples from all depths were 
analysed for CFCs.  Some 1100 measurements of F11, F12, F113 and CCl4 have been 
processed.  These data will be used to determine mixing rates and apparent ages 
of the water masses in the North Atlantic.  Sampling and interpretation will be 
done in close co-operation with all groups involved.

For running the CFC analyses onboard 

(1) 1062 samples for CFC have been collected and analysed for F11, F12, F113, 
    CCl4. All analyses have been evaluated preliminarily at sea.
(2) In addition 77 3He-samples have been collected (classical method) for inter 
    comparisons with the Heidelberg group.

All samples were collected with the standard rosette system.  The CFC-samples 
were drawn on large glass syringes.  During sampling, contamination with helium 
and CFCs was to be avoided or controlled.  The sampling strategy on the section 
followed the WOCE recommendations. Except for shallower areas each station was 
sampled at up to 36 levels.  The vertical resolution had a higher priority than 
the horizontal one for the case the throughput of the CFC-system was limited.  
The deep boundary currents, particularly in the western part of the section, 
were of special interest.


3.2.4  MOORING RECOVERY ON SECTIONS WHP-A2 AND WHP-A1
       (BSH, K.P. Koltermann and IfMHH, J. Meincke)

On the Gauss cruise 226 an array of three mooring was deployed west of the Mid-
Atlantic Ridge an section WHP-A2 in the summer of 1993 to measure the vertical 
and horizontal extend of a deep high salinity boundary current and its temporal 
changes.  Previous attempts to recover these mooring had failed as there seem to 
are problems with the acoustic releasers.  On this cruise another attempt for 
recovery was planned, depending on the prevailing weather situation and time 
availability.

On WHP-A1 the mooring D2 was deployed to measure the vertical structure of the 
depth controlled current.  Several attempts to recover the mooring acoustically 
had failed.  On the leg M30/3 another attempt to recover the mooring by dredging 
was not successful.  Further attempts to dredge for other moorings on this 
section had to be abandoned for weather reasons.


3.2.5  TRITIUM/HELIUM AND 14C-SAMPLING ALONG WHP-SECTIONS A2 AND A1
       (IUP-HD, R. Bayer)

The zonal section along 48°N (WHP-A2) was sampled for the first time for a 
detailed analysis of helium, tritium and 14C signals.

Comparing the 1972 GEOSECS data in the Northwestern Atlantic with the TTO/NAS 
data in 1980-81 has shown a prominent invasion of the transient tracer signals 
from the surface into the deep waters.  An additional survey of these tracer 
fields in 1994 (WHP-A2) gives further indications on how much and how fast this 
invasion has proceeded.  This will help to parameterize the renewal rates for 
the individual deep basins.  Clear horizontal gradients of higher tracer signals 
in the West are seen.  The deep western boundary currents with the most recent 
and youngest waters are clearly evident, showing similar features as on the A1 
section sampled in 1991.  A detailed survey of these gradients along the 
sections and the meridional connection of the tracer signals in the Deep Western 
Boundary Currents are of particular interest.

On WHP-A2 474 helium and tritium samples have been collected. In addition 311 
helium samples have been taken to test a sea-going extraction facility.  Of the 
51 stations sampled a denser coverage was attempted for the western boundary 
currents, but had to be aborted due to bad weather but succeeded across the Mid 
Atlantic Ridge, with an even station distribution along the rest of the section.

In parallel to the large volume 14C-sampling we sampled for AMS-14C-analyses.  
The large volume samplers are used at the relevant stations in two casts: the 
shallow cast was followed by the CTD-rosette cast for small volume samples to 
give time for the 14C-extraction and the subsequent preparation of the large 
volume samplers for the deep cast for 14C.  As experienced in recent years in 
our polar work a complete 14C station was worked in about 5 hours (ca. 20 LVS 
samples at 4000 m water depth).  For the 48°N section 8 LVS stations with 204 
LVS samples and 60 samples for AMS-14C have been worked.

Sampling on WHP-A1 (West and East) followed for the Eastern part largely the 
1991 strategy and results. Some 400 helium and tritium samples were analysed 
ashore.  We used the seagoing extraction facility with great success.  Similar 
to the sampling strategy on the previous leg on A2, sampling focused on the 
basin boundaries with ca. 25 stations in total.  We tried to resolve the 
temporal and seasonal variability of the tracer signatures in order to compare 
them with existing data from the European Polar Seas and work done further south 
within the frame-work of WOCE.  This also applies for the work in the Labrador 
Sea on A1 West.  Here we had planned ca. 100 samples for helium and tritium, and 
3 stations for LVS-14C work but succeeded only in working 2 stations due to bad 
weather.


3.2.6  WOCE NORTH ATLANTIC OVERTURNING RATE DETERMINATION (WOCE-NORD, WHP 
       section A1)
       (IfMHH, J. Meincke and BSH, A. Sy)

The meridional transports of heat and matter in the North Atlantic are 
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 intermediate and 
greater depths and spreads further south, forming the source water masses of the 
North Atlantic Deep Water.  This "overturning" process is regarded as the main 
driving mechanism for the global thermohaline circulation. Quantifying both 
input and output in the North Atlantic overturning system will help to improve 
modelling the role of the ocean in the climate system.

Leg M30/3 is part of the WOCE-NORD project, running over six years.  To extend 
the data basis needed to calculate the transport rates involved in the 
overturning process, sections have been repeated seasonally between Ireland and 
South Greenland.  A combination of current measurements from the ship in motion, 
long-term moorings of current meters and surface topographies from altimeter 
data are being used.  This leg M30/3 was the third repeat of the WOCE 
hydrographic section A1E/AR7E.  Extending this time the work to the western part 
A1W together with the work on A2 improves the transport estimates using inverse 
modelling.

Along a section through the Labrador Sea Basin (A1W) from Hamilton Bank to South 
Greenland and continuing on a section from South Greenland to Ireland (A1E) we 
observed the fields of the classical hydrographic parameters pressure, 
temperature, salinity, content of dissolved oxygen and nutrients (NO3, NO2, PO4, 
SiO3).  The work along A1E was, except for weather "gaps", an identical repeat 
of the work on Meteor cruise M18 (September 1991).  The work programme followed 
the strategy used during the previous leg M30/2 and all instruments and 
procedures were continued.  Only for nutrients and oxygen work other groups 
joined in St. John's employing their own slightly modified procedures.  All 
data, particular the CTD data, were processed on board, except for applying 
post-cruise laboratory calibrations to the pressure and temperature sensors.


3.2.7  CFCS ON THE SECTION WHP-A1
       (IfMK, M. Rhein)

On the third leg of M30 we determined the tracer characteristics of the water 
masses that have spilt over the ridge system between Greenland and Iceland 
(DSOW) and between Iceland and the Shetlands (ISOW).  After leaving the ridges 
these denser masses sink to the bottom and entrain ambient water masses.  The 
extent of the mixing and the changes of the water mass characteristics after 
leaving the ridges are also a focus of these investigations.  The data will be 
used to improve the parameterisation of the Deep Water formation process north 
of the ridge system and to derive at better mean spreading velocities for 
individual water mass components.  Other tracer and oceanographic data will be 
used as well.  Besides the overflow water masses we also sampled the newly 
formed deep water from the Labrador Sea, both at the exit of the Labrador Sea 
and along its spreading paths in the Irminger Sea and the North-Eastern Atlantic.

On all stations of the WOCE section WHP-A1 water samples from all depths were 
analysed for CFCs. Some 1800 measurements of F11, F12, F113 and CCl4 have been 
processed. These data will be used to determine mixing rates and apparent ages 
of the water masses in the North Atlantic. Sampling and interpretation will be 
done in close co-operation with all groups involved.


3.3  JGOFS- PROGRAMME

3.3.1  THE CONTROL FUNCTION OF THE CARBONATE-SYSTEM IN THE OCEANIC CO2 UPTAKE, 
       WHP-A2
       (IfMK, J. Duinker, L. Mintrop)

Measuring pCO2, total carbonate and alkalinity we investigated the CO2 exchange 
between ocean and atmosphere in a regional and seasonal resolution to contribute 
to a global budget.  In parallel these data will be used together with 
measurements of the 13C-signal to follow the spreading of the anthropogenic 
CO2-signal in the ocean.

We used on the WHP section A2, M30/2 the experience of our previous WOCE cruise 
Meteor M22/5 along 30°S (WHP-A10).

(1) Sampling
    ~ Sampling for alkalinity and total carbonate ca. once every 24 h (i.e. 
      every third or fourth CTD station in parallel with the tracer sampling),
    ~ sampling for 13C-measurements in total on 23 stations ( 359 samples),
    ~ surface sampling from the clean sea water system along the cruise track 
      every 30 to 60nm.
(2) Measurements
    ~ direct measurements on board of alkalinity and total carbonate,
    ~ in parallel we used a continuous system to measure the CO2 partial 
      pressure.


3.3.2  THE OCEAN AS A CO2 SINK: COMPLIMENTARY STUDIES OF THE BALTIC SEA AND THE 
       NORTH ATLANTIC, WHP-A1
       (IOW, B. Schneider)

Measuring the parameters pCO2, total carbonate and alkalinity we will, in 
combination with oxygen and nutrients data describe the CO2 exchange between the 
ocean and the atmosphere in the North Atlantic in early winter.  The results 
from the WHP section A1 of leg M30/3 are compared with similar measurements in 
the Baltic Sea to differentiate between the CO2 systems of two ecologically 
different marine environments.

(1)  Continuous measurements of the CO2 partial pressure along the entire 
     ship's track from St. John's into the North Sea (M30/3).
(2)  Measurements of total carbonate on water samples of the WOCE stations 
     along the sections A1W and A1E. We processed ca. 40 samples/d.


3.4  INDIVIDUAL PROJECTS

3.4.1  129I FROM NUCLEAR FUEL PROCESSING AS AN OCEANOGRAPHIC TRACER
       (CSCSM-CNRS, G. M. Raisbeck)

On the two legs M30/2 and M30/3 water samples were taken to determine the 129I 
concentration.  This nuclide originates from the nuclear fuel reprocessing 
system and has shown some interesting facets used as an additional oceanographic 
tracer.  Previous work in the North Atlantic has as yet not been satisfactory to 
provide an adequate signal/noise ratio to assess its information content in 
oceanographic applications.

129I measurements, using AMS techniques, have been taken from seaweed and 
seawater along the European coasts and waters.  From the 129I/127I ratios we 
have been able to demonstrate spreading pattern from this man-made tracer.  
First examples from the North Atlantic show that 129I can be used to 
differentiate sources other then those associated with tracers already used in 
oceanography.  With samples from this cruise on WHP-A2 and WHP-A1 we would like 
to develop an estimate of the dynamic range this signal has in the full-depth 
ocean and evaluate if the information contained in these data is useful to 
describe water masses, their fate and behaviour.


3.4.2  PROFILING ALACE FLOATS TO DETERMINE THE DEVELOPMENT OF THE STRATIFICATION 
       IN THE LABRADOR SEA OVER TWO YEARS
       (SIO, R.Davis and WHOI, B.Owens)

On the leg M30/3 six ALACE (Autonomous Lagrangian Circulation Explorer) floats 
for two US-American groups (SIO/WHOI) were deployed in the Labrador Sea to 
determine the velocity field at a pre-selected depth level of 1500dbar over more 
than two years.  These floats surface at regular weekly intervals to radio their 
position and data from their drift and ascend and descend phases to a satellite.  
This provides information besides the float track-derived velocities, on the 
evolution of the profiles of temperature and salinity with time.

For two years we will follow the evolution of the Labrador Sea stratification 
for the top kilometre with profiling ALACE floats (P-ALACE).  They are deployed 
across the Labrador Sea gyre and part of the boundary current regime and surface 
at weekly intervals to report profiles of temperature (5 floats) and temperature 
and salinity (one float) via satellite.  The tracks will give a first glance at 
the velocity field of the gyre and its changes.  We will use this information 
for planning a convection experiment in 1996.  Some other ALACE floats with 
RAFOS transducers will be deployed to test the effective sound ranges with the 
existing Newfoundland Basin array.  Experience from the Arctic has shown that we 
have to consider reduced ranges in this region.  The results are needed to 
design a RAFOS array for work from 1996 onwards.

Fig. (1) Track and Station map of Meteor leg M30/1
         star: moorings,dot: benthic station, arrow: cruise track



4  NARRATIVE OF THE CRUISE

4.1  Leg M30/1
     (Chief Scientist O. Pfannkuche)

FS Meteor left Las Palmas on the evening of Sept. 6, 1994 heading north for the 
first station at 49°N, 16°30'W on the Porcupine Abyssal Plain.  En route the 
ship stopped 3 times in international waters on the Iberian Abyssal Plain in 
order to test a new version of the multiple corer and the CTD/Rosette system.  
On Sept. 12 at 0400h we started to work at the first station at the Porcupine 
Abyssal Plain.  After water sampling and CTD profiling the sediment trap mooring 
of the Institute of Oceanographic Sciences, UK, which was deployed in spring 
1994, was successfully retrieved.  A series of multiple corer samples followed.  
In the afternoon the refitted sediment trap mooring was deployed again and 
Meteor headed east for the next station at the bottom of the continental rise.  
Besides sediment and water sampling a new sediment trap mooring (OMEX IV) was 
deployed.  From now on sampling stations followed the contours of the 
continental slope (Fig. 1) from the Pendragon Escarpment (water depth 3600 m) up 
to the Great Sole Bank  (water depth 220 m).  Station work on the Pendragon 
Escarpment had to be interrupted on Sept. 13 until the afternoon of Sept. 14 as 
a storm (8-9 Bft) prevented the use of any sampling gear.  On all slope stations 
sampling followed the same routine: sediment samples with box grab and multiple 
corers, water samples with Go-Flow bottles, a Niskin bottle rosette sampler and 
a marine snow catcher (only one haul), and CTD profiling.  Two more sediment 
trap moorings of the OMEX project were successfully retrieved and re-deployed 
after refitting.  OMEX III at 3670 m on the Pendragon Escarpment on Sept. 15 and 
OMEX II at 1418 m on the upper slope on Sept. 16.  A free vehicle grab 
respirometer (bottom lander) was moored on the Pendragon Escarpment for two days 
(Sept. 13 - 15).  At 1700h on Sept. 17 station work was finished on the outer 
Great Sole Bank and METEOR headed back to Germany.  The cruise M30/1 ended at 
0800h on Sept. 21, in the port of Bremen.


4.2  Leg M30/2
     (Chief Scientist K.P. Koltermann)

FS Meteor left its berth in Hamburg after a routine shipyard refit in thick fog 
on Oct 12, 1994 at 0900.  After a smooth transit with increasing visibility, the 
first station (#436) for testing all equipment was worked on Oct. 15, 1994 from 
1232 UTC on 48°09.9'N, 11°44.9'W on 3420 m depth in international waters.  On 
Oct 16, the first station of the trans-Atlantic transect was begun at 0444 UTC 
on 49°14.1'N, 10°39.9'W and a depth of 153 m.  The first autumnal gales caught 
up with us already the next day, where winds of S10-11 Bft stopped station work.  
Weather-related breaks were used to find the optimum combination of rosette, 
underwater command module and CTD.  Several attempts to dodge the weather and 
use lower wind speed periods where unsuccessful, so that we could only return to 
the planned station in the morning of Oct 20, 1994.  Work progressed until the 
evening of the next day, when the ship again had to weather winds from the West 
with 10-11 Bft.

The next week saw better progress westward.  On Oct 27 an attempt to dredge for 
the mooring K1 west of the Mid-Atlantic Ridge was not successful, although the 
mooring had responded to acoustic signals. Moorings K2 and K3 were acoustically 
located but did not release.  No dredging attempts were made.  Increasing winds 
prohibited station work afterwards until Oct 29, although that station had to be 
interrupted again for heavy winds.  This stop-and-go station work continued 
until Nov 8.  Station spacing had to be adjusted to allow for distance made west 
during gales and time lost.  Time had also to be used either to return to a 
planned station position when the position had been overrun or heave to at a new 
position and wait for the weather to calm down.  While work was stopped at times 
by heavy weather east of the Mid-Atlantic Ridge, work was only possible in the 
"weather windows" between a succession of depressions west of the ridge.  In the 
westernmost part of the section up onto the Grand Banks the number of stations 
had to be reduced severely as time was running out when the extra-tropical storm 
"Florence" hit the area.  This decision was made easier as the CCS Hudson had 
worked that part only days earlier during recovery of an extended mooring array.  
The last two stations of the section could be worked as planned, and in transit 
an extensive set of deep XBT casts will provide the essential continuity between 
stations.  Work was finished on Nov 10, 1994 at 0059 UTC and the ship made for 
St John's, Nfld where she arrived on Nov 12, 1994 at 0600.  A total of 53 
stations with 82 rosette casts was worked instead of the planned 82 stations 
(Fig. 2).

Fig. (2) Track and station maps of Meteor legs M30/2 (WHP-A2) and M30/3 (WHP-
         A1). Top panel: hydrographic stations and numbers, bottom: XBT stations 
         and numbers


4.3  LEG M30/3
     (Chief Scientist J. Meincke)

Following three days in port for exchanging the scientific party, setting up the 
laboratory installations, hand-over meeting with the previous party and visits 
between the ship and local scientific institutions at the St. John's Memorial 
University and the Northeast Fisheries Center, the ship left St John's on Nov 
15, 1994 at 1400.  A test-station for the CTD-Rosette systems was carried out en 
route to the starting position for the Labrador Sea section WOCE A1W on Hamilton 
Bank. Station work only began on Nov 18, at 0600 since a NW-gale stopped any 
progress for 20 hrs during Nov 16/17.  Stations 490 to 496 over the Canadian 
continental slope were completed on Nov 19, 1200 when the weather forecast 
strongly recommended to leave the Canadian side and change over to the Greenland 
side of the Labrador Sea as fast as possible.  During the transit four P-ALACE 
(Profiling Autonomous Lagrangian Circulation Explorers) were deployed and 2000 m 
XBTs were launched every 20 nm.  The following two days were dominated by strong 
winds at temperatures around the freezing point, only one station (497) could be 
completed.  From Nov 22 onwards regular station work resumed, starting in the 
convective regime of the Labrador Sea and crossing the boundary current regime 
towards the Greenland shelf (stations 498 -505).  Again the weather forecast 
determined to finish activities in the Labrador Sea and take up the WOCE line 
A1E from east of Kap Farvel to Ireland.  Therefore we had to leave the section 
A1W uncompleted in its central part and sailed around Kap Farvel.

Station work resumed on Nov 24 at 2200 on the eastern Greenland shelf (stat 506) 
down the slope into the Irminger Basin, but had to be interrupted following 
station 511 for Nov 26 and 27 because of a severe gale.  However, we experienced 
a full week of moderate winds and seas and completed stations 512 - 537 until 
Dec 4, 1994.  This phase included 12 hours on Dec 2 of unsuccessful dredging for 
the current meter mooring D2 which had been deployed in 1992.  Three previous 
recovery attempts in 1993 and 1994 had already failed.

The next phase of severe winds and seas started on Dec 5 in the area 53°N, 24°W.  
On Dec 6 we experienced the highest wind speeds (100 kts) and highest seas (12 
m) during this cruise.  On Dec 9 a continuation of these conditions until at 
least Dec 14 became evident from the long- and medium-range numerical weather 
predictions.  We decided to give up to complete of this WOCE section and return 
to Hamburg.  At 2000 the ship started to head east, launching XBTs every 15nm 
and XCTDs every 30nm.  However, on the morning of Dec 10 the numerical forecasts 
changed radically and predicted the development of a high pressure ridge over 
the operation area to stabilize for a few days from Dec 12 onwards.  This chance 
was to be taken, the ship turned around and indeed from Dec 12 to Dec 15 0600 
the WOCE section was completed in fine weather conditions (stations 538 - 551).

Since a few series of intense atmospheric depressions was announced to move into 
the operations area for Dec 16, the original plans to dredge for further 
moorings with release malfunction were given up.  The ship made for Hamburg were 
it docked on Dec 19, 1994 at 0100 LT.



5  OPERATIONAL DETAILS AND PRELIMINARY RESULTS

5.1.  OMEX PROGRAMMES

5.1.1  BIOCHEMISTRY

~ PHASE TRANSFER OF ORGANIC COMPOUNDS DURING SHELF EDGE PASSAGE
  (UHIBl, I. Büns, A. Pfeifer and U. Brockmann)

Within the biogeochemical transfer and transformation processes in the area 
across the shelf edge, nutrients and organic compounds are key parameters.  
During the cruise, water samples were taken from defined depths at fixed 
stations on a west-east profile along the Goban Spur.  The samples were 
filtrated and conserved for a later analysis, since besides oxygen titration, pH 
and photometric measurements, no chemical analysis could be done on board.  
Sampling should be done with a multi-bottle-rosette (24), connected to a CTD 
probe (Oceanography, Kiel).  A test-run at station 423 was successful.  
Unfortunately, this was the only station, where multi-bottle-rosette and probe 
worked properly!  We have to thank Prof. Balzer for the use of their GO-Flow 
rosette as a temporary replacement for the multi-bottle-rosette at some 
stations!  Furthermore, they took care that another multi-bottle-rosette 
(University Bremen), which was stored on board, could be used later.

Fig. (3a) Nitrate (including nitrite) profiles. This diagram is dominated by 
          the variations of nitrate. In general, there was a strong gradient 
          (0.1 - 9.5 mol/l), increasing with depth, already in the euphotic 
          zone. At station 430 a peak was observed in 30 m depths.

At station 425/IOS (depths > 4800 m), when multi-bottle-rosette and CTD totally 
failed, only 5 samples with the GO-Flows down to 200 m could be taken.

Station 426/OMEX IV: multi-bottle-rosette and CTD still did not work; because of 
lack of time the GO-Flows couldn't be used.

At station 427/OMEX III the CTD probe was run separately; the multi-bottle-
rosette still refused to work properly.  As there was no time for a separate 
sampling, we got part of the samples of Prof. Balzer, but the total volume that 
we actually needed for the filtration was not available.

Station 428/F: another trial, to run the multi-bottle-rosette from Bremen 
together with the CTD failed.  We got samples from the GO-Flows, but as the 
interval between sampling and the time where we got our subsamples was too long, 
we couldn't use them.

At the station 430/OMEX II the CTD probe and the multi-bottle-rosette were run 
separately.  Finally, success!

At the stations 433/B 1, 434/OMEX 1 and 435/A sampling now was successful.


METHODS:
A vacuum filtration was run with controlled 0.2 bar at 9 filtration stands.  
Depending on the concentration of suspended matter, volumes from 750ml to 1750ml 
were filtrated over Whatman GF/C filters for the determination of CHN, part. P, 
part. CH and dry weight.  An additional filtration stand was used for volumes up 
to 5 l for each filter for the determination of lipids.  All filters were stored 
frozen at -17°C.  The filtrate was fixed with mercury-(II)-chloride (0.01% w/v) 
and stored in glass and polyethylene bottles in a cooling chamber for a later 
analysis of nitrate, nitrite, phosphate, silicate and ammonium.  A wet-chemical 
oxidation method was used to prepare samples for determination of total 
dissolved nitrogen and phosphorus.  Immediately after sampling, measurements of 
turbidity (Turner nephelometer), pH (WTW pH 91) and fluorescence (Turner 
fluorometer and 1 Hz fluorometer) were conducted.  Oxygen was determined by 
Winkler titration with a Metrohm titration stand.


FIRST RESULTS:
The following diagrams (Fig. 3a-c) show nutrient-depth profiles for the sequence 
of stations from west to east.  The profiles consist of raw data, not yet 
controlled.  In general, the profiles show high nutrient concentrations within 
the deep water masses and low values due to nutrient consumption in the euphotic 
zone in the mixed layer.

~ ORGANIC MATTER DEGRADATION, DENITRIFICATION AND TRACE METAL DIAGENESIS.
~ DISSOLVED AND PARTICULATE TRACE ELEMENTS 
  (UBMCh, W.Balzer, A.Deeken, H.Dierssen)

Within the OMEX-project on trace element cycling at the Celtic margin it is our 
task to determine the fluxes and reactions near the sediment/water interface.  
In order to gain a link to water column processes, the distribution of dissolved 
trace elements in the pore water and solid sediments has to be compared with 
their concentration in the water column and its suspended particulate material 
(SPM).  During M30/1 the main objectives were to investigate for a summer 
situation whether dissolved Al and suspended particles (eventually resuspended 
from the sediments) are injected from the margin into the open ocean and whether 
they affect the trace element chemistry of the open ocean.  Two particulate 
phases were sampled using different techniques: (i) the SPM filtered by using 
in-situ pumps is supposed to consist of slowly sinking biogenic and terrestrial 
detritus exhibiting a large surface area for sorptive processes, (ii) the 
sediment representing the ultimate result of all water column processes and 
early diagenetic modifications near the sediment/water interface. 

Fig. (3b) Phosphate profiles. Starting in the euphotic zone, similar strong 
          gradients with increasing depths down to 1000 m characterized the 
          profiles (0.1 - 1 mol/l). Again a peak (0.6 mol/l) occurred at 30 m 
          depth at station 430.

Due to the low concentration of SPM below the mixed layer, large volumes of sea 
water were filtered for trace element determinations in SPM.  Between 250L and 
550L sea water were filtered through acid cleaned 293 mm Nuclepore filter using 
in-situ pumps.  To reduce contamination risks a non-metallic wire was used and 
all handling of the filters was performed under a clean bench within a clean 
room container.  Because in-situ pumping is very time-consuming pumps were 
combined with bottle casts whenever possible.  Due to limited ship time only 7 
filters were obtained from the Goban Spur transect at depths between 50 m and 
1450 m.  Another 3 filters were disrupted during deployment.  At all stations 
where in-situ-pumps were deployed and especially where sediment trap moorings 
were positioned, casts of GoFlo bottles were taken to analyse the vertical 
distribution of Al and eventually other trace metals in the water column.  For 
the trace metal studies precautions had to be taken against the risks of 
contamination: before use the GoFlo bottles were acid cleaned thoroughly, at 
station the bottles were attached to a non-metallic wire, during handling on 
deck both opening ends were covered with plastic bags, all manipulations after 
sub-sampling were performed under a clean bench.  During the cruise Al from 6 
stations was measured on board using a fluorometric technique.  The vertical and 
horizontal distribution will be compared with results from the particle 
analysis. 

Fig. (3c) Silicate profiles. The silicate gradients in the euphotic zone 
          started at 0.5 mol/l. In depths below 500 m the gradients were 
          comparable to those of nitrate and phosphate. Again a small peak could 
          be seen at 30m depth at station 430.

Solid sediments and pore water samples for the determination of dissolved trace 
metals were taken at 7 stations along the Goban Spur transect (see below).  On 
board ship the pore water samples were preserved after filtration and 
acidification; preconcentration and the separation from the salt matrix will be 
performed at the home laboratory.


~ DISSOLVED ORGANIC CARBON
  (UBMCh, S.Otto, W.Balzer)

In order to investigate dissolved organic carbon (DOC) in the water column 
across the continental margin, samples from seven CTD-rosettes or GoFlo casts 
were taken at the Goban Spur transect.  At each position the whole water column 
was sampled.  It is very critical in the determination of DOC to avoid 
contamination of the samples.  Therefore, great care was taken from the first 
step of sampling throughout the whole work-up procedure: samples from the 
rosette were taken in pre-cleaned glass bottles, immediately filtered through 
pre-combusted GF/F filters and finally acidified and sealed in brown glass 
ampoules.  All samples were stored at +4°C until analysis.  The DOC 
determinations were performed by the High-Temperature-Catalytic-Oxidation 
(HTCO).

In addition to the investigation of DOC in the water column, sediments taken at 
6 stations with a multi-corer were sampled to determine DOC in pore waters.  
After squeezing the sediment in a cold room, the pore water was analysed for DOC 
and for total inorganic carbon (TIC).  While TIC at the deeper stations was 
always close to 2 mmol/L it was much higher at the shallow stations showing a 
maximum of 5.6 mmol/L. DOC in the pore water varied between 0.8 and 2.6 mmol/L, 
again having higher concentrations at the shallower stations.


~ PORE WATER CHEMISTRY
  (UBMCh, W.Balzer, A.Deeken, H.Wellmann)

The OMEX-project was established to contribute towards the understanding of the 
cycling of nitrogen, carbon and trace metals at continental margins where 
benthic processes are expected to play a significant role for the chemistry of 
the whole ocean.  Necessary for the understanding of the major controls over 
release fluxes from boundary sediments is a detailed investigation of early 
diagenetic processes acting within the sediments.  It was therefore planned to 
conduct extensive work on pore water chemistry and on solid sediment phases at 
the Goban Spur transect across the Celtic margin.  From the sediments taken at 7 
stations (#425, #426, #427, #428, #430, #433, #434) by a multicorer, the pore 
water was squeezed or centrifuged under in-situ temperature conditions (cool 
room).  Nitrate as the pore water constituent providing most information about 
the diagenetic milieu, showed systematic variations in the profiles over the 
transect.  All nitrate pore water profile showed sub-oxic conditions typical for 
hemipelagic sediments of the North Atlantic ocean but there was also a 
significant contribution of sulphate reduction to organic matter degradation at 
the stations shallower than 1500 m.  The rates of carbon combustion by oxygen 
and nitrate, respectively, were assessed by use of a model for steady-state 
diagenesis of organic matter.  The rates for organic carbon degradation by 
oxygen decreased systematically with water depth with one exception: station 
#430 at 1500 m showed an extremely high rate which is consistent with benthic 
lander results obtained by Dutch colleagues.


~ BENTHIC DENITRIFICATION AND BIOIRRIGATION
  (UBMCh, W.Balzer, A.Deeken, H.Wellmann)

For the estimation of denitrification rates two independent methods were 
applied: (i) the evaluation of the rate from the modelling of the pore water 
nitrate distribution, and (ii) the direct determination according to the 
"acetylene-block" incubation method.  The pore water nitrate profiles can be 
used simultaneously to estimate integrated rates of denitrification, for the 
reaction being first order with respect to nitrate.  Denitrification was 
detectable but weak in the depth range from 5300 m to 3665 m but became much 
more intensive when the shallower region (1500 m to 670 m) was approached.

The determination of denitrification rates by C2H2-block incubation comprises 
the following steps: (i) sub-sampling a box-corer with several acrylic glass 
tubes, (ii) injection of acetylene into the pore water of the whole sediment 
column of the sub-cores to block the further reduction of the intermittently 
formed N2O to dinitrogen, (iii) sectioning of the sub-cores after appropriate 
incubation times, (iv) equilibration of the sediment sections with the gas phase 
in small closed jars after stopping the reactions with KOH, and (v) head-space 
analysis of the N2O concentration in the gas phase by GC-ECD.

Only 4 sediment stations (#428, #430 (OMEX II), #433 and #434 (OMEX I)) were 
selected for this lengthy procedure. For each station 6 sub-cores were used: 2 
sub-cores for an average N2O-profile, 2 sub-cores for an average 1-day-
incubation and 2 sub-cores for an average 2-day-incubation.  There was no N2O-
production at station #428.  The other 3 shallower stations showed intensive 
N2O-production close to the surface with maximum rates at the depth range 2-4 cm 
in all cases.  When comparing these rates with the denitrification rates 
obtained from pore water modelling two features deserve special attention: (i) 
considering the widely differing boundary conditions, assumptions, etc. of the 
two methods, the agreement within a factor of 3 is remarkable, (ii) there might 
be a difference in the process that is measured by the two methods: the pore 
water profile might correspond more to the long-term steady-state situation 
while the incubation might respond to seasonal effects more directly.

The N2O profiles in the pore-water (without incubation; from which release rates 
were calculated) showed highest concentrations near the sediment surface in all 
cores investigated. N2O release, however, is significant only in sediments of 
the upper continental margin again having a relative maximum at 1530 m as 
suggested by the relative heights of the rates obtained from incubation.  The 
relative heights of the N2O release rates can be estimated directly from a 
comparison of the profiles.  The absolute rates can only be calculated when the 
modelling of the tracer incubation experiments for the calculation of bio-
irrigation rates is finished - which is presently underway. 

Especially in the shallower parts of the continental margin, the release fluxes 
from the sediment surface might be enhanced by the bio-irrigating action of 
(bioturbating) macrofauna organisms.  To estimate the enhancement over molecular 
diffusion, tracer experiments were performed by applying a tracer in the 
overlying water and incubation of the sediment core at in-situ temperature.  
After 2-4 days the core was cut into slices and the tracer concentration was 
determined in the pore water.  By numerical modelling (using a "quasi-
diffusional" coefficient) the transport of the tracer into the sediment column 
can be followed and the best-fitting coefficient can be evaluated.


5.1.2  AIR CHEMISTRY

~ EXCHANGE OF REDUCED SULPHUR COMPOUNDS BETWEEN OCEAN AND ATMOSPHERE
  (MPICh, G. Uher, O. Flöck, G. Schebeske, V.Ulshöfer)

The biogeochemical processes, which are controlling the production of carbonyl 
sulphide (COS) and dimethyl sulphide (DMS) in surface seawater as well as their 
emission to the atmosphere were the focus of the biogeochemical investigations 
by our group.  These studies were accompanied by measurements of chlorophyll 
concentration, absorbance and fluorescence of dissolved organic matter on one 
hand, and of the atmospheric concentrations of condensation nuclei, black 
carbon, and radon (222Rn) on the other hand.  In the following sections some 
preliminary results are presented. 


~ COS IN SURFACE SEAWATER AND ATMOSPHERE
  (V. Ulshöfer)

COS is formed photochemically in surface seawater and is believed to be the main 
source of the stratospheric sulphate layer during periods of low volcanic 
activity.  This sulphate layer affects the Earth's radiation balance as well as 
stratospheric ozone levels.  Emission from the oceans is one of the main sources 
in the global budget of COS.  In this budget, however, exists an imbalance 
between sources and sinks which partly may be due to large uncertainties in the 
quantification of single sources and sinks.  For a better assessment of the 
oceanic source, we investigated the diurnal and seasonal cycle of COS in the 
Northeast Atlantic.  Atmospheric and dissolved COS was determined using a semi-
continuous seawater equilibration system with cryogenic preconcentration, gas 
chromatographic separation and flame photometric detection.  Ambient air was 
drawn through a Teflon tube from the top of the ship's mast to the analytical 
system.  Air was analysed directly and after equilibration with seawater (for 
the determination of dissolved COS in seawater).  Water from approx. 7 m depth 
was supplied continuously to the equilibrator by a non-contaminating pumping 
system.  This pumping system consisted of a Teflon membrane pump (all wetted 
parts polyvinylidene fluoride) and a polyvinyl chloride tube mounted inside a 
hollow stainless steel shaft which was submerged beneath the keel through the 
ship's "moon pool".  The fully automated system allowed the hourly analysis of 
atmospheric and dissolved COS.  The saturation ratio of COS in surface waters 
with respect to its atmospheric concentration was calculated:

                 SR = [COS]equilibrated air / [COS]ambient air

During the entire cruise leg dissolved COS was supersaturated in surface waters 
with respect to its ambient atmospheric concentration and a diurnal cycle with 
maxima in the afternoon and minima before sunrise was observed.  The results 
from the former Meteor cruise legs M27/1 (January 1994, OMEX area) and M21/2 
(April/May 1992, BIOTRANS area at 47°N, 20°W) are in contrast to these findings.  
The winter data (M 27/1) showed persistent undersaturation and no diurnal cycle 
of dissolved COS, probably due to low light intensity and hence low 
photochemical production during daytime.  The spring data from the BIOTRANS area 
(M 21/2) showed undersaturation as well as supersaturation and no net flux to 
the atmosphere could be found within the experimental uncertainty.  The results 
from these three cruise legs cover three seasons (winter, spring, and summer) 
and show a pronounced seasonal variability of the sea surface COS concentration.  
This set of data will be used to estimate an annual cycle of dissolved COS in 
the Northeast Atlantic, based on meteorological and oceanographic data.  
Moreover a kinetic model for the diurnal cycle of dissolved COS will be applied 
that considers light dependent and light independent COS production, hydrolysis, 
and gas exchange across the air-sea interface.  Consequences with respect to 
estimations of the global marine emissions of COS will be addressed.


~ DEPTH PROFILES OF DISSOLVED COS AND PHOTOCHEMICAL INCUBATION STUDIES 
  (O. Flöck)

Depth profiles of dissolved COS were taken using non-contaminating, gas tight 
GoFlo water samplers.  The water samples were pressure filtered (GF/F Whatman 
filters, preheated at 400 C for 2h), transferred into volume-calibrated glass 
flasks (approx. 300 ml) and stored in the dark at 4 C for not longer than 6 
hours.  Photochemical incubation studies were performed using surface seawater 
obtained from our non-contaminating seawater pumping system.  The water was GF/F 
filtered, filled into glass flasks and exposed to sunlight for ca. 10 hours.  
The samples (including dark controls) were held at sea surface temperature 
during the irradiations. COS was determined by gas stripping of seawater, 
followed by cryogenic trapping, gas chromatographic separation, and flame 
photometric detection.  All results were corrected for sample losses due to 
hydrolysis.

At ten stations the vertical distributions of dissolved COS were recorded.  
These data included high resolution profiles within the upper 100 m and profiles 
down to depths of 2000 m.  Generally the vertical profiles showed maxima at the 
sea surface and an approximately exponential decay to a certain background level 
beneath the mixed layer (about 50 m during the cruise).  Although the COS 
concentration in deeper waters was very low, some transport or non-photochemical 
production mechanisms are required to maintain this background level and 
compensate losses due to hydrolysis.  In addition to the station work, time 
series of COS photoproduction were obtained from ten sunlight irradiations of 
surface seawater.  These time series together with our continuously recorded UV-
light intensities will enable us to determine COS photoproduction constants.  
Our complete data set which includes atmospheric mixing ratios, sea surface 
concentrations, depth profiles, and COS photoproduction constants, will be used 
to test one-dimensional transport models for the prediction of surface 
concentrations and global marine emissions of COS.  We will be able to 
investigate the influence of downward mixing of dissolved COS out of the zone of 
photochemical formation on the sea surface concentration and hence on the sea-
to-air flux of this climatically relevant trace gas.


~ SEA SURFACE CONCENTRATIONS OF DISSOLVED DMS
  (G. Uher)

DMS is formed mainly by the enzymatic cleavage of dimethylsulfonium propionate 
(DMS) which is a metabolic product of marine phytoplankton.  Former work showed 
that the concentration of dissolved DMS is controlled by a complicated interplay 
of algal speciation and trophic interactions.  Air-sea exchange processes result 
in the emission of dissolved DMS into the atmosphere where it is oxidized mostly 
to aerosol sulphate.  These aerosol particles act as cloud condensation nuclei 
(CCN), and thereby influence the reflectivity and stability of clouds.  Thus the 
Earth's radiation balance is sensitive to the CCN number concentration which in 
turn might be sensitive to changes in phytoplankton biomass.  Global estimations 
of marine DMS emissions still suffer from the insufficient knowledge about its 
regional and seasonal distribution all over the oceans.  The emission of DMS is 
largely controlled by its sea surface concentration and wind speed.  During this 
cruise leg we performed measurements of sea surface DMS with high time 
resolution to improve our data base with respect to regional distribution, 
patchiness, and seasonality of DMS in surface waters. 

DMS was determined using a semi-continuous seawater purge and trap system with 
cryogenic preconcentration, gas chromatographic separation and flame photometric 
detection.  Seawater was sampled using our non-contaminating pumping system.  
The newly developed automated analytical system hourly sampled seawater which 
then was filtered (GF/F Whatman filters) and analyzed for dissolved DMS.  The 
concentrations ranged from 1 nmol l-1 up to 12 nmol l-1 with an average of 2.8 
nmol l-1 for the entire data set.  During the transect from the Canary Islands 
to the Celtic Sea margin, the DMS concentrations increased slowly from 1.5 nmol 
l-1 to about 3 nmol l-1, but no pronounced gradient across the shelf edge could 
be observed.  This is not surprising, however, since we could neither find any 
pronounced increase in chlorophyll (indicator of phytoplankton biomass) nor in 
absorbance or fluorescence of dissolved organic matter which were used to 
classify the water masses of the different biogeographic regions (e.g. coastal & 
shelf, open ocean).  On the shelf region, dissolved DMS showed maxima up to 12 
nmol l-1 which were associated with areas of high chlorophyll concentration.  
Our attempts to find consistent relationships between chlorophyll and dissolved 
organic matter on one hand and sea surface DMS on the other did not result in 
simple correlations.  Nevertheless, we will continue in carefully looking for 
relations between DMS and chlorophyll within distinct oceanic regions to further 
investigate the possibility of using satellite imagery as a tool for 
extrapolating and predicting DMS concentrations.

Based on our time series of dissolved DMS we will estimate sea-to-air fluxes of 
DMS.  These fluxes then will be compared to the number concentrations of 
condensation nuclei (CN, Aitken nuclei).  Our black carbon and radon (222Rn) 
data will help us to distinguish between marine and continental air masses.  
Hence we will be able to look for relationships between CN and the precursor 
compound DMS within the marine boundary layer.


~ CHLOROPHYLL AND DISSOLVED ORGANIC MATTER IN SURFACE SEAWATER 
  (G. Schebeske, V. Ulshöfer)

In addition to the defemination of sulphur compounds, chlorophyll along with 
absorbance and fluorescence of seawater was recorded.  We intended to use 
chlorophyll as an indicator of phytoplankton biomass and furthermore absorbance 
and fluorescence of dissolved organic matter as tracers to determine the degree 
of mixing between different water masses as well as their optical and 
photochemical properties.  Surface seawater from our non-contaminating pumping 
system was sampled approximately every 4 hours.  The samples were stored in 
detergent washed polyethylene bottles at 4°C in the dark, generally for not 
longer than 10 hours. 250 ml were filtered (GF/F Whatman filters, preheated at 
400°C for 2h).  The filters were homogenised and extracted with acetone/water 
(90/10) at room temperature.  Then the solution was filtered again to remove the 
glass fibres, filled up to a standard volume with acetone/water, and analyzed 
fluorometrically (Ex 425±20 nm, Em 665±20 nm) using a Shimadzu RF1501 
spectrofluorometer equipped with a 10 mm quartz cell.  The instrument was 
calibrated before and after the cruise using a solution of chlorophyll a (Sigma 
Chemie) in acetone/water.Both absorbance and fluorescence was measured on 
filtered seawater (GF/F Whatman filters, preheated at 400 C for 2h).  The 
spectral absorbance was recorded from 250 nm to 700 nm using a Shimadzu UV160A 
spectrophotometer and 100 mm quartz cells. Milli-Q water was used as a 
reference.  The absorbance data have been normalized to compensate for the 
instrument's drift by subtracting the reading at 690 to 700 nm.  Fluorescence 
emission spectra., 325 nm, and 340 nm as excitation wavelengths and an emission 
wavelength scan in the range of excitation wavelength plus 15 nm up to 600 nm.  
The spectral response of Milli-Q water was subtracted and the fluorescence 
intensities then were expressed in quinine sulphate units (the maximum intensity 
of 1 mg l-1 quinine sulphate dihydrate in 0.105 M HClO4 at the excitation 
wavelength used was defined as 1 quinine sulphate unit).  Preliminary results 
show absorption coefficients a(350 nm) lower than 0.1 m-1 for the transect from 
the Canary islands to the celtic sea margin and no significant increase across 
the shelf edge could be observed.  (a(350 nm) here is defined as the decadic 
absorption coefficient and normalized to one meter optical pathlength.  Thus 
Lambert Beer's law is written: A = a*l (A=absorbance, l=optical pathlength)).  
On the shelf area slightly higher absorption coefficients a(350 nm) of about 
0.15 m-1 were found.  The results from the fluorescence measurements in general 
showed the same trend.


(1)  CONDENSATION NUCLEI (CN, AITKEN NUCLEI), BLACK CARBON, AND RADON (222RN) 
     WITHIN THE MARINE BOUNDARY LAYER 
     (G. Schebeske, V. Ulshöfer)

The atmospheric concentrations of condensation nuclei, black carbon, and radon 
were used as tracers to distinguish between marine and continental air masses.  
The sampling inlets for the continuous aerosol analysers (CN, black carbon, and 
222Rn) were located on a beam extending into the air flow just above the flying 
bridge (ca. 30 m above sea surface) where the ship's air chemistry laboratory is 
located.  Tubing lengths between inlet and instruments were less than 5 m. For 
CN sampling electrically conductive tubing was used.  The sampling inlet for 
black carbon was automatically interrupted by a Weathertronics sampler 
controller if the relative wind direction was more than 120 off the bow to avoid 
the sampling of stack emissions.  CN concentrations were determined with a TSI 
model 3020 condensation nucleus counter.  Black carbon was measured with an 
aethalometer (Magee Scientific).  Both CN and black carbon were recorded 
continuously and integrated over 5 min periods.  222Rn was recorded continuously 
via the decay products 214Po and 218Po using an APIA monitor.  The counts were 
integrated over 2 hour periods.


ACKNOWLEDGEMENTS

We thank Karl Pegler, Ralf Lendt, and Harald Rätzer for letting us use their 
stainless steel sampling inlet. Thanks are due to Alexander Pfeiffer and Ilse 
Büns for helping us with their pH-data.


5.1.3  SEDIMENTOLOGY

~ PARTICLE FLUX AND IN SITU MARINE AGGREGATE STUDIES AT THE CONTINENTAL MARGIN
  (IfMK, A.N. Antia, W. Erasmi; IOSDL, R.S.Lampitt; T. Kumbier; IOW, G. Lehnert)

~ PARTICLE FLUX 

Particle flux studies within the OMEX programme focus on addressing the 
transport of material on the shelf-slope regions of the Goban Spur, with an 
emphasis on exchange of material between these regions and the adjacent open 
ocean.  The positions of moorings with sediment traps, current meters and 
transmissometers have been chosen to quantify both particle flux out of the 
euphotic zone and winter mixed layer as well as to determine mid-water transport 
at the slope edge on the Pendragon Escarpment, at which position particles from 
the continental margin may be expected to be exported to the adjoining abyssal 
basin and the transport of dissolved nutrients onto the slope would take place.  
During METEOR 30/1 these moorings were successfully recovered and re-deployed 
and yielded a near-complete set of sediment trap samples and current meter data 
for the previous 9 months of deployment (Jan - Sept 1994).  For the deployment 
period July 1993 - Jan 1994 (autumn/winter), currents at the position OMEX 2 
were seen to flow along the bottom contours in a northerly direction, i.e. along 
- slope, whereas at the Pedragon Escarpment off -slope water transport was 
registered, accompanied by an increase in particle concentrations in the 
sediment traps at intermediate depths as compared to that directly beneath the 
winter mixed layer.  The data obtained during M 30/1 show a different picture 
for the spring and summer.  Fig. 4 (a - e) shows current meter data from the 
moorings OMEX 2 and OMEX 3 at the different depths.  Data are presented as 24-
hour running means to smooth out tidal oscillations which are present in all 
data, though with decreasing amplitude with increasing distance from the shelf.  
At OMEX 2 a change in current direction from predominantly northwest-flowing 
(~300( magn.) to south-easterly currents during March and again during May is 
apparent.  Mean current speed decreases from 11.75 cm/sec at 620 m to 9.41 
cm/sec at 1070 m over the 9-month deployment.  Although few data of this kind 
exist for the Goban Spur, such a reversal of shelf currents during the summer 
months has been documented by Pingree & LeCann (1989) in an adjacent region.  
This reversal in current direction has implications on the source area of 
particulate material intercepted in the sediment traps.  Southwesterly currents 
would carry material from the region of the shelf break, characterised by high 
chlorophyll concentrations, to the trap positions.  Another feature that is 
evident from the data is the occurrence of warmer water during the winter 
months, as has been found in the Bay of Biscay region (Pingree & LeCann 1990).  
A transmissometer mounted on the vane of the current meter at 1070 water depth 
at OMEX 2 (data uncalibrated; jump at day 120 due to readjustment), show short 
events of increased water turbulence; the correlation of such variations in the 
suspended pool with particulate sedimentation is, however, tenuous at best.  
Results of sediment trap sample analyses will be available in the coming year; a 
rough idea of seasonality in bulk flux can be seen, however, from Fig. 5 (a and 
b); clear here is the increase in sedimentation during late April following 
spring phytoplankton growth.

At the OMEX 3 site on the Pedragon Escarpment, current direction fluctuates 
frequently during spring and summer.  Residual currents flow eastward at 580 m, 
and south-westwards at 1450 and 3280 m during this deployment period.  Average 
current speeds during this deployment period again decrease with depth, from 
10.4 cm/sec at 580 m to 6.8 cm/sec and 4.4 cm/sec at 1450 and 3280 m 
respectively.  However at all depths events of on - slope water flow are seen, 
providing valuable information on the cross-slope exchange of nutrients to the 
productive shelf and slope regions.  The general impression of bulk 
sedimentation at OMEX 3 shows a marked increase in sedimentation with depth in 
the lower two traps (Fig. 5 c, d), as was seen at this site during the prior 
period of deployment (July 1993 - Jan 1994).  The qualitative nature of this 
material, which we take as evidence of export of slope material to the abyssal 
plain, will be better described upon analyses of trap samples.  Of particular 
interest in the context of OMEX is determination of the fate of this material 
leaving the slope environment and its deposition in the Porcupine Abyssal Plain, 
where conditions for the subsequent long-term burial of organic matter differ 
from those of the benthos in the slope and shelf environments.  To be able to 
better elucidate and quantify this export of slope material to the deep sea bed, 
an additional mooring was deployed in 4485 m water depth off the Pedragon 
Escarpment in co-operation with colleagues at NIOZ (Texel, The Netherlands) 
(Mooring OMEX 4, 48°59.51'N; 13°44.06'W).  This mooring contains a single 
sediment trap (at 4015 m depth ) and current meter ( at 3995 m), which, on the 
basis of previous data available from this site, are above the region of near-
bottom resuspension. 

TABLE 5.1.1:  OMEX SEDIMENT TRAP MOORINGS CURRENTLY IN DEPLOYMENT.

MOORING	LATITUDE	LONGITUDE	WATER	DEPTH	INSTRUMENT
					DEPTH	(M)
OMEX 2	49°11.20'N	12°49.18'W	1445 m	595	Sed. trap
						618	RCM
						1052	Sed. trap
						1076	RCM+Trans.
OMEX 3 	49°05.00'N	13°25.80'W	3650 m	556	Sed. trap
						580	RCM
						1465	Sed. trap
						1489	RCM+Trans
						3260	Sed. trap
						3284	RCM+Trans
OMEX 4	48°59.51'N	13°44.06'W	4485 m	4015	Sed. trap
						3995	RCM+Trans

A list of OMEX moorings presently in deployment is given in Table 5.1.1.  These 
moorings will be recovered and redeployed from board the RSS DISCOVERY in 
September 1995. 

The OMEX sediment trap mooring line naturally extends onto the Porcupine Abyssal 
Plain.  Sediment traps have been deployed by the Institute of Oceanographic 
Sciences (UK.) at "Station H" (40°N, 16.5°W) since April 1992 with a view to 
determining long-term trends in particle flux at an oceanic site removed from 
the influence of the continental shelf and slope.  Traps have in general been at 
depths of 100, 3400 and 4500 m above bottom (water depth 4600 m) with an array 
of current meters and camera systems to examine temporal trends in marine snow 
concentration.  The latest deployment had been from RSS DARWIN in April 1994.  
During METEOR 30/1 this was recovered, refurbished and redeployed within 11 
hours.  From the recovered traps, apart from one on which the mechanism failed 
halfway through its cycle, all functioned well and have provided a good 
collection of samples.  These will be analysed in a variety of ways to give 
information about the composition of the material, and the flux of organic 
carbon, nitrogen, pigments, radionuclides and various organic markers.


~ MARINE SNOW STUDIES

Marine snow is loosely defined as inanimate particles of diameter greater than 
0.5 mm.  They are thought to be the principal vehicles by which material sinks 
through the water column.  Such studies therefore are of considerable importance 
in developing our understanding of material flux.  The distribution of these 
fragile particles is best determined using photographic techniques such as the 
Marine Snow Profiler.  This instrument is attached to the CTD and photographs 
about 40 l of water every 15 seconds using orthogonal illumination from a deep-
sea flash light.  Up to 400 frames can be taken.

During Meteor M30/1 seven deployments of the MSP were successfully made and the 
resulting images will be examined on an image analyser to determine the 
abundance, size and volume concentration of these particles. 

In order to make further studies on marine snow particles they must be 
collected.  This was achieved during Meteor 30/1 using the specially designed 
marine snow catcher or "Snatcher".  This is a messenger operated 100 l closing 
water bottle designed to minimise damage to the marine snow particles.  After 
standing on deck for at least 2 hours, the upper 95 l is drained off and the 
lower portion of the Snatcher disconnected along with 5 l of water.  The 
particles can then be recovered from the base plate using a pipette.  During 
this cruise, after some initial compatibility problems, the Snatchers were 
successfully deployed on two occasions to depths of 30 and 50 m. 

TABLE 5.1.2:  MSP DEPLOYMENTS:

DEPL. #	STA #	DATE		TIME(H)	CAST	 WATER	  LONG.°N	LAT.°W
					DEPTH(M) DEPTH(M)
89	427	14.09.94	18:55	500	 3668	  49.09		13.41
88	428	15.09.94	00:02	500	 3668	  49.15		13.09
87	429	15.09.94	18:03	500	 3643	  49.08		13.41
86	430	16.09.94	02:31	500	 1524	  49.18		12.85
85	433	16.09.94	23:31	500	 1148	  49.24		12.50
84	434	17.09.94	06:59	500	 672	  49.42		11.54
89	435	17.09.94	13:55	200	 211	  49.47		11.15


~ CTD - WORK

CTD profiles, with registrations of conductivity, temperature, pressure, 
fluorescence and oxygen, were taken at a number of stations along the transect 
followed during M 30/1.  Unfortunately, malfunction of the release mechanism of 
the rosette prevented water samples being taken during these deployments.  CTD 
drops were thus mainly confined to the upper 500 m of the water column where a 
marine snow profiler, attached to the CTD frame, registered snow concentrations 
with a fine vertical resolution.


5.1.4  BENTHIC BIOLOGY

~ BENTHIC MICROBIOLOGY 
  (IfMK, K. Poremba, K. Jeskulke)

Microbiological investigations involved the determination of abundance and 
activity of bacteria in the sediment.  Sediment samples were taken with a 
multicorer.  The samples were immediately transferred into a cooled laboratory 
avoiding artefacts due to temperature shifts of the samples.

The measurements included the fixation of subsamples with formaldehyde and later 
counting of bacterial cells (in the home laboratory), and the measurement of 
extracellular hydrolytic activity using 5 different fluorogenic analog 
substrates for protease, esterase, chitinase, and beta-glucosidase.  Esterase 
activity represents a value of overall microbial activity, while the other 
enzyme rates enables the detection of different types of microbial degraders.

Several stations of a transect over the continental shelf margin of Goban Spur 
were visited during leg M 30/1.  The sampling was focused on sites deeper than 
2000m, because extensive sampling between 200 and 2000 m had already been made 
on a former cruise with RV VALDIVA in July 1993 (VA 137).  The experiments 
conducted on VA 137 had shown that the activity of hydrolytic enzymes in 
sediment decline with water depth.  Cleavage rates of relatively easy degradable 
substances declined faster than degradation rates of more refractory molecules, 
which gave evidence for a close relationship between biological activity and 
quality of organic matter at the sea floor, and supported the theory of pelagic-
benthic coupling in the sea.  The measurements of M30/1 should elongate the 
transect of the previous measurements, because the sampling season of VA 137 and 
M30/1 was similar, so that only small seasonal impact could be expected.

Fig. (4a) 24-hour running means of current meter data from OMEX 2 at 620 m 
          from Jan - Sept 1994 (Day Nos. 11 - 260).

Fig. (4b) 24-hour running means of current meter data from OMEX 2 at 1070 m 
          from Jan - Sept 1994 (Day Nos. 11 - 260). Jump in transmissometer data         
          at day 108 is due to readjustment; transmissometer data are 
          uncalibrated.

Fig. (4c) 24-hour running means of current meter data from OMEX 3 at 580 m 
          from Jan - Sept 1994 (Day Nos. 11 - 260).

Fig. (4d) 24-hour running means of current meter data from OMEX 3 at 1450 m 
          from Jan - Sept 1994 (Day Nos. 11 - 260). Transmissometer data 
          (uncalibrated) are off scale at 4.505 Volt.

Fig. (4e) 24-hour running means of current meter data from OMEX 3 at 3280 m 
          from Jan - Sept 1994 (Day Nos. 11 - 260).

Fig. (5)  A rough estimate of seasonality in sedimentation of the mooring OMEX 
          3 between January and September 1994 (x-axis, day numbers 11 - 260) as 
          shown from the height of particle accumulation (y-axis, cm) in the 
          sediment trap cups. Although these data are in no way quantitative, it 
          is clear that a pulse of sedimentation following the spring bloom 
          occurs in late April. Also conspicuous is the increase in bulk and 
          duration of sedimentation in the deeper traps.

The weather conditions during the cruise were relatively good, so 4 sediment 
sampling at depths of 4805 m (the IOS-station in the Porcupine Sea Bight), 4471 
m (close to the basis of Goban Spur), 2269 m and 1535 m (slope of Goban Spur) 
were possible.  Generally, the found activity rates accorded to the range, 
which could be expected from our former measurements on VA 137.  The rates were 
lower than on more shallow situated sampling sites (a detailed comparison of 
data is not possible in the moment, because the value are not exactly corrected 
on volume basis).  Unusual high activity of protease and esterase (higher than 
at 1535 m) were found at 4471 m, which indicates that the basis of the 
continental margin acts as an accumulation zone for organic matter.  Counting 
of bacterial abundance and must be performed later in the home laboratory.


~ CARBON MINERALIZATION BY THE BENTHIC COMMUNITY
  (IHF, T. Soltwedel, Geomar, O. Pfannkuche)

Recent results from the temperate northeast Atlantic exhibited a strong 
seasonality in phytoplankton production and subsequently a varying supply of 
phyto-detritus to the benthos (Pfannkuche, 1993).  Thus, benthic activity and 
biomass is subject to spatial and seasonal variations in response to the 
sedimentation of particulate organic matter. RV METEOR' cruise 30, leg 1 was 
part of a series of expeditions to survey the reaction of the benthic community 
to episodic (seasonal) food pulses and to assess the role of the benthic 
organisms for the carbon flux through the sediment.

Benthic sampling was carried out along a depth transect across the Goban Spur 
continental margin from the outer Celtic Sea to the adjacent deep-sea basin, the 
Porcupine Abyssal Plain (Fig. 1 ).  A total of eight stations with water depths 
ranging from 200 m to 4800 m were sampled with a modified SMBA style multiple 
corer (MC).

To estimate the input of phytodetritus to the benthic community, we analysed 
chlorophyll/pheophytin concentrations within the sediments.  Changes in activity 
and biomass of the benthic infauna was assessed by measuring a series of 
biochemical assays:

activity parameters:  -esterases with fluorescein-di-acetat, FDA 
                      -adenosintriphosphate, ATP

biomass parameters:   -total adenylates, ATP+ADP+AMP
                      -desoxyribonucleinacid, DNA
                      -phospholipids
                      -particulate proteins

Additionally, samples were taken for grain size analyses and to determine the 
sediment water content (porosity).  Our investigations restrict to the upper 10 
cm of the sediments.

First results (Fig. 6) demonstrated the close relationship between food supply 
and benthic activity.  Concentrations of sediment-bound chloroplastic pigments 
(indicating primary organic matter) and enzymatic activity (fluorescein-di-
acetat turnover, FDA) showed a fairly similar pattern along the Goban Spur 
transect, with increasing values on the upper slope (1150 m, MC 31) and on the 
Pendragon Escarpment (3666 m, MC 27).  So far, no explanation could be given for 
the unexpected high FDA values in 4500 m water depth (MC 26) while CPE values 
were lowest on that particular station.  Results from other biochemical analyses 
might probably help to explain this discrepancy. 

To assess the carbon flux through the sediment, measurements of in situ 
community respiration rates were planned using a new benthic lander system.  
Unfortunately the central command unit of the benthic chamber could not be 
activated caused by a leakage of the pressure cylinder.  For time reasons a 
second mooring of the system was not possible.

Fig. (6)  Chloroplastic pigments and heterotrophic activity within the 
          uppermost centimetre of the sediments


5.2  WOCE PROGRAMMES:

5.2.1  PHYSICAL AND CHEMICAL OCEANOGRAPHY ON LEG M30/2

OPERATIONAL DETAILS
(BSH, K.P. Koltermann, K.C. Soetje, IORAS, V. Terechtchenkov)

Following the WOCE Hydrographic Programme requirements, the section WHP-A2 along 
nominally 48° has been worked as part of the One-Time Survey.  In addition to 
the classical hydrographic parameters, nutrients, small and large volume tracer 
concentrations have been determined.  Continuous ADCP (Acoustic Doppler Current 
Profiler) data provide the absolute vertical current shear of the top 500 m to 
calculate, from geostrophic transports, the absolute transport through this 
section.  With a horizontal station spacing between 5 and 30 nm, a 24 x 10 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, due to bad weather, 53 stations.  Additional 
stations for performance tests of the CTD/rosette system, calibrations and for 
the instruments for the chemical analyses have been worked weekly.  A 
distribution of the water samples along the section WHP-A2 is given in Fig. 
(7a).


CTD-ROSETTE EQUIPMENT AND PROCEDURES
(BSH, K.P. Koltermann, P. Wöckel)

The first few stations had to be used to find the most reliable and appropriate 
combination of CTD, rosette pylon and trip electronics and GO-bottle set.  
Problems were encountered with a rosette underwater unit that did not release 
properly and safely at pressures higher than 2600 dbar.  To economize on ship 
time and allow for the time required to draw water samples properly from the 
shallow and deep rosette, a sequence of rosette deployments was tested where 
the first rosette/CTD was run deep, followed if required by the LVS casts.  
This was followed by a shallow rosette/CTD to provide close sample spacing in 
the top 1500 m.  First, this second rosette was then deployed on the first, 
that is deep cast of the following station to avoid changing the rosette and 
CTD connections to the wire.  This was abandoned rather early in the cruise in 
order to run all deep casts with the best CTD/rosette combination available, 
and deploy the shallow cast with the priority for water samples and ensuing 
trip CTD data only.  This sequence has provided a much more secure calibration 
procedure and calibration data set for the full-depth CTD data, as in essence 
it will not be necessary to match data from two different CTD units for this 
section.

For the deep casts the CTD Neil Brown MkIII, labelled DHI1, was used on pylon 
no.7 with 24 x 10 l GO bottles uniquely marked.  The shallow cast was run with 
the Neill Brown MkIII, labelled NB3 of IfM Kiel, with the Kiel pylon and 24 x 10 
l GO-bottles.  All bottles were equipped with stainless steel springs with 
grease-free O-rings to avoid contamination for CFC-sampling.  The station 
routine was maintained throughout the cruise.  Only few mistrips occurred and 
were accommodated for by standard oceanographic procedures. 

In heavy weather and seas, particularly at the end of the cruise, on a few 
stations heavy wire wear was observed ca. 20 - 50 m above the rosette.  This was 
seen as a result of the rosette package starting to kite.  Extra weight was 
added to the package and the lowering speed decreased slightly to 1 m/s.  No 
more problems occurred afterwards.

The acquisition software showed some mysterious problems at the beginning of the 
cruise where the acquisition at depth stopped and the system could not be 
restarted again.  A simple software problem was solved after being identified.

More details of the sampling procedures are given in 5.2.3.  The CTD- 
calibration coefficients for the M30/2 leg are essentially identical to those 
for M30/3.  Both data sets have been processed similarly.  Bottle data files for 
both leg are, again, processed according to the WHP guide-lines and with 
consistent meta-data file documentation.

The statistics of water bottle samples for the four calibration stations worked 
during M30/2 are given in Tab. 5.2.1.1.


BIO SAMPLE CODING
(BSH, K.P. Koltermann)

On this cruise we used for both WOCE legs a sample labelling system introduced 
by the Bedford Institute of Oceanography, Canada.  A uniquely numbered label is 
assigned to each water sampler at the rosette on each individual cast.  The 
same number is assigned also to all subsamples of this particular sample 
bottle.  Records of all groups analysing water samples maintain this unique 
number within their procedures until the hydrocast file is collated and merged 
with the trip data from the CTD of that cast.  The uniquely identified sample 
can be traced back to the particular container/bottle of the cast it originates 
from.  If mistrips have to be accommodated later, or sampling trip depths 
change due to recalibration of the pressure sensor, the sample is still tied to 
that volume of water/rosette bottle it was sampled from.  Sampling depth was 
thus removed from being a sample identifier, and would later on be substituted 
as a parameter of the sample.

Almost all groups had not been familiar with this procedure prior to the cruise.  
They happily adopted it after only the first station.  The CTD watch was 
particularly pleased with it as they were relieved of frequent curious questions 
as to what sampling depth the sample was supposed to come from.

TABLE 5.2.1.1:  PRECISION OF DUPLICATE SAMPLES (I.E. FROM DIFFERENT ROSETTE 
                BOTTLES FIRED AT THE SAME NOMINAL DEPTH) OF CALIBRATION STATIONS 
                ON WHP-A2.

		   STAT. #43601		STAT. #43603	STAT. #45301	STAT. #47601
Duplicates:	   N = 7		N = 24		N = 24		N = 24
Parameter	   mean±sdv		mean±sdv	mean±sdv	mean±sdv 
Pctd/db		   3237.96 +1.52	3201.46±0.27	4304.18±2.1	3301.73±0.87
(Pdsrt)		   none			none		none		3304.25±2.96
p/db									- 2.52
Tctd/mK		   2.7192±.000		42.7410±.0019 	2.5769±.0003	2.5766±0.0005
(Tdsrt)		   none			none		none		2.5807±0.0044
Delta-T									.0041
Sctd		   34.9335±.0005	34.9284±.0004	34.9049±.0004	34.9200±0.0003
Sali		   34.9318±.0003	34.9332±.0008	34.9120±.0004	34.9185±0.0004
Delta-S		   - .0017		.0048		.0071		-.0015
Oxygen (µmol/l)	   251.99±.942		251.90±.694	249.87±.591 	284.27±.472
Nitrate (µmol/l)   22.001±.083		none		22.507±.0079	16.992±0.045
Phosphate (µmol/l) 1.561±.011		none		1.581±.0026 	1.159 ±0.014
Silicate (µmol/l)  36.324±.159		none		41.709±.314 	19.541±0.133


THERMOSALINOGRAPH
(BSH, M. Stolley; IORAS, V. Terechtchenkov)

An Ocean Sensors OS200 thermosalinograph was mounted to the ship´s laboratory 
sea water pumping system.  The data together with position and additional 
temperature data were logged at 1' intervals.  Except for a few periods in heavy 
weather where air was caught in the system, the data are of good quality.  
Salinity samples were taken on each watch; the stability of the conductivity 
sensors and their statistics are promising.


ADCP
(BSH, M.Stolley)

The shipboard ADCP system with a RD unit was run throughout the cruise.  Serious 
data quality problems occurred during heavy weather because of air being trapped 
under the ship.  Data were recorded at 6 min intervals, a total of 6145 profiles 
down to 500 m depth was archived.  From Oct 22 through 27 and between 21°W and 
30°W computer problems impeded the data quality.  During a gale on Oct 19, 1994 
one transducer of the ADCP seems to have been damaged resulting in a reduced 
signal to noise ratio.  The data from a new Ashtech 3D GPS system could not be 
successfully merged with the ADCP data stream.  For the leg M30/3 new software 
was available only in St John's.  For M30/2 the normal shipboard GPS data were 
logged with the ADCP data stream.  All data are being processed at the level 
previously developed for M18.


~ DETERMINATION OF THE MERIDIONAL TRANSPORTS OF HEAT, SALT AND FRESHWATER AT 
  48°N IN THE NORTH ATLANTIC ALONG THE WHP SECTION A2
  (BSH, K.P. Koltermann, A. Sy; IORAS, V. Terechtchenkov)

PRELIMINARY RESULTS
The 48°N section was sampled for the fourth time since 1957.  It was an exact 
repeat of the 1993 sampling with RV Gauss.  By now we have a very clear picture 
of the main hydrographic features and spatial scales on this section, such as 
the deep boundary current regimes on both sides of the Mid-Atlantic Ridge (MAR), 
the spatial scales of the westward propagating Mediterranean Outflow and the 
eastward propagation of the Labrador Sea Water (Fig. 7 b-e).

The cooling of the LSW and deepening of the LSW core layer that was previously 
seen during 1993 (Koltermann and Sy, 1994) has continued during the autumn of 
1994.  But it now is seen more prominently also in the Eastern Basin of the 
North Atlantic.  The LSW core temperatures had changed in 1993 since the 1982 
occupation of this section by CCS Hudson by -0.45°C.  The core layer had 
deepened in that same period by 641 dbar.  From summer 1993 to autumn 1994 the 
temperature west of the MAR had cooled by another 0.057°C and deepened further 
by 27 dbar. From 1982 to 1993 the LSW core temperature east of the MAR at ca. 
27°W had decreased by -0.154°C; in just over one year from 1993 to 1994 it 
cooled by another 0.096°C, deepening by ca. 152 dbar.  Salinity changes in the 
Western Basin are small, order 0.001, compared to the temperature changes.  The 
effect on the density is ca.0.045 kg/m3 in the Western and 0.005 kg/m3 in the 
Eastern Basin manifested in the increase in depth (Fig. 8 a-d).  All this 
clearly shows how the LSW formed in the Labrador Sea in larger quantities since 
the late 1980s (Lazier, 1995) now invades the Eastern Basin (see also 5.2.3).

Fig. (7a) Distribution of water samples along section WHP-A2

Fig. (7b) Salinity distribution from bottle samples along WHP-A2

Fig. (7c) Potential temperature along WHP-A2

Fig. (7d) Density sigma-theta distribution along WHP-A2

Fig. (7e) Density sigma-2 (reference 2000 dbar) distribution along section 
          WHP-A2

A feature not observed in that prominence on earlier cruises along A2/AR19 is 
the low surface salinity at #483, 42°26.5'W.  This drop in salinity coincided 
with a drop in temperature by ca. 5°C.  Only at 500 m depth both salinity and 
temperature level out to values comparable to neighbouring CTD stations.  As 
this drop was already noticed in the thermosalinograph records approaching the 
station, closely spaced XBT-drops have resolved the temperature structure of an 
extensive eddy of northern origin on both sides of station 483.  The effects of 
this eddy can be traced down to 2500 m in the density fields (Fig. 7d,e).  CCS 
Hudson had surveyed the area only days earlier and had located the centre of 
this quasi-stationary feature, dubbed the "Mann Eddy", at 41°46'N and 44°10'W.

Long-term changes in the characteristics of the Labrador Sea Water LSW for the 
three comparable manifestations of this section along ca. 48°N are summarised in 
Fig. (8 a-d).  All three cruises follow an identical track east of the Mid-
Atlantic Ridge MAR, only in the Western Basin the tracks of Gauss 226 in 1993 
and Meteor M30/2 in 1994 are identical.  For CCS Hudson the track was chosen to 
follow 48°N exactly, crossing Flemish Cap and its local circulation regime.

An indication of the heat and salt available at 48°N and their changes since 
1957, the year of the Discovery section during IGY, gives Fig. (8e,f).  All 
available data have been interpolated on the same grid across the section.  The 
Discovery and Hudson sections have been, for the Western Basin, projected onto 
the new track of the Gauss and Meteor sections.  For each grid column potential 
temperatures and salinities have been averaged.  The mean values are plotted 
against longitude west, and the bottom topography of the section has been 
included.  For the continental shelf slope regions on both sides of the section 
the mean values are biased by the considerably shallower depths, not to be 
discussed here.  From these figures it becomes obvious that outside the 
continental slope regimes the Eastern and Western basins show individual 
features.  The Eastern Basin is much smoother, quieter at no distinct spatial 
scales below the basin scale.  The MAR clearly separates both basins.  
Variations in the West show distinct spatial scales, order 300 km and much 
greater variability than in the East. The Labrador Current on the shelf break 
and the Deep Western Boundary Currents on the continental slope are seen in the 
general decrease in temperature and salinity west of 44°W.

Fig. (8a,b) Potential temperature (8a) and depth (8b) of the Labrador Sea Water 
            core along 48 °N for 1982, 1993 and 1994

Fig. (8c,d) Salinity (8c) and density (8d) of the Labrador Sea Water core along 
            48°N for 1982, 1993 and 1994

Fig. (8e,f) Depth-averaged potential temperatures (top) and salinities (bottom) 
            along 48°N for 1957-1994

In the deep ocean we note the smooth curves in the Eastern Basin.  For 1957 
(Discovery) we find here the highest, for 1982 (Hudson) the lowest temperatures.  
The most recent survey in 1994 (Meteor) gives the lowest salinities, for 1957 
with Discovery the highest.  Disregarding potential accuracy questions with the 
Discovery salinities, we find that in 1982 and 1993 the mean salinities are 
almost the same, indicating that the cooling of the LSW we have observed already 
in the Western Basin has now progressed into the Eastern Basin.  Across the MAR 
the boundary currents on both sides leave their imprint by coherent changes 
towards higher or lower values at a given location.  West of the MAR up to the 
Milne Seamounts at 39°W for 1993 and 1994 we find the highest mean temperatures 
and salinities, for 1957 and 1982 the coldest and freshest water.  This tendency 
continues into the Western Basin proper, that is West of the Milne Seamounts.  
Here the warming between 1957/1982 and 1993/1994 amounts to about 1°C, and the 
salinity increase to ca. 0.2.  Despite the considerable input of newly formed at 
great depth, the net vertically averaged property changes are towards higher 
temperatures and salinities.


~ NUTRIENTS MEASUREMENTS FOR FINE RESOLUTION OF OCEANIC WATER MASSES ON THE 
  METEOR CRUISE M30/2 (SECTION WHP-A2) IN THE NORTH ATLANTIC 
  (IfMK, L. Mintrop, H. Johannsen, F. Malien)

Nutrient analyses as well as determinations of dissolved oxygen were carried out 
according to the WOCE WHP standards from the samples obtained from all 
hydrocasts.  By sampling from every successfully closed bottle, a total number 
of 1692 and 1737 samples were analysed for nutrients (nitrate, phosphate, 
silicate) and dissolved oxygen, respectively, by the nutrient team from the 
Institute of Marine Sciences, Marine Chemistry Department, Kiel, Germany.  The 
quality of the data was assured by carrying out the quality and reproducibility 
checks according to the WOCE standard operation procedures.  These parameters 
were also measured from the samples (a total of 138) obtained with the large 
volume samplers of the C-14 group.  The data from the measurements were made 
available to the participants at the end of the cruise to help in the fine 
resolution of oceanic water masses in the North Atlantic.  Besides this goal, 
nutrient and oxygen distributions, especially in the upper water column, allow 
the interpretation of seasonal biological processes and therefore contribute to 
the CO2-studies of this cruise.

The data are summarised in the Fig. (9 a-d).

Fig. (9a)   Distribution of dissolved oxygen along section WHP-A2

Fig. (9b-c) Distributions of silicate (8b), nitrate (8c) along section WHP-A2

Fig. (9d)   Distribution of phosphate along section WHP-A2


~ CFCS ON THE WHP SECTION A2
  (IUP-B, W. Roether, A. Putzka, K. Bulsiewicz, C. Rüth, H. Rose)

OPERATIONAL DETAILS
The CFC analyses are performed onboard.  Except for shallower areas almost each 
station was sampled at up to 36 levels.  The CFC samples were drawn from 10 
liter Niskin bottles on large glass syringes.  During sampling the contamination 
with ambient CFC had to be avoided and controlled.  In all 1062 analyses for 
F11, F12, F113 and 978 analyses for CCl4 have been performed, and the data were 
evaluated preliminary at sea.

The investigated tracers are the man-made chlorofluorocarbons (CFC) F11, F12, 
F113 and carbon tetrachloride CCl4.  Their time-dependent input 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.  
Measuring the concentration of the tracers delivers information about time 
scales of ventilation processes of subsurface water.  The atmospheric F11 and 
F12 contents increase monotonously with different rates since the forties.  CCl4 
increases since 1920 while F113 started to increase in 1970.  Hence the 
concentration ratios of the different tracers vary over wide time ranges and can 
be used to indicate the 'age' of water masses (age since leaving the surface).  
'Younger' water is tagged with higher CFC concentration compared with 'older' 
water.


SAMPLING
Samples were taken according to the WOCE scheme. 


CFCs: 
glass syringes, on 45 of 53 hydrographic stations 1048 samples were taken 
and measured on board.


HELIUM: 
80 helium samples in copper tubes for on shore extraction, intercalibration 
purposes. Samples to be measured on shore.


MEASUREMENTS: 
All CFC measurements were done using a gas-chromatographic system especially 
improved because of problems with the analysis of F113 (chromatographic 
interference with CH3I). The system is now equipped with a new designed micro-
trap for collecting the different gases purged from a water sample, a special 
pre-column to improve especially the resolution between CH3I and F113 and a 
electronic pressure regulator for a better baseline stability.  Due to these 
changes we were able to measure F113 with sufficient chromatographic resolution 
and to produce for the first time a high quality set of measurements for the 
whole section.

Fig. (10) F113 (upper part) and CCl4 distribution on A2. Values given in ppt. 


PRELIMINARY RESULTS
In Fig. (10) sections for F113 and CCl4 are shown.  Within the eastern basin of 
the section the lowest F113 and CCl4 values were found below about 3500 m 
indicating as expected the oldest water found on the section.  For the deep 
western basin a layer of water with higher F113 concentration is found at the 
bottom due to the recently ventilated overflow water from the Denmark Strait.  
Lower concentrations were observed at a depth range between 3000 and 4000m on 
the western flank of the Mid Atlantic Ridge.  This indicates most probable a re-
circulating portion of a mid depth North Atlantic Deep Water (NADW).  Most 
significant is a layer with higher F113 and CCl4 concentrations indicating the 
Labrador Sea Water (LSW) at about 1900m depth which extends over the whole North 
Atlantic.

The Mediterranean Overflow Water (MOW) shows up slightly above 1000m depth at 
the eastern side of the West European basin.  While the F113 and also F11 and 
F12 (not shown here) is here lower, the CCl4 shows a much clearer minimum.  It 
is known that CCl4 degrades but only within water warmer than about 10-12°C.  
The original overflowing Mediterranean Water is above that temperature and 
therefore the MOW found in the Atlantic has significant lower concentration in 
CCl4 compared to Atlantic waters of comparable temperature or comparable 
concentration of the other CFCs. 


~ TRITIUM/HELIUM AND 14C-SAMPLING ALONG WHP-SECTIONS A2 AND A1
  (IUP-HD, R. Bayer, B. Kromer, M. Born)

The experimental goal of the cruise was the collection and measurement of a 
representative data set of geochemical tracers along the WHP section A2.  The 
data will be used to determine mixing rates and apparent ages of the water 
masses in the North Atlantic.  A special focus is on the deep boundary currents 
along the continental margins and the Mid Atlantic Ridge.  Sampling and 
interpretation will be done in close cooperation with all groups involved.  The 
transient tracer data obtained will be compared with the 1972 GEOSECS data and 
the TTO/NAS data from 1980/81 in the Northern Atlantic.  From the evaluation of 
the tracer fields further indications will be obtained how much and how fast the 
invasion of the tracer signals from the surface into the deep waters has 
proceeded.

The sampling programme was split into two components: small volume samples for 
analyses of the CFCs, helium isotopes, tritium and AMS-14C to be collected with 
the rosette system, and a C-14 programme using large volume samplers.

During M30/2 468 tritium samples have been collected.  About 1 liter of water is 
sampled in glass bottles for determination of the tritium concentration.  In the 
home laboratory from a certain amount of water the helium is degassed 
quantitatively and the sample is stored in a vacuum container for several 
months.  During that time tritium decays and the decay product, 3He, is 
enriched.  The latter will be detected with a special high sensitivity, high 
resolution mass spectrometer. 

For helium measurement ca. 40 cc of sea water are sampled in a copper tube 
sealed with pinch-off clamps.  Analyses will be performed on-shore with a 
dedicated helium isotope mass spectrometer after extraction of the helium 
dissolved in the water.  A total of 474 samples were collected.

In addition samples have been taken to test a seagoing helium extraction system.  
In all 311 samples were taken both parallel and supplementary to the 
conventional sampling procedure.  All samples have been processed onboard, and 
the measurements have been done in the home laboratory after the cruise.  The 
duplicate samples obtained in copper containers as well as several seagoing 
replicate samples will be used to assess the performance of the new system.

Furthermore 60 AMS-14C samples have been drawn from the rosette.  This programme 
is supplementary to the large volume 14C sampling and was restricted mainly to 
the upper water column.

For the large volume sampling ten Gerard-Ewing bottles with a volume of 270 
liter each are used.  The bottles are run in vertical series in two casts at the 
relevant stations.  The shallow cast was followed by a CTD/rosette cast to give 
time to the onboard 14C-extraction and the subsequent preparation of the large 
volume samplers for the deep 14C-cast.  For the M30/2 section 8 large volume 
stations with a total of 204 14C samples have been worked.


PRELIMINARY RESULTS
As a first example of the data from this cruise Fig. (11) shows selected 
profiles of tritium concentrations in the Western Basin.  West of the MAR one 
can distinguish clearly separated depth ranges.  For the LSW depth range we find 
tritium values of 1.2 -1.4 TU.  Deeper, the distribution is more homogeneous, 
particularly in the central basin with a mean concentration of ca 0.75 TU.  On 
the WHP-A1 section further north during leg M30/3 we find for these water masses 
significantly higher concentrations.  We intend to use a multi-tracer approach 
to determine the mixing ratios and spreading rates for these water masses.  We 
will also estimate the mean renewal times for the individual depth ranges.

Fig. (11) Selected tritium profiles for the Western Basin on section A2


5.2.2  MOORING RECOVERY ON WHP- A2 AND WHP-A1
  (BSH, K.P. Koltermann and IfMHH, J. Meincke)

During the Gauss cruise no 226 in the summer of 1993 three moorings were 
deployed west of the Mid Atlantic Ridge on the WOCE section A2 to measure the 
fluctuations and spatial extent of a deep salinity maximum.  These moorings 
could not be turned around in the summer of 1994 and thus a recovery was planned 
as part of this cruise.  Two of the three moorings could be interrogated 
acoustically, one failed to answer.  An attempt to dredge for the mooring K1 in 
a weather lull was not successful.  Weather changes prevented other attempts to 
recover these moorings.

In summer 1995 the mooring K3 was completely and the mooring K1 partially 
recovered from RV Gauss by dredging.  The mooring K2 could not recovered.  From 
K3 some 640 days of data are now available.

The recovery attempts for the mooring D2 on leg M30/3 by dredging was not 
successful.  Further attempts for dredging operations for other moorings had to 
be cancelled because of the prevailing weather and time constraints.


5.2.3  PHYSICAL, CHEMICAL AND TRACER OCEANOGRAPHY ON LEG M30/3

HYDROGRAPHIC MEASUREMENTS ON WHP-A1 
(BSH, A. Sy)

Hydrographic casts were carried out with a NBIS MK-IIIB CTDO2 unit (internal 
name: "DHI-1") mounted on a GO rosette frame with 24 x 10 litre Niskin bottles 
and owned by BSH.  The mean constant maximum descent rate was 1 m/s.  CTDO2 data 
were collected at a rate of 64 ms/cycle using a PC based (HP Vectra 486) data 
acquisition software (CZHEAD rev. 18) designed by BSH.  A video tape unit was 
used as a backup system on each cast.  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 tripping failures 
encountered.

Both pressure and temperature (ITS90) were calibrated before (Sept./Oct. 1994) 
and after the cruise (February 1995) by the calibration facilities at IfM Kiel.  
The post cruise pressure calibration needed to be repeated in November 1995 due 
to uncertainties with results from the February calibration.  Salinity was 
calibrated by comparison of CTD with sample salinities.  24 SIS digital 
temperature meters (RTM 4002) and 7 SIS digital pressure meters (RPM 6000), 
calibrated by the manufacturer in October 1994, were used in a rotating mode 
throughout this cruise leg to control the CTD sensors' stability.  DSRT 
readings, along with salinity, oxygen and chemical data from the rosette water 
samples, were also used to detect erroneous depths of bottle firings.  
Unfortunately, 7 DSRTs were destroyed at the ship's side by heavy sea. 

The bottle sampling sequence was as follows.  Oxygen samples were collected soon 
after the CTD system was brought on board and after CFC and 3He were drawn.  The 
sample water temperature was measured immediately after the oxygen sample was 
drawn.  The next samples drawn were TCO2, 14C, 3H, nutrients (NO2 + NO3, SIO3, 
PO4), and salinity.  All bottle samples taken were linked to the rosette Niskin 
bottles by the "Bedford" sample identification system (see 5.2.1).

Salinity samples were drawn into dry 200 ml BSH salinity bottles with 
polyethylene stoppers and external thread screw caps.  It was found by Kirkwood 
and Folkard (1986) that these bottles guarantee best long-term storage 
conditions, a problem encountered with the old soft glass seawater sample 
bottles (Sy and Hinrichsen, 1986).  Bottles were rinsed three times before 
filling.  Samples were collected as pairs of replicates (i.e. two samples from 
the same rosette bottle), one for shipboard salinity measurements and one for 
backup purposes, e.g. for the possibility of cross checks by later 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 calibration.

In all 18 CTDO2-rosette stations were occupied along section A1/West and 45 
CTDO2-rosette stations along section A1/East (Fig. 12a, List 7.1.3), of which 
the first two casts at station # 489 were used to test winch, cable, two CTD-
rosette systems as well as the sampling procedure and the laboratory equipment.  
Three casts were used for rosette sample quality tests at stat. # 496, 517 and 
542 by means of multi-trips at the same depth level (Table 5.2.3.1).  An 
overview of the locations of water samples is given in Fig. (16 a).  Activities, 
occurrences and measured parameters are summarised in the station listing (List 
7.1.3).

Fig. (12a) Positions of CTDO2/rosette stations for R.V. "Meteor" cruise no. 
           M30/3

Fig. (12)  CTD-sections A1/West, (b) potential temperature (°C), (c) salinity, 
           (d) density (sigma-t)

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 oxygen 
and nutrient samples) were carried out on board during the cruise using BSH 
designed software tools.  The final CTD data processing was done in the 
laboratory at BSH and included the application of corrections to pressure, 
temperature and salinity and the oxygen calibration.  Property sections from CTD 
data are presented in Fig. (12b-d).  CTD data processing and quality evaluation 
will be discussed in greater detail in a separate data report.  All hydrographic 
data are submitted for independent quality evaluation to the WOCE Hydrographic 
Programme Office.

The ADCP was serviced during the St. John's stopover.  The antenna configuration 
of the new Ashtech GPS-system was re-initialised there.  Measurements started on 
Nov. 15,1 1994 and had to be discontinued on Nov 28, 1994 in the Irminger Sea 
due to total collapse of the system due to transducer flooding in heavy weather.  
The third transducer had already failed on Nov 18, 1994.  In all 2983 velocity 
profiles at 6 min intervals have been recorded are being processed with standard 
methods.

TABLE 5.2.3.1: PRECISION OF DUPLICATE SAMPLES (I.E. FROM DIFFERENT ROSETTE 
               BOTTLES FIRED AT THE SAME NOMINAL DEPTH) OF ROSETTE TEST 
               STATIONS.

		STAT. #496	STAT. #517*)	STAT. #542
Duplicates:	N = 19		N = 16		N =11
Parameter	mean±sdv	mean±sdv	mean±sdv
Pctd/db		1473.7±5.7	1401.4±1.2	3948.5±4.0
(Pdsrt)		1471.9 		1402.0±3.5	none 
Tctd/mK		2.8125±.0013	3.0466±.0100	2.4761±.0007 
(Tdsrt)		2.8177±.0028	3.0542±.0077	none 
Delta-T		.0054±.0027	 .0045±.00240	none
Sctd		34.8332±.0011	34.8621±.0012	34.9070±.0002
Sali		34.8320±.0004	34.8617±.0014	34.9050±.0003
Delta-S		-.0013±.0004	-.0004±.0007	
Oxygen		6.9125±.0043	6.8764±.0124	5.5216±.0039 
(ml/l)		(.06 % fs)	(.18 %)		(.07 %)
Nitrate		16.876±.061	17.217±.068	23.507±.0128
(µmol/l)	(.36 % fs)	(.39 %)		(.54 %)
Phosphate	1.0982±.0035	1.0982±.0082	1.5810±.0068 
(µmol/l)	(.32 % fs)	(.75 %)		(.43 %)
Silicate	9.371±.043	9.746±.026	45.110±.056 
(µmol/l)	(.46 % fs)	(.27 %)		(.12 %)
*) Water mass not as homogeneous as desired

It turned out that the pre- and post-cruise laboratory calibrations of pressure 
and temperature were stable (no significant differences) and thus these 
functions were used for the final correction of the field data (Fig. 13, Tab. 
5.2.3.2).

Fig. (13) Pre- and post -cruise calibration
          (a) Pressure at T = 10°C (Oct 94)
          (b) Pressure at T = 1.6°C (Oct 94)
          (c) Pressure at T = 8-9°C (Nov 95)

Fig. (13d) Pre- and post -cruise calibration, Temperature

The salinity correction was carried out by means of in-situ data.  After 
pressure and temperature corrections were applied and salinity recalculated, the 
remaining salinity error consists of a small temporal drift only (Fig. 14).  For 
salinity analysis of samples a standard Guildline Autosal salinometer model 8400 
(s/n 56414) was used on board together with the processing software (SOFTSAL 
with ATS rev. 1.3 and ATSPP rev. 2.1) designed by SIS.  One ampoule of IAPSO 
Standard Seawater (batch P 124) was used per 2 stations (48 samples).  The 
instrument was operated in the ship's constant temperature laboratory at a bath 
temperature of 24°C with the laboratory temperature set to 23°C.  Salinity was 
measured about 2 days after water collection.  No backup seawater sample 
analysis was needed to be carried out.

Oxygen sample measurements were carried out by BSH technicians (see 5.2.3.4).  
Because CTD oxygen sensors cannot be calibrated satisfactorily in the 
laboratory, field calibration is the only alternative.  This procedure was 
carried out in line with the guidelines given by Millard (1993) by merging the 
down-profile CTD data with corresponding up-profile water samples.  Oxygen 
residuals of the final fit versus stations are shown in Fig. (15).

Fig. (14a) Salinity residuals, versus CTD salinity, M30/3

Fig. (14b) Salinity residuals, versus CTD stations, M30/3

Fig. (15)  Oxygen residuals of final fit versus CTD stations


TABLE 5.2.3.2: LABORATORY CALIBRATION COEFFICIENTS FOR CTD "DHI-1" 
               TEMPERATURE AND PRESSURE CORRECTION POLYNOM PCORR, TCORR  (E.G. 
               TNEW = TOLD + TCORR)

	Temperature	Pressure	Pressure 
			(downcast)	(upcast)
a0	 0.0010		-1.68		-2.31
a1	-0.000508	 0.0140268	-0.001693
a2	 9.3139 E-6	-2.14633 E-5	 1.10129 E-6
a3			 1.24996 E-8	-6.08444 E-11
a4			-3.39917 E-12	-1.21793 E-14
a5			 4.39732 E-16	
a6			-2.19759 E-20	

Note:  The a0-coefficients for pressure are caused by the lab calibration 
       procedure only and are not used for pressure correction.  The actual 
       pressure offset protocolled for each station is used as a0.


NUTRIENTS ALONG WHP-A1
(BSH, A. Sy, MAFF. D. Kirkwood)

Along the entire two part of WHP-A1 concentrations of dissolved oxygen and 
nutrients have been analyzed from water samples.  Details of the analyses and 
methods are given in 5.2.3.4 and 5.2.3.5, respectively.  In Fig. (16a-e) we 
display the distribution of the sample positions and the data.

Fig. (16a)   Distribution of water samples along WHP-A1

Fig (16b)    Distribution of the concentrations of dissolved oxygen along WHP-A1

Fig (16c)    Distribution of the concentrations of silicate (16c) along WHP-A1

Fig. (16d-e) Distribution of nitrate (16d) and phosphate (16e) along WHP-A1


SPREADING OF NEWLY FORMED LABRADOR SEA WATER
(BSH, A. Sy)

As an outstanding event, comparable to the "Great Salinity Anomaly" of the mid 
1970s (Dickson et al., 1988), a rapid cooling of the intermediate layer is 
taking place in the subpolar North Atlantic and in the transition zone between 
the subpolar and subtropical gyres during the last years (Koltermann and Sy, 
1994).  This cooling is attributable to a relatively fast spreading of new modes 
of LSW.

The comparison of the LSW core temperatures along section A1 for the years 1991, 
1992 and 1994 (Fig. 17) reveals a clear cooling event in the Irminger Sea in the 
order of -0.23°C in 3 years.  It looks as though every year a new mode of LSW 
arrives in the Irminger Sea ("LSW cascade").  Cooling in the Iceland Basin of -
0.1°C also indicates the arrival of renewed LSW.  The 3-year cooling rate from 
the Rockall Trough area was found to show the same value.  But the arrival of 
the LSW cascade is probably 1 to 2 years later than that in the Iceland Basin.

For the other parameters we find an increase in density of the LSW of 0.018 
kg/m3 for the Irminger Sea and 0.012 kg/m3 for the area east of the MAR (Fig. 
18), and a deepening of LSW which is greatest in the Irminger Sea (250 dbar) and 
Rockall Trough area (200 dbar) (Fig. 19).  However, there is no significant 
signal in salinity (Fig. 20).

The characteristic property change of the cascade of new LSW modes are cooling 
and deepening and only little or no freshening.  Another striking but not 
surprising feature is the separation, by the Reykjanes Ridge, into two different 
hydrographic regimes, the Irminger Sea and the Iceland Basin.  The erosion of 
the LSW core east of the central Iceland Basin (27°W) reflects the longer 
pathway with mixing and enhanced mixing over topography.

These results correspond well with observations of newly formed LSW in the 
central Labrador Sea reported by Lazier (1995).  According to his findings, the 
recent period of LSW formation started in 1988.  He showed that the 
characteristic signal of the new LSW period in its source region is the 
temperature decrease rather than a salinity decrease, and also a distinct 
density increase and deepening.

Because of the similarity of the LSW characteristics found in the Labrador and 
Irminger Seas, Lazier et al. (1995) estimated a circulation time of 8 to 20 
months from the central Labrador Sea to the central Irminger Sea, or a speed of 
1 to 3 cm/s.  The pathway to the eastern North Atlantic is much longer and the 
arrival of the LSW signal will be years later.  If the circulation scheme 
proposed by Talley and McCartney (1982) is adopted, then the water in the 
Iceland Basin should be of more recent origin than that south of the Rockall 
Trough.  The erosion of the LSW core east of the central Iceland Basin is also 
indicative of a longer pathway (see Fig. 20).

It is assumed that the LSW observed in December 1994 south of the Rockall Trough 
is a product of the beginning of the cascade of new LSW modes because in 1991 
and 1992 no significant change was detectable.  That was not the case in the 
Iceland Basin where new LSW arrived earlier. 

For the events observed east of the Reykjanes Ridge, it is concluded that the 
new LSW needed 5 to 6 years to propagate from the source region to the entrance 
of the Rockall Trough.  That corresponds to a mean speed of about 1.5 cm/s which 
is about 3 times faster than suggested by Read and Gould (1992).  From CFC 
measurements a travel time of 8 to 9 years is estimated (see 5.2.3.6).

Fig. (17) Within 3 years the LSW in the Irminger Sea cooled down in the order 
          of -0.23°C.  The 3-year cooling rate from the Iceland Basin and the 
          Rockall Trough area is in the order of -0.1°C

Fig. (18) Within 3 years the density of the LSW core increased by 0.018 kg/m3 
          in the Irminger Sea and by 0.012 kg/m3 in the area east of the MAR

Fig. (19) A mean deepening of the LSW core of about 250 dbar was found for the 
          Irminger Sea and of more than 200 dbar for the Rockall Trough area. 
          For the Iceland Basin a deepening of only 53 dbar was found.

Fig. (20) No striking change of the LSW core salinity appeared within the 3 
          years of observation.


THERMOSALINOGRAPH, XBT AND XCTD MEASUREMENTS 
(BSH, A. Sy)

Unfortunately, underway measurements of surface temperature and salinity along 
section A1 failed, although an Ocean Sensors OS200 Thermosalinograph, which was 
mounted at the ship's laboratory sea water pipe system, worked without technical 
problems.  However, due to the near surface sea water intake, rough sea over 
long periods and the absence of a bubble trap, the data quality was so badly 
affected by air bubbles, that the data were rejected.


XBT SECTIONS
(BSH, A. Sy)

In order to improve the spatial resolution of the hydrographic sections XBT 
profiles were collected at least after each CTD station and halfway between two 
stations (Fig. 11).  157 Sippican T-5 probes (nominal depth range 1830 m) and 8 
Sippican T-7 probes (760 m) were launched from the vessel's stern using a hand-
held launcher.  The data acquisition system used a Compaq SLT/286 laptop 
computer with extension unit, equipped with a Sippican MK-12 interface rev. J, 
firmware rev. 2.1 and NOAA SEAS-III software rev. 3.2.  Where practicable, the 
measurements were carried out according to the guidelines given by Sy (1991).

Fig. (21) Positions of XBT profiles for "Meteor" cruise M30/3

Vertical sections from XBT data are presented in Fig. (22).  The inflection 
points calculated by the SEAS programme were transmitted as BATHY messages via 
BSH into the GTS network.  The complete raw data were processed at BSH according 
the procedures described by Sy and Ulrich (1994).

Fig. (22) XBT sections (a) A1/West, (b) A1/East

For test reasons XBT probes were launched at selected CTD stations in parallel 
to the CTD casts.  The purpose of this test was to provide data from the North 
Atlantic for the international co-ordinated re-evaluation of T-5 and "Fast Deep" 
probe's depth fall rate with the aim of developing community-wide accepted 
recommendations for a new depth formula as already published for T-7, T-6 and T-
4 probes (Hanawa et al., 1995).


XCTD FIELD TEST
(BSH, A. Sy)

An XCTD field evaluation in the eastern North Atlantic from 9 to 14 December 
1994 has completed a series of field trials started in 1992.  The first at-sea 
tests revealed significant deficiencies in the system's performance (Sy, 1993).  
The urgent need to improve the reliability and accuracy of XCTD measurements led 
to the development of various modified devices by the system's manufacturer, 
Sippican, Inc.  The combined modifications result in a new configuration of the 
MK-12 hardware, firmware and software, and also include changes of the XCTD 
probe.  After several field and laboratory tests carried out by the manufacturer 
(Elgin, 1994), the results were sufficiently promising to convince the customer 
of significant improvements of the overall system performance.  The purpose of 
the last field evaluation was to check the manufacturer's specification of the 
final product independently, i.e. from the customer's point of view.  The 
system's accuracy for XCTD measurements is claimed by the manufacturer to be 
±.03°C for temperature, ±.03 mS/cm for conductivity, and ±5 m or 2% for depth 
(Sippican, 1992; 1994).

A total of 12 XCTD probes were calibrated by Sippican, Inc. in September 1994 
and made available for this test.  The data acquisition system was the same as 
for the XBT measurements except a faster Compaq LTE/33C and Sippican's software 
rev. 2.2.1.  The XCTD test sites are located west of the British Isles, because 
this ocean area provides favourable conditions due to its well developed 
hydrographic stratification in both temperature and salinity. 
Severe weather conditions forced a premature end of our regular research 
programme before we had the opportunity to carry out the planned XCTD field 
trial.  Therefore, it was decided to use a combination of T-5 XBT and test XCTD 
probes en route home as a poor makeshift substitute to complete our hydrographic 
section in a rough-and-ready way (XCTD test part A).  After successful and 
problem-free launching of 6 XCTDs at a ship's speed of about 6 knots, we were 
surprised by a sudden unpredicted favourable change of the weather situation.  
We returned to the break-off point of the hydrographic section to resume our 
field work including the originally planned XCTD versus CTD inter-comparisons 
(XCTD test part B).  This field test part was carried out with XCTD drops at 2 
regular CTD stations (stat. # 542 and # 546) side by side with the down-
profiling of the CTD.

All 12 probes launched gave traces from the sea surface to below 1000 m depth.  
No calibration failure and no increasing signal noise with depth was detectable.  
The range of temperature differences between XCTD and CTD traces does not exceed 
the ±0.03°C limit in the homogeneous mixed layer (Fig. 23) and remains within 
this limit also for the deeper ocean (Fig. 24).

The conductivity, however, is low with respect to the reference CTD in the upper 
layer (Fig. 25).  This difference becomes smaller with increasing probe depth 
and eventually falls inside the ±0.03 mS/cm limit in the deeper ocean (Fig. 26).  
At some profiles a significant discrepancy in conductivity (slow start-up) 
appeared in the upper 30 to 60 m (Fig. 25).  Ordinary air bubbles seem to be 
responsible for this effect.  Trapped in the conductivity cell they cause too 
low a conductivity measurement until they collapse by increasing pressure.  On 
the other side, micro air bubbles seem to be responsible for the generally 
reduced conductivity accuracy in the profiles' upper part.

As for XBT probes (Hanawa et al., 1995) the XCTD probes fall faster than 
specified.  The depth fall rate variability is small and the depth error is 
estimated to be about -30 m at 900 m depth (or about 3.3%).  The review of the 
XCTD depth fall rate will be the next action to be taken by the IGOSS Task Team 
on Quality Control of Automated Systems (TT/QCAS). 

Fig. (23) CTD and XCTD temperature profiles of the upper 150 dbar
          (a) at stat. # 542, (b) at stat. # 546

Fig. (24) CTD and XCTD temperature profiles of deeper layers
          (a) at stat. # 542, (b) at stat. # 546

Fig. (25) CTD and XCTD conductivity profiles of the upper 150 dbar
          (a) at stat. # 542, (b) at stat. # 546

Fig. (26) CTD and XCTD conductivity profiles of the deeper layers 
          (a) at stat. # 542, (b) at stat. # 546

The results of the field evaluation conclusively reveal that modification 
efforts of the manufacturer during the last years have resulted in a significant 
MK-12/XCTD system performance improvement.  Obviously most performance 
difficulties encountered at previous sea trials have been successfully solved 
and the system is close to the point of meeting the claimed specification.  
Unsolved deficiencies are the slow conductivity start problem, the reduced 
conductivity accuracy at low pressure, and the inaccurate depth formula.


SAMPLE OXYGEN MEASUREMENTS ON WHP-A1
(BSH, I. Horn, R. Kramer, F. Oestereich)

Oxygen samples were taken from the rosette bottles right after freon and helium 
samples.  A silicone tube of 20 cm length was slipped over the outlet valve of 
the Niskin bottle and used as drawing tube.  Oxygen flasks were rinsed twice 
before filling, then filled with at least a 3 bottle volume overflow to avoid 
the inclusion of air bubbles.  Immediately after each oxygen sample was drawn, 
the reagents MnCl2 and NaI/NaOH were added with the tips of the pipettes below 
the neck of the oxygen flask.  After adding the reagents the flask was stoppered 
and shaken for about two minutes.  Meanwhile the seawater temperature in the 
rosette bottle was measured with a NTC sensor. 

Further analysis was carried out in the laboratory.  After removing the stopper 
1 ml H2SO4 reagent was added and the titration was performed with the oxygen 
flask.  Therefore any loss of iodine was avoided.

Dissolved oxygen analysis was carried out according to the Winkler method 
modified by Carpenter with a Metrohm Titroprozessor 686 and a double platinum 
electrode.  Polarisation titration was used.  The electrodes were driven by a 
constant current of 1 µA.  The resulting voltage was measured as a function of 
the titrant.  Because of the dependence on the sample material (blank, standard, 
seawater sample) an endpoint determination before any measurement was necessary.  
During the cruise the voltage of the endpoint was verified and in case of a 
drift (>20 mV/4-5 samples) an additional correction was applied.  The point of 
equivalence determined from the titration plot is 90- 95% of the endpoint 
voltage which is the voltage minimum.  The calculations were carried out with 
Microsoft Excel 4.0.

An overview on instrumentation and reagents used, standardisation and 
calculation procedures carried out and precision estimated follows.


TECHNICAL EQUIPMENT:
Metrohm Titroprozessor 686,
Dosimat 665+ stirrer E649, 
Polarizer E585,
Thermometer Testotherm 1100, NTC sensor, accuracy 0.1°C,
calibrated oxygen flasks, 
calibrated pipettes for standard solution,
calibrated volumetric flask for standard solution,
calibrated Eppendorf-pipettes for reagents.


REAGENTS:
Potassium Iodate Stand.: 1 hour at 105°C in a dryer, aliquots of about 
0.3567 g; each portion was dissolved in 1 liter pure water; water temperature 
was measured for correction. The weight of KIO3 was corrected for air buoyancy.
Sodium Thiosulphate: Merck Titrisol ampoule, 0.01 mol/l; 2 ampoules within 1 
liter, 0.02 molar.
Alkaline Sodium Iodide: 600 g NaI/l, 4 molar; 320 g NaOH/l, 8 molar.
Manganous Chloride: 600 g (MnCl2 x 4H2O)/l, 3 molar.
Sulphuric Acid: 280 ml concentrated H2SO4/l, 5 molar. 
All reagents were dissolved into demineralized water.


BLANK DETERMINATION:
Blanks were determined in demineralized water weekly according the following 
procedure: 

        1 ml KIO3 + 100 ml H2O + 1 ml H2SO4 + 1 ml NaI/NaOH + 1 ml MnCl2

After titration another 1 ml KIO3 was added followed by a second titration.  The 
difference of the thiosulphate volumes was regarded as reagent blank.  Five 
blanks were determined and the difference between them should be within 0.004 
ml.  The blank value (mean) is an important part of the calculation of oxygen 
concentrations.


STANDARDIZATION:
Standards were determined in demineralized water daily according the following 
procedure:

        10 ml KIO3 + 100 ml H2O + 1 ml H2SO4 + 1 ml NaI/NaOH + 1 ml MnCl2

The titration of the standard was repeated three times.  The scatter of the 
thiosulphate titer should be less than 0.05% (0.002 ml).  For further 
calculations the mean was used.  While standard determination the ambient 
temperature was measured and included in the calculation.


CALCULATION OF OXYGEN CONCENTRATIONS:
	O2 = [(((Vx-Vblk,dw)*VI03*NI03*5598)/(Vstd-Vblk,dw))-1000*DOreg)/(Vbot-Vreg)]
Vx	=thiosulfate titer of sample
Vblk,dw	=thiosulfate titer of pure water blank (cm3)
Vstd	=thiosulfate titer of standard (cm3)
Vbot	=volume of sample bottle (cm3) at sampling temperature
Vreg	=volume (2 cm3) of sample displaced by reagents
VIO3	=volume of iodate standard (cm3) at temperature of standardization
NIO3	=normality of iodate standard (= 6 molarity) at temperature of 
	standardization
DOreg	=absolute amount of oxygen added with reagents, 0.0017 ml (Murray et al, 
	1968)
O2	=oxygen concentration in sample (ml/l)


CALCULATION OF KIO3 STANDARD:
	NI03(tp) = WKI03*Fbuoy, KI03*6/V(tp)*214.001
	V(tp) = V(20)*[1+alpha-v(tp-20)]
NIO3(tp) =normality of iodate standard (= 6 molarity) at tp °C
WKIO3	=weight of KIO3 in air
Fbuoy,KIO3=buoyancy correction for solid KIO3 (=1.000159)
214.001	=1987 molecular weight KIO3
tp	=preparation temperature of KIO3 solution
V(tp)	=volume of volumetric flask at temperature, tp °C
V(20)	=volume of volumetric flask at 20 °C reference temperature
alpha-v	=cubial coefficient of thermal expansion 1.0*10-5 for borosilicate 
	glass


NORMALITY OF KIO3 STANDARD AT REFERENCE TEMPERATURE 20°C:
	NI03(20) =NI03(tp)*[pw(20)/pw(tp)]
NIO3(20)=normality KIO3 at reference temperature 20°C
NIO3(tp)=normality KIO3 at preparation temperature
pw(20)	=density of pure water at reference time 20°C
pw(tp)	=density of pure water at preparation temperature


DENSITY OF PURE WATER:
pw	=0.999842594 + 6.793952*10-5*t - 9.095290*10-6*t2 + 1.001685*10-7*t3 - 
	1.120083*10-9*t4 + 6.536332*10-12*t5
t	=water temperature in °C


NORMALITY OF KIO3 STANDARD AT STANDARDIZATION TEMPERATURE:
	NI03 = NI03(20)*[pw(tstd)/pw(20)]
NIO3(20)=normality of iodate standard at 20°C
pw(tstd)=density of pure water at standardization temperature
pw(20)	=density of pure water at reference temperature 20°C


PRECISION:
With the three calibration stations (# 496, 517, 544) the overall error of 
oxygen measurement between 0.06% fs and 0.18% fc was determined.  Between twelve 
to twenty rosette bottles were released at the same depth to provide independent 
samples of the same water mass.  The results are presented in Fig. (27).

Fig. (27a,b) Results of oxygen measurements at calibration stations, (a) 
             #496,(b) #517

Fig. (27c)   Results of oxygen measurements at calibration stations, (c) #544


NUTRIENT MEASUREMENTS ON WHP-A1
(MAFF, D. S. Kirkwood)

The Skalar SA-4000 auto-analyser and data-system gave trouble-free service 
throughout the cruise.  1257 seawater samples from 63 CTD stations were analysed 
for nitrate, phosphate and silicate.  142 additional analyses were undertaken in 
the course of quality control procedures.


EQUIPMENT AND METHODS:
Nitrate, phosphate and silicate were determined simultaneously using the SA-4000 
segmented continuous-flow auto-analysis system manufactured by Skalar Analytical 
BV, Breda, Netherlands.  The data acquisition and processing software was 
version 6.1.  The chemical methods used are contained in Skalar's (1994) booklet 
on seawater analysis and are summarised briefly here.

Nitrate: Following on-line reduction of nitrate to nitrite by passage through 
a packed column of copperised cadmium granules, a diazo-couple compound is 
formed at pH < 2.4 as described by Bendschneider and Robinson (1952).  Strictly 
speaking, it is the sum (nitrate + nitrite) that is measured, as nitrite, but on 
the assumption that in oceanic work the nitrite contribution is negligible, the 
term nitrate is used throughout.  
Phosphate: Murphy and Riley's (1962) procedure is followed in respect of 
sulphuric acid and molybdate concentrations, but their antimony-containing salt 
is omitted and the reducing agent is hydrazine at 65°C, as in the Oregon State 
University method (Atlas et al., 1971).
Silicate: As the sensitivity of the method is lab-temperature dependent, the 
entire manifold is made from polypropylene tubing and is wound externally around 
the heat exchanger simultaneously used in the phosphate method.  This is very 
similar to the construction proposed by Grasshoff et al. (1983), and the 
chemistry is identical.

These methods are fully discussed and described by Kirkwood (1995), and using 
them, the MAFF (Lowestoft) laboratory has produced high-quality results in the 
two most recent ICES nutrients inter-comparison exercises (Kirkwood et al., 
1991; Aminot et al., 1995).


PROCEDURES:
Samples were drawn from the rosette bottles directly into 1-litre polyethylene 
bottles having a separate neck-insert seal secured by a screw cap.  Bottles and 
seals were rinsed twice with sample and the same two crates (2 x 24) of bottles 
were re-used continuously throughout the cruise with no cleaning between samples 
other than the rinsing procedure.

The sub-sample for analysis was decanted into an 8 ml sampling cup, rinsing 
copiously.  Cups were used new, as supplied, without any pre-cleaning other than 
the rinsing with sample and a dummy-run at the first CTD station.  The same 40 
cups were re-used throughout the cruise and at no time were they allowed to dry 
out.  As a protection against contamination, this regime has proved to be as 
good as any, better than some, and is simple.  Filled cups were placed on the 
carousel in small batches (six or seven) to minimise the period they might be 
exposed to airborne contamination, and to prevent significant bias due to 
evaporation.

Working calibration solutions were freshly prepared daily.  A full calibration 
accompanied each CTD station's samples and consisted of five concentration 
levels with linear intervals in the ranges 0 - 24, 0 - 2, and 0 - 24 µmol/l for 
nitrate, phosphate and silicate respectively, utilising second-order curve-
fitting although the response to concentration is essentially linear in these 
ranges, 0 - 0.66, 0 - 0.12  and 0 - 0.50 absorbance, respectively.  For deeper 
waters in the later part of the cruise (station 535 onward), these ranges were 
extended as required, to accommodate silicate concentrations approaching 40 
µmol/l.

A single analysis of each sample was considered sufficient unless a result 
appeared to be in any way oceanographically inconsistent, in which case the 
analysis was repeated.  Such events were rare and were generally attributable to 
slight but significant phosphate contamination.  Analyses were, in most cases, 
completed within three hours of the rosette's arrival on board.  Results were 
obtained initially on a µmol/l basis and subsequently recalculated to µmol/kg 
taking account of salinity and laboratory ambient temperature, 18 - 20°C.


QUALITY CONTROL:
On November 16th at the first CTD station (# 491/1), twenty-three sampling 
bottles were closed at the same nominal depth as part of rosette and CTD testing 
procedures and residual water from these bottles was collected in a 25-litre 
carboy for nutrients quality control purposes.  This bulk (QC) sample was kept 
cool (in the rosette handling laboratory) but not refrigerated.  A 150 ml sub-
sample was taken daily and analysed, in duplicate, in the course of the analysis 
of rosette samples from each CTD cast.

Note:	Each analytical run begins with a full calibration, which is then followed 
by the rosette samples (in decreasing order of depth) interposed between two 
replicates of the QC sample.  These two replicates are also designated drift 
samples; they are analyzed over an hour apart, and are a check on any (chemical) 
sensitivity drift that may occur during the run.  Sensitivity drift, detected as 
a difference in net peak heights (i.e. after subtraction of the baseline), is 
assumed by the data-system to be linear, and the signal from each rosette sample 
is individually corrected, pro rata, according to its position in the run, 
before its concentration is calculated using the calibration data.  Apparent 
concentrations are calculated (uncorrected) for the two 'drift' peaks so that 
the extent of any drift can be visualised.

No significant drift was observed in phosphate or silicate during any analytical 
run, but for nitrate a consistent trend was evident, the second QC replicate 
almost invariably producing a slightly lower result than the first, the 
difference between their means being 0.24 µmol/l (1.4%).  This observation is 
entirely consistent with the chemistry and hydraulics of the nitrate 
determination, negative drift resulting from a degradation of the reduction 
column's wash-out characteristics due to increasing dead-volume as metal is 
consumed.  It follows that the result produced by the first QC replicate is the 
more accurate because its analysis occurs immediately after calibration and is 
therefore virtually unaffected by drift.  The summary of the QC data takes 
account of this by treating only but for phosphate and silicate, data from both 
QC replicates are treated as equivalent and are pooled.

Full QC data are depicted in Fig. 18. Standard deviations are as follows: 

                   nitrate  phosphate  silicate
relative s.d. (%):  1.38      1.27       0.85

Fig. (28) show a gradual increase in nitrate and phosphate concentrations in the 
          QC sample with time, but no such trend in silicate. This suggests some 
          remineralisation during the 31-day measuring period. The purpose of 
          the sample was to check day-to-day comparability, thereby avoiding 
          serious systematic errors. High stability for this sample over the 
          duration of the cruise was not assumed. It therefore follows that the 
          above standard deviations for nitrate and phosphate are over-
          estimates, and the true day-to-day precision for nitrate and phosphate 
          is similar to that shown for silicate. Errors from a variety of other 
          sources contribute to these standard deviations:

1. Sub-sampling:  (contamination of intermediate container and auto-sampler 
                  cups)
2. Calibration:   (contamination, stability of calibration materials, 
                  gravimetric/volumetric errors)
3. Auto-analyzer: (repeatability of the chemistry, measurement of the chemistry)

Of these, auto-analyzer performance is most amenable to evaluation.  A typical 
sample from station # 535 was analyzed in replicate (x 24) by repeat sampling 
from a 75 ml container suitably positioned on the auto-sampler after removal of 
the carousel.  Standard deviations are as follows:

                   phosphate  nitrate  silicate
relative s.d. (%):   0.36      0.29     0.11

Phosphate performance is the least satisfactory, but its precision approaches 
the noise level of the system.  It is clear that the Skalar SA-4000 analyzer and 
data-system contribute only a small proportion of the total imprecision 
associated with the measurement of typical samples.

Fig. (28a) Quality control samples, (a) nitrate + nitrite and silicate

Fig. (28b) Quality control samples, phosphate


TRACER STUDIES ON WHP-A1
(IUP-HD, R.Bayer and IfMK M.Rhein)

The experimental goal of the tracer programme is the collection and measurement 
of a representative data set for geochemical tracers along the WHP section A1.  
The data will be used to determine mixing rates and apparent ages of the water 
masses in the North Atlantic.  Special focuses are on the North Atlantic 
overturning, the deep boundary currents as observed along the continental 
margins and the Mid Atlantic Ridge and the formation and spreading of Labrador 
Sea Water.

The interpretation of the data will be done in close cooperation with all groups 
involved.  The tracer information will be compared with the 1972 GEOSECS data, 
the TTO/NAS data from 1980/81 in the Northern Atlantic, the data obtained during 
the first occupation of WHP-A1/E in 1991 and other data available from the 
region.  The evaluation of the tracer fields yields further indication how much 
and how fast the invasion of the tracer signals from the surface into the deep 
waters has proceeded.  The observations will specifically give starting 
concentrations for the North Atlantic Deep Water.  Tracer concentrations within 
the overflows will also yield information on the turnover of the water masses 
feeding the overflows.  Moreover, all tracers studied have transient 
distributions and may be used to study the temporal evolution further on.

Onboard measurements were carried out of the CFCs F11 and F12.  Samples for 3He, 
tritium and 14C (large volume programme) were taken for measurement at the 
tracer laboratory at Heidelberg.  Additional 14C samples for Accelerator Mass 
Spectrometry (AMS) were obtained and the subsequent analyses will be performed 
at the Eidgenössische Technische Hochschule Zürich (ETH).  Furthermore a new 
seagoing extraction line for 3He was tested.  All measurements were designed to 
meet the WOCE quality standards.


TRACER OCEANOGRAPHY: TRITIUM/HELIUM AND RADIOCARBON 
(IUP-HD, R. Bayer, M. Born, E. Gier, F. Müller)

OPERATIONAL DETAILS
The sampling programme was divided into two components: small volume samples for 
analyses of the helium isotopes, tritium and AMS-14C were collected with the 
rosette system, and on the other hand a large volume 14C-sampling programme was 
run.  Helium and tritium samples were obtained on 58 stations.  Seven large 
volume casts were performed and a total of 70 LV-14C samples was collected. 

About 580 helium and tritium samples were collected.  About 1 litre of water was 
sampled in glass bottles for determination of the tritium concentration.  In the 
home laboratory the helium is degassed quantitatively from a certain amount of 
water and the sample is stored in a vacuum container for several months.  During 
that time tritium decays and the decay product, 3He, is enriched.  The latter 
will be detected with a special high sensitivity, high resolution mass 
spectrometer.  For helium measurement ca. 40 cc of sea water was sampled in a 
copper tube sealed with pinch-off clamps.  Analyses will be performed on-shore 
with a dedicated helium isotope mass spectrometer after extraction of the helium 
dissolved in the water.

In addition samples were obtained to test a new seagoing helium extraction 
system.  About 330 samples were taken from the rosette both parallel and 
supplementary to the conventional sampling procedure.  All samples were 
processed onboard, and the measurements will be done in the home laboratory soon 
after the end of the cruise.  The duplicates to the samples obtained in copper 
containers as well as several seagoing replicate samples will be used to check 
the performance of the new system.

Furthermore 32 AMS-14C samples were obtained from the rosette.  This programme 
is supplementary to the large volume 14C sampling and was restricted to the 
upper water column.  The total inorganic carbon dissolved in the samples will be 
extracted in the home laboratory.  Measurement of the carbon isotope ratio will 
be done at the AMS facility of the ETH in Zürich/Switzerland.

For the large volume programme Gerard-Ewing bottles with a volume of 270 litre 
each were used.  Ten depth levels were sampled on each cast, and a total of 7 
stations (Labrador Sea 5, Irminger Sea 1, Icelandic Basin 1) was occupied.  The 
total inorganic carbon dissolved in the samples was extracted onboard using two 
separate extraction lines, and the CO2 derived was trapped in sodium hydroxide 
solution.  Further processing of the samples (low-level proportional gas 
counting) will be done in the home laboratory, and the C14 content will be 
determined with a precision of 2 permille or better.


PRELIMINARY RESULTS
The section WHP-A1W (Fig. 29) shows at the southern (A,C) and northern (B,D) 
boundaries of the Labrador Sea close to the surface influences of river run-off 
with its high tritium values.  The deep boundary current system at more than 
2500 m of DSOW is marked with higher tritium concentrations from its source 
region, the Irminger Sea, compared to the water masses of the central Labrador 
Sea.  It also shows a lower 3H/3He age.  The LSW shows a smooth tracer 
distribution: the mean tritium concentration is ca. 1.65 TU and the 
characteristic 3H/3He age ca 7.5 a.  The tracer gradients of the deeper GFZW (or 
NADW) indicate the low ventilation of this water mass.

Fig. (29a,b) Distribution of tritium (A, B) along a section across the 
             Labrador Sea (M30/3, WHP-A1W).

Fig. (29c,d) Distribution of 3H/3He age (C, D) along a section across the 
             Labrador Sea (M30/3, WHP-A1W).


TRACER OCEANOGRAPHY: CFCS 
(IfMK, M.Rhein, P.Heil, A.Schaub)

OPERATIONAL DETAILS
During leg M30/3, the CFC components F11 and F12 have been sampled on 54 
stations and about 700 water samples have been analyzed.  About 10 to 30 ml of 
seawater are transferred from 10 liter Niskin bottles to a Purge and Trap device 
using 100 ml glass syringes.  The O-rings and valves as well as the stainless 
steel springs of the 10 liter Niskin bottles have been precleaned.  The gases 
are separated on a ss packed column, and detected by electron capture detection, 
following the procedures described in Bullister and Weiss, 1988.  Blanks of the 
measurement system and the syringes are determined by degassing CFC free water, 
produced by purging ECD clean Nitrogen permanently through 10 liter seawater.  
The blanks were lower than 0.005 pmol/kg for both, F11 and F12.  Calibration is 
done using a gas standard with near air concentrations kindly provided by R. 
Weiss, SIO.  The values are therefore reported according to the SIO scale.  
Calibration curves with 7 points are carried out before and after the water 
analysis of a station.  It is assumed that the efficiency changes linearly in 
time between the two calibration curves.  CFC concentrations are calculated by 
using the two neighboured calibration points, assuming, that the calibration 
curve is linear between these points.  Reproducibility was checked by replicate 
measurements, at least 4 pairs at each station.  The mean reproducibility for 
single stations varied for both components from ± 0.5% to ± 2.0% with a mean of 
±1.1%.


PRELIMINARY RESULTS
Although the Labrador Sea section could not be completed due to bad weather, 
some of our stations (497-499) represent the central Labrador Sea (Fig. 30).  
The CFC-11 concentrations of LSW (Labrador Sea Water) were as high as 4.5 
pmol/kg, reflecting the recent vigorous convection activities.  Similar high 
values are observed near the bottom in the Denmark Strait Overflow Water (DSOW).  
This high tracer burden originates north of the Denmark Strait, where the 
overflow water was subject to convection.  After overflowing the sill, the 
neighboured water masses in the Irminger Sea (mostly LSW) are entrained.  
Between those tracer maxima, a CFC minimum zone connected to the intermediate 
salinity maximum is found.  They characterize the Gibbs Fracture Zone Water 
(GFZW), which is a mixture of CFC poor Iceland-Scotland Overflow Water and 
entrained North East Atlantic Water.  The NEAW adds the salt and the small CFC 
signal characteristic for this water mass in the sub-polar North Atlantic.

The CFC concentrations in the LSW of the Irminger Sea (Fig. 31) are only 
slightly lower than in the Labrador Sea.  These surprisingly high values found 
in the Irminger Sea, indicates that most likely newly formed LSW invades the 
Irminger Sea within 8 months, which is faster than previously thought.

The horizontal CFC distribution shows the CFC minimum of the GFZW in the 
Irminger Sea spreading along the basin except the western edge.  On the bottom 
of the western flank, the high tracer signal of the DSOW can be observed in two 
or even three near bottom patches, indicating that probably more than one flow 
core of the DSOW exists.  These features were also observed in the tracer 
distributions measured in 1991 (Meteor cruise M18).

The CFC concentrations in the LSW of the Iceland basin are drastically lower 
than in the Irminger Sea (Fig. 32); they reach at the maximum 2.8 pmol/kg CFC-11 
above the Eriador seamount, whereas the Labrador Sea and the Irminger Sea 
exhibit water with 4.4 pmol/kg CFC-11. Moreover the LSW in the Iceland basin is 
warmer and saltier.  These features point to a LSW component in the Iceland sea 
which is older than the one in the Irminger Sea.  On both cruises, M18 and M30, 
the most pronounced LSW was found above the Eriador Seamount, which could be a 
topographic guidance to the inflow of LSW into the Iceland basin.

Fig. (30) CFC11 section (pmol/kg) of the northern part of the WHP-A1W Labrador 
          Sea section

On the eastern flank of the MAR, the tracer core of the GFZW water is found with 
high salinities near 34.97 and a CFC-11 signal of 2.5 pmol/kg.  The salinity and 
the tracer maxima decrease off the ridge.  Below the GFZW, water with decreasing 
CFC concentrations and, similar to the results from 1991, decreasing F11/F12 
ratios near the bottom are observed.

Fig. (31) CFC11 concentrations vs s1,5 for the stations in the Labrador Sea 
          (l) and the central Irminger Sea (x). This density range characterizes 
          Labrador Sea Water (LSW)

Fig. (32) CFC11 section (pmol/kg) along section WHP-A1E

The lowest concentrations are observed in the Lower Deep Water (LDW) which 
enters the Eastern Atlantic through the Romanche (near the equator) and Vema 
Fracture zones (at 11°N).  LDW is a mixture of water from the Circumpolar 
Current (salinity poor, cold and freon poor) and overlying remnants of the 
overflow water masses mostly from the Denmark Strait.  The CFC-11 concentrations 
found in LDW entering the Eastern Atlantic through the Vema Fracture Zone was 
0.05 pmol/kg in March 1994.  The CFC-11 concentrations in LDW in the subpolar 
North Atlantic was found to range between 0.05 to 0.07 pmol/kg, indicating 
further mixing of LDW with neighboured water masses carrying CFCs. 

Surprisingly high CFC values (2.6 pmol/kg) and low salinities were observed near 
16°W, in the density range characterizing LSW.  The Salinity/CFC-11 correlations 
of this water compared to the correlations in the Labrador and Irminger Sea in 
1994 shows that despite the low salinities the water was not formed in 1994 or 
1993 but after 1990.  The water could not be older, because of its high CFC 
content.  The original CFC level the water received during its formation in the 
Labrador Sea has to be higher than the values observed at 16°W.  Thus the time 
scale of the spreading of LSW in the subpolar North Atlantic is significant 
faster than previously thought.


R/V METEOR 30/3 SUBPOLAR NORTH ATLANTIC CHLOROFLUOROCARBONS
(Monika Rhein)

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.

Calibration is done using a gas standard with near air concentrations kindly 
provided by R. Weiss, SIO. 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 
           plotted against station number. The lines represent the mean rms.

Figure 2:  Deep CFC-11 concentrations [pmol kg-1] versus potential 
           temperature [°C], Meteor cruise 39/5, Aug. 1997: stations 566-569 
           (black dots), Meteor cruise 30/3, stations 540-544.


PERFORMANCE 
During cruise Meteor 30/3 the Kiel CFC system worked continuously. Both CFC 
components CFC-11 and CFC-12 had been sampled on 54 stations and about 700 
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 replicate measurements, at least 4 pairs at each 
station. The mean accuracy for single stations varied for both components 
from 0.5% to 2.0% with a mean of 1.2% for CFC-12 and 1.1% for CFC-11 (Figure 
1).

Blanks of the measurement system and the syringes are determined by degassing 
CFC free water, produced by purging ECD clean Nitrogen permanently through 5 
L sea- water. 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 39/5, 
August 1997 (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). If time 
permitted, a calibration curves with 7 points are carried out before and 
after the water analysis of a station. It is assumed that the efficiency 
changes linearly in time between the two calibration curves. CFC 
concentrations are calculated by using the two neighboured calibration 
points, assuming that the calibration curve is linear between these points.

In 1994, we used company precalibrated sample volumes (Machery und Nagel, 
Germany) for the analysis of the 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 sample 
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. The 1994 CFC concentrations 
have been corrected to this calibration.

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.


Figure 3:  CFC-11/CFC-12 ratios versus depth, all CFC data. The open circles 
           present ratios for CFC-11 concentrations lower then 1 pmol kg-1.

Figure 4:  CFC-11/CFC-12 ratios versus depth, star: cruises M45/2 (June 
           1999, eastern North Atlantic), dot: M45/3 (July 1999, western North 
           Atlantic), and circle: M30/3.

Figure 5:  CFC-11 saturation (0-50 m) relative to 265 ppt CFC-11, dot: 94-
           97%, star: 90-94%, circle: 85-90%, and cross: 83-85%.


COMMENTS
During the cruise the WHP section AR7 and the section A1E/AR7E were measured. 
Due to bad weather the Labrador Sea section could not be completed.

The CFC-11/CFC-12 ratios of all measurements are presented in Figure 3. The 
scatter is higher than expected from the accuracy and shifted to higher 
ratios than the values from the Meteor cruises Meteor 45/2 and Meteor 45/3, 
which cover the same region as the Meteor 30/3 cruise (Figure 4). The scatter 
increase considerably when the CFC-11 concentrations are below 1 pmol kg-1.

The CFC-11 surface saturations varied from 83% to 97% (Figure 5), the CFC-12 
saturations from 80% to 101%. Owing to bad weather conditions and heavy 
swell, the shallowest water samples were taken at about 20-40 m depth instead 
of 10 m. The undersaturations are presumably due to the different times 
scales of cooling and/or mixed layer deepening and the air sea gas exchange 
(Figure 5).

Within the Labrador Sea Water (LSW) the CFC-11 concentrations varied between 
2 and 4 pmol kg-1 (Figure 6). Whereas the gradient between the Labrador Sea 
and the Irminger Sea is surprisingly small [Sy et al., 1997].

Similar high values were observed at the bottom in the Denmark Strait 
Overflow Water (DSOW). However, in the east Atlantic this water mass is not 
present and the CFC concentrations reached nearly the detection limit at the 
bottom.

Figure 6:  Cruise Meteor 30/3, all CFC-11 concentrations [pmol kg-1] versus 
           depth.


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.

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 'meteor303.sum'     the bottle file 'meteor303.sea' 
    includes:                           includes:
1  station number                   1  station number
2  year                             2  bottle number
3  month                            3  depth (dbar)
4  day                              4  in-situ temperature (°C)
5  hour: minutes in decimal system  5  salinity (psu)
6  latitude: minutes in decimals    6  CFC-12 (pmol kg-1)
7  longitude: minutes in decimals   7  CFC-11 (pmol kg-1)
8  water depth (m)                  8  WOCE quality flag for CFC-12 
9  depth of CTD profile (m)                              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
          Chromatogram analysis      Shimadzu Integrator C-R4A
          Standard gas               R. Weiss, SIO
          Precision                  CFC-11: 3%, CFC-12: 3%
          Accuracy                   CFC-11: 1.1%, CFC-12: 1.2%
          Blanks                     negligible



5.3  JGOFS PROGRAMMES:

5.3.1  THE CONTROL FUNCTION OF THE CARBONATE-SYSTEM IN THE OCEANIC CO2 UPTAKE, 
       WHP-A2
       (IfMK/J. Duinker, SIO/C. Atwood, IfMK/A. Körtzinger, S. Schweinsberg, 
       A.v. Hippel, C. Senet)

The parameters to determine the oceanic carbonate system are partial pressure of 
CO2 (pCO2) in seawater, total carbonate concentration (TCO2) , alkalinity and 
pH.  The goal is to investigate the CO2 exchange between ocean and atmosphere in 
a regional and seasonal resolution to contribute to a global budget assessment.  
Alkalinity and TCO2 were determined by potentiometric (alkalinity) and coulometric 
titration (TCO2) from hydrocast samples taken at 28 out of the 53 
stations of the cruise (694 samples in total).  During the whole cruise two 
automatic systems were operated to continuously measure the pCO2 and the pH, 
respectively.

While these two systems measured the properties of surface seawater obtained by 
the ship's pumping device, with the latter system also several samples from the 
hydrocast bottles were measured for evaluation of system performance.  At some 
occasions, samples for alkalinity and TCO2 determination were drawn from the 
seawater line to perform a consistency check between all four parameters (21 
samples).

To detect the anthropogenic signal in dissolved carbon, a recalculation of pre-
formed values can be carried out using information about the 'history' of the 
water obtained from oxygen, nutrient, alkalinity and TCO2 values.  The nutrient 
and oxygen data obtained during this cruise will be used for this purpose. 

Another way to follow the invasion of anthropogenic CO2 into the ocean is by 
monitoring the C-12/C-13 ratio, since CO2 emitted by fossil fuel combustion is 
depleted in C-13.  From the hydrocasts, samples were taken for C-13 analysis at 
18 stations (359 samples).  These are being measured at the Institute for Pure 
and Applied Physics at Kiel University, Germany.  From the same samples the O-
16/O-18 ratio can be measured.  This will be done for selected samples.

The pCO2 of seawater is controlled by physical (cooling, wind stress) and/or 
biological (photosynthesis/respiration) processes.  As a means to trace the 
relevance of biological processes, seawater samples from the upper 200 m of the 
water column were filtered for the determination of chlorophyll a were taken and 
filtered at about 30 stations (123 samples).

PRELIMINARY RESULTS
The surface waters along the entire transect contain almost its full component 
of anthropogenic CO2 (ca. 62 µmolkg-1).  Anthropogenic CO2 has penetrated 
through the entire water column west of the Mid-Atlantic Ridge: even in the 
deepest waters (ca. 5000 m) a mean value of 10.4 µmolkg-1 excess CO2 was 
estimated (Körtzinger et al., 1996).

Fig. (33) Cumulated depth profiles of CTant for the western (left) and eastern 
          (right panel) basins of the North Atlantic Ocean along WHP-A2 in 1994. 
          Also shown are the third polynomial least squares fit functions.


5.3.2  THE OCEAN AS A CO2 SINK: COMPLIMENTARY STUDIES OF THE BALTIC SEA AND THE 
       NORTH ATLANTIC, WHP-A1 
       (IOW, B. Schneider, H. Thomas, R. Prado-Fiedler)

During the cruise leg M30/3 measurements of two parameters of the oceanic 
carbonate system were performed along the WOCE lines WHP-A1W and WHP-A1E: the 
CO2 partial pressure in surface water (pCO2) was measured continuously and total 
carbonate (TCO2) profiles were recorded at all stations in 8-12 depths.

The aim of the measurements is the calculation of fluxes of inorganic, dissolved 
carbon. With the data from the pCO2 measurements the exchange between the 
atmosphere and the surface of the ocean can be estimated. In addition with data 
of water masses and their movement it is possible to get an idea of horizontal 
and vertical transport of carbon in the subarctic North Atlantic. In addition to 
these three parameters we make an attempt to develop a model of all fluxes of 
dissolved inorganic carbon in the ocean and between the ocean and the 
atmosphere.


ANALYTICAL METHODS:
TCO2 was determined by a coulometric method (SOMMA). The analytical precision 
was better than ± 1 µmol/kg. The results were checked by measurements of 
standard waters and by determination of the standard deviation. Also comparisons 
of the TCO2 contents of very deep water with results of the earlier cruise M18 
showed a very good agreement. pCO2 was determined by equilibration of an air 
stream with a continuous flow of sea water and subsequent detection of CO2 by an 
infra red spectrometer. Due to the missing of standard water it is difficult to 
determine the error of the measurement.


PRELIMINARY RESULTS
The calculation of the pCO2 requires data from the ship's meteorological 
station, but they have not been available yet. So instead of exact results only 
a first view of the pCO2 data can be given: 

Fig (34) Profiles of total carbonate concentrations for selected stations (#515, 
         #529, #541) of M30/3, section WHP-A1

The range of the pCO2 of the surface water was approx. 360 ppm ± 20 ppm except 
in coastal areas. Thus it was very close to the pCO2 of the air (= 360 ppm). 
This means that the pCO2 of the surface water was in the range of the saturation 
partial pressure and that only low CO2 fluxes occur between the surface of the 
ocean and atmosphere.

Fig. (34) shows three profiles as examples for the TCO2 data, which were 
determined on the WOCE line WHP-A1E, stat. 515 situated in the Irminger Sea, 
stat. 529 in the Iceland Basin and the (JGOFS) stat. 541 in the Rockall Plain. 
The profile of stat. 515 shows the typical behaviour of TCO2, in the Irminger 
Sea and also in the Labrador Sea, which is similar to the nutrients. In all 
profiles the lowest TOC2 values can be observed in the mixed surface layer 
(MSL). The profile of stat. 529 shows a typical behaviour of the eastern part of 
the Northern Atlantic Ocean. In depths between 300 m (stat. 515) and 800 m 
(stat. 529 and 541) the Subpolar Mode Water (SPMW) is identified in different 
distances to its origin: at the stations 529 and 541 is the older water mass 
with higher TCO2 values (2160 µmol/kg) than in station 515 (2153 µmol/kg). The 
water between 1500 m and 2000 m you can identify as the young Labrador Sea Water 
(LSW) with its low TCO2 contents (2145-2150 µmol/kg). The increase in TCO2 
(2160-2170 µmol/kg)in the depth between 2500 m and 3000 m is caused by the older 
Iceland Scotland Overflow Water (ISOW).  At the deepest station 541 occurs the 
Antarctic Bottom Water (AABW) with the highest TCO2 values 2190 µmol/kg), which 
are caused by the highest degree of remineralisation of organic matter. Only in 
the area around stat. 529 there was in the depth between 300 m and 500 m a water 
mass as well with low TCO2 contents (2150 µmol/kg) as with low nutrient 
contents. This is a small stream of Subpolar Surface Water (SPSW). 


5.4  INDIVIDUAL PROGRAMMES:

5.4.1  129I FROM NUCLEAR FUEL PROCESSING AS AN OCEANOGRAPHIC TRACER 
       (CSCSM-CNRS, G. M. Raisbeck)

We have collected 78 samples of 1 l each from WOCE sections A2 and A1.  Samples 
should be resolving the depth profile as good as possible.  Stations sampled are 
typical of the oceanographic regime encountered; four stations per North 
Atlantic Basin, one in each BC region, two in the centre of the basin are now 
ready for analysis.  The samples have been prepared for measurement.  This will 
proceed in the next year.

Fig (35) One year of ALACE data in the Labrador Sea at 1500 m depth. One arrow 
         represents one week's displacement of a float. Individual floats are 
         grey-coded. The bathymetry is overlaid to indicate regions where its 
         effect seems to result in rectified or sluggish flow.


5.4.2  ALACE FLOAT DEPLOYMENTS
       (SIO, R. Davis; WHOI, B.Owens)

During Leg M30/3 in all six ALACE floats were deployed.  Two had additional CTD-
sensors, four only temperature sensors.  After deployment all floats stayed as 
planned for 24 hours on the surface and then sank to the pre-assigned pressure 
level of 1500 dbar.  One S-PALACE (CTD) died after one week, a temperature P-
ALACE died in May 1995.  Four floats are still working.  The tracks of the 
floats for the first year of deployment are shown in Fig (35).



6  SHIP'S METEOROLOGICAL STATION

6.1  LEG M30/1
     (DWD/SWA, G. Kahl)

When "Meteor" left Las Palmas de Gran Canaria on September 6th, 1994, the Azores 
High was at position just south and west of the archipelago thus blocking a cold 
front extending from an Icelandic gale center. The Northeast Trade Winds were 
blowing, force being 6 Bft.

This synoptic situation did not last long, however. The gale center moved from 
southwest of Iceland to the northern part of Azores and then to the southwest, 
reaching the Bahamas and swinging into the Caribbean. South of this 
transatlantic front the subtropical high had sent a wedge into Portugal. 
Consequently, light northerly winds only were experienced by the "Meteor". Winds 
backed west the next day as the research vessel progressed north, force being 5 
Bft on September 10th, too.

By then, however, a gale center had developed in the Gulf of St. Lawrence, and a 
secondary low had made its way across the ocean to the Celtic Sea where it 
intensified. North 6 Bft resulted for "Meteor". During September 12th, the next 
low arriving from the west developed into a gale center even before reaching our 
research vessel's longitude to that northwesterly gales force 7 to 8 Bft tried 
to impede our journey on September 13th and 14th, subsiding by then. While the 
low responsible for that kind of weather developed further into a storm center 
creating havoc in the North Sea, a high was building over Iceland, its wedge 
reaching "Meteor"'s working area. Having arrived at our site, the wedge 
strengthened into a high by itself. As a result, winds were light to that 
scientific work was not impeded. Even the swell did subside. Favourable 
conditions accompanied the "Meteor" into the Channel while conditions in the 
North Sea took their time to calm down on September 18th. Meanwhile, another low 
had arrived to the southwest of Iceland and its secondary low west of Ireland. 
During the last days of the voyage this secondary low moved southeast to east, 
thereby intensifying. "Meteor" strived to keep just ahead of it, experiencing 
moderate winds from southerly to southeasterly directions. 


6.2  LEG M30/2
     (DWD/SWA, E.Röd)

The behaviour of the atmosphere was controlled by the vicinity of a quasi-
permanent westerly jet with a continuous series of ridges and troughs and proved 
to be very close to the climatic average of this belt of prevailing westerlies. 
The weather was somewhat better than expected before, because in spite of the 
advanced season no really extreme pressure was recorded. The lowest value at the 
ship was 984 hPa, the mean 1010 hPa, the deepest low over the northern Atlantic 
just around 970 hPa.  Prevailing wind direction was 245°.

Six well developed cyclonic events were responsible for a remarkably high mean 
wind speed of 25 knots. These eddies originated over the western subtropical 
Atlantic or south of the Great Lakes over the central USA and moved east or 
northeast. This movement however was so slow, that a long lasting intense cold 
sector flow could persist for several days. The series of cyclonic curls ended 
with a low that had formed over Kentucky and then swept in a large curve to 
Belle Isle Strait and the Grand Banks. In connection with this low quite an 
unusual exciting development took place: already since the 25 October at low 
latitudes about 27°N the birth of a tropical disturbance could be seen by the 
spreading of a bright cirrus field that formed a distinct frontal system later 
on. Finally, when this depression had assumed the typical structure of a 
tropical hurricane, it was named "Florence" and remained stationary on its 
position at first. On 6 November 1994 it was caught by the circulation system of 
the low over the St. Lawrence Gulf and accelerated towards north- east. On the 
8th it reached 41°N just at a distance of 180 nm ESE of Meteor. Here the 
northern spiral arm of "Florence" met the warm front of the Newfoundland low. At 
the occlusion point in addition a secondary low pressure core had formed. This 
oblong shaped complex low now swung towards northeast giving free way to a 
northwesterly flow from Labrador down to subtropical latitudes.

The temperature changed widely between 11°C and 21°C depending on warm sector- 
or cold sector conditions. Even higher was the variation of the dew-point: 1°C 
in fresh arctic air and 19°C within moist subtropical warm air. It was 
astounding, that also in warm air over colder water no significant fog patches 
could form.  Only twice during the hole cruise visibility was reduced for less 
than one hour by frontal fog. Due to the cold air advection also the ill-famed 
Newfoundland Banks were free of fog. The small statistic given below shows a 
quasi-Gaussian distribution of wind-force with a maximum of frequencies at 6 
Bft.

The absolute maximum of wind speed was 64 knots. Calm air was not observed at 
all.  The sea was rather rough at times but didn't exceed 7 m of height. Ship's 
manoeuvres and scientific station work were temporarily hampered by hard weather 
but not seriously jeopardized. 

Distribution of wind directions and wind force in Beaufort in percent of a total 
number of 568 hourly observations during M30/2

	First obs: 15.10.94, 01 h
	Last obs : 08.11.94, 23 h
	Number of hourly observations: 568

N	NE	E	SE	S	SW	W	NW	VRB
6	1	1	12	9	13	39	20	0%

0	1	2	3	4	5	6	7	8	9	10	11	12 Bft
<1	1	2	6	13	18	21	18	14	6	<1	<1	0
Rem.:	Between the hourly observations different values may have occurred.


6.3  LEG M30/3
     (DWD/SWA, E. Röd)

The meteorological conditions during the operational phase of the cruise M30/3 
between Hamilton Bank and Porcupine Bank from the 16th of November to the 15th 
of December 1994. 

This leg of the voyage back to Europe was located approximately 900 nm north of 
the preceding one from Europe to Newfoundland and therefore much closer or even 
directly underneath the axis of the polar jet stream. Very frequently in the 
daily radio-soundings maximum winds ranging from 80 to 160 kts could be seen a 
few thousand feet under the tropopause, which in polar cold air came down as far 
as 7 to 8 km with temperatures higher than -50°C. Whereas hurricane "Florence" 
could approach the route of "Meteor" during the preceding leg and join a strong 
polar front low lateron, the second hurricane "Gordon" - extraordinarily late in 
the season - remained in subtropical latitudes far away in the south and faded 
away near Florida. In brief, conditions might be summarized as a typical 
jetstream weather with rapidly alternating lows and ridges. Cyclonic regime 
however was prevailing, which may also be seen in the average atmospheric 
pressure of 990 hPa.  Corresponding to these circumstances wind was rather 
strong with a mean value of 28 kts, that is by 17% more than on the southern 
leg. Cyclogenetic processes were mostly intense, but not extreme. The most 
spectacular pressure fall reached 17 hPa in 3 hours deepening a frontal wave 
into a vigorous storm centre of 950 hPa in the Irminger Sea and Denmark Strait. 
This vortex produced the heaviest storm of the cruise on the 26th and 27th of 
November with nearly constant W 10 gushing up frequently into full 12 Beaufort.

This storm was followed by a less windy week which opened a large "weather 
window" for station work. Between the 5th and the 11th of December a new stormy 
period made research impossible: rapid pressure fall of nearly 5 hPa/h announced 
the approach of a vortex nearly equally intense (963 hPa) as the preceding one. 
The sharp pressure rise in its cold sector originated a long lasting 
northwesterly to westerly flow. On the 6th of December hurricane-like gusts 
exceeding 100 knots marked the absolute wind maximum of the whole cruise. 
Towards the end of November at 59°N/34°W as a counterpart to subtropical 
hurricanes a typical Polar Low could be observed near the ship. Under weak 
gradient conditions, which geostrophically could have brought only 2 or 3 Bft, 
wind remained nearly constantly about 7 Bft.  Examining closely the satellite 
image the sub-scale polar eddy with its characteristic structure could be 
detected.

On 9 December, 1994 dramatic numerical forecasts suggested to leave the ship's 
position as soon as possible heading towards the English Channel. Fortunately 
already on the following day this prognosis was replaced by a quite optimistic 
one which proved to be correct when "Meteor" had returned to the working area. 
Under high pressure conditions the transect could be completed without any 
meteorological problems. This case was quite a good lesson about the reliability 
of medium range forecasts. It was striking during this cruise that several 
depressions were born on the leeward side of the Rocky Mountains west of the 
Great Lakes, but even more originated over the area between the Caribbean Sea 
and the Bermuda. This is to be ascribed to the fact, that frequent Anticyclones 
over the North American continent drove arctic cold air far down into the south 
against subtropical warm air, whereas cyclogenetic processes in more or less 
uniform cold air masses over Canada remained rather weak.

Visibility was nearly always good, mostly unlimited. The duration of the 
extremely rare fog events due to frontal processes was less than half an hour. 
The average atmospheric pressure amounted to 995 hPa with a lowest value of 
956,5 hPa and a maximum of 1031,5 hPa. The mean wind was 234°/28 knots. 

Statistics for the period 16.11.-14.12.94 

Distribution of wind directions and wind force in Beaufort in percent of a total 
number of 695 hourly observations. 

Wind Directions
N	NE	E	SE	S	SW	W	NW	VRB
11.5	2.4	5.0	5.6	10.8	16.5	28.6	19.3	0.0%

Wind Force
0	1	2	3	4	5	6	7	8	9	10	11	12 Bft
1.0	1.2	1.9	3.9	0.4	17.4	16.1	12.9	18.6	9.2	4.9	1.6	1.0%

Distribution of wave heights in meter in percent of a total number of 160 visual 
observations during daylight. 
0	1	2	3	4	5	6	7	8	9	10	11	12
0.6	4.4	10.6	31.9	25.6	16.9	6.3	2.5	0.6	0.6	0	0	0%

In the hourly wind measurements and the three-hourly wave observations higher 
values might have occurred. Thus the absolute wind maximum of 100 kts and the 
highest waves exceeding 10 m do not show up in that list. 



7  LISTS

7.1  LIST OF STATIONS

7.1.1  LISTS OF SAMPLING STATIONS M30/1

Water samplers: 	Go-Flows, Rosette sampler, Marine snow catcher
Sediment samplers:	Multiple corer, Box grab
Water column profiling:	CTD

STATION	DATE	GEAR		COORDINATES			SAMPLING
NO.	(1994)			N		W		DEPTH (M)
422	09.09.	Multiple corer	38 28,5'	15 53,0'	4989
		(failed)			
423	09.09.	CTD/Rosette	39 18,3'	15 55,7'	0-3500
424	10.09.	Multiple corer	41 49,8'	16 03,7'	5330
425	12.09.	Go-Flows	48 56,9'	16 26,7'	0-1200
		Multiple corer	48 58,4'	16 28,4'	4805
		(failed)			
		Multiple corer	48 58,3'	16 28,3'	4805
		Go-Flows	48 59,7'	16 26,7'	0-200
		Go-Flows	48 59,8'	16 26,7'	0-200
		Multiple corer	48 59,7'	16 26,5'	4807
426	13.09.	Multiple corer	48 59,1'	13 45,1'	4500
		Box grab	48 59,4'	13 45,3'	4469
		(failed)			
427	14.09.	Go-Flows	49 03,2'	13 24,6'	0-1500
		Bottom lander	49 04,0'	13 23,4'	3635
		(partly failed)			
		CTD		49 05,5'	13 24,7'	0-500
		Multiple corer	49 05,5'	13 24,8'	3665
428	15.09.	CTD		49 08,9'	13 05,2'	0-500
		Rosette		49 08,9'	13 05,2'	0-1500
		Multiple corer	49 09,0'	13 05,6'	2268
428		Box grab	49 09,0'	13 05,5'	2277
		(failed)			
		Box grab	49 09,0'	13 05,6'	2260
		Go-Flows	49 09,8'	13 08,7'	0-2200
429	15.09.	Marine snow	49 04,7'	13 24,2'	50
		catcher			
		Marine snow	49 04,7'	13 24,4'	50
		catcher			
		CTD		49 04,6'	13 25,0'	0-500
		Go-Flows	49 04,4'	13 25,1'	0-50
		Multiple corer	49 03,7'	13 23,3'	3629
430	16.09.	CTD		49 11,0'	12 50,8'	0-500
		Rosette		49 11,0'	12 50,8'	0-1400
		Multiple corer	49 11,1'	12 51,0'	1535
		Box grab	49 11,1'	12 50,9'	1529
431	16.09.	Go-Flows	49 14,0'	12 30,2'	0-1100 
		Multiple corer	49 14,0'	12 30,0'	1165
432		Go-Flows	49 13,2'	12 48,9'	0-1300
433		Box grab	49 14,2'	12 29,6'	1158
		CTD		49 14,5'	12 29,4'	0-500m
	17.09.	Rosette		49 14,0'	12 28,9'	0-1000
434	17.09.	Multiple corer	49 24,1'	11 32,1'	674
		Box grab	49 24,0'	11 32,2'	674
		CTD		49 25,2'	11 32,2'	673
		Go-Flows	49 24,9'	11 32,2'	0-650
		Rosette		49 25,0'	11 33,8'	0-650
435		Multiple corer	49 27,9'	11 12,2'	227
		Multiple corer	49 28,0'	11 12,5'	230
		Multiple corer	49 28,0'	11 12,4'	231
		CTD		49 28,0'	11 09,4'	0-200
		Go-Flows	49 28,4'	11 08,7'	0-200
		Rosette		49 28,4'	11 08,5'	0-200
		Multiple corer	49 28,6'	11 08,0'	231


7.1.2	STATION LIST LEG M30/2 SECTION WHP-A2

EXPO-	 WOCE	STAT.	CAST	CAST	DATE	TIME	CODE	POSITION			CODE	BOTTOM	METER	MAX	BOTTOM	NO.OF	PARAMETERS	COMMENTS
CODE	 WHP-ID	NO.	NO.	TYPE		UTC		LATITUDE	LONGITUDE		DEPTH	WHEEL	PRES	DIST.	BTLS		
06MT30/2 A2	436	01	ROS	101594	1232	BE	48 09.9 N	11 44.9 W	GPS	3422					
06MT30/2 A2	436	01	ROS	101594	1338	BO	48 09.9 N	11 44.9 W	GPS	3422		3236		12	1-4,6,7,8,27,28
06MT30/2 A2	436	01	ROS	101594	1511	EN	48 09.9 N	11 45.2 W	GPS	3422					
06MT30/2 A2	436	02	LVS	101594	1605	BO	48 09.9 N	11 45.0 W	GPS	3430		300		5	1,12,13
06MT30/2 A2	436	03	ROS	101594	1648	BE	48 10.0 N	11 45.3 W	GPS	3418					
06MT30/2 A2	436	03	ROS	101594	1810	BO	48 10.1 N	11 45.7 W	GPS	3418		3201		24	1-2
06MT30/2 A2	436	03	ROS	101594	1952	EN	48 10.1 N	11 46.3 W	GPS	3418					
06MT30/2 A2	437	01	ROS	101694	0444	BE	49 14.1 N	10 40.0 W	GPS	0154					
06MT30/2 A2	437	01	ROS	101694	0449	BO	49 14.0 N	10 39.7 W	GPS	0154		132	20	7	1-4,6
06MT30/2 A2	437	01	ROS	101694	0507	EN	49 13.9 N	10 39.6 W	GPS	0154					
06MT30/2 A2	438	01	ROS	101694	0658	BE	49 11.6 N	11 11.1 W	GPS	0192					
06MT30/2 A2	438	01	ROS	101694	0702	BO	49 11.6 N	11 11.1 W	GPS	0192		173		10	1-4,6,7,8,27,28
06MT30/2 A2	438	01	ROS	101694	0718	EN	49 11.6 N	11 10.9 W	GPS	0192					
06MT30/2 A2	439	02	ROS	101694	0928	BE	49 10.7 N	11 25.6 W	GPS	0478					
06MT30/2 A2	439	02	ROS	101694	0943	BO	49 10.7 N	11 25.6 W	GPS	0478		461		11	1-4,6
06MT30/2 A2	439	02	ROS	101694	1003	EN	49 10.7 N	11 25.6 W	GPS	0478					
06MT30/2 A2	440	01	ROS	101694	1257	BE	49 06.4 N	12 11.7 W	GPS	1001					
06MT30/2 A2	440	01	ROS	101694	1318	BO	49 06.4 N	12 11.7 W	GPS	1001		985	20	17	1-4,6,7,8,27,28
06MT30/2 A2	440	01	ROS	101694	1356	EN	49 06.4 N	12 11.6 W	GPS	1001					
06MT30/2 A2	441	01	ROS	101694	1600	BE	49 03.1 N	12 42.3 W	GPS	1502					
06MT30/2 A2	441	01	ROS	101694	1630	BO	49 03.3 N	12 42.3 W	GPS	1502		1501	20	21	1-4,6,7,8,27,28
06MT30/2 A2	441	01	ROS	101694	1720	EN	49 03.5 N	12 42.1 W	GPS	1502					
06MT30/2 A2	442	01	ROS	101694	1853	BE	49 01.2 N	12 51.4 W	GPS	1986					
06MT30/2 A2	442	01	ROS	101694	1934	BO	49 01.2 N	12 51.4 W	GPS	1986		1994	20	24	1-4,6,7,8,27,28
06MT30/2 A2	442	01	ROS	101694	2034	EN	49 01.2 N	12 51.3 W	GPS	1986					
06MT30/2 A2	443	01	ROS	101694	2159	BE	49 00.0 N	12 58.8 W	GPS	2500					
06MT30/2 A2	443	01	ROS	101694	2245	BO	49 00.2 N	12 58.5 W	GPS	2500	2500	2510		24	1-4,6,7,8,27,28
06MT30/2 A2	443	01	ROS	101694	2359	EN	49 00.4 N	12 57.9 W	GPS	2500					
06MT30/2 A2	444	02	ROS	101794	0425	BE	48 59.9 N	13 02.6 W	GPS	3068					
06MT30/2 A2	444	02	ROS	101794	0523	BO	49 59.8 N	13 02.6 W	GPS	3068		3127	20	23	1-4,6
06MT30/2 A2	444	02	ROS	101794	0642	EN	48 59.8 N	13 02.7 W	GPS	3068					
06MT30/2 A2	445	01	LVS	101794	0925	BO	48 55.0 N	13 16.5 W	GPS	3725		1700		10	1,12,13
06MT30/2 A2	445	02	ROS	101794	1106	BE	48 55.5 N	13 17.1 W	GPS	3718					
06MT30/2 A2	445	02	ROS	101794	1220	BO	48 55.6 N	13 16.5 W	GPS	3718		3735	20	23	1-4,6,7,8,27,28
06MT30/2 A2	445	02	ROS	101794	1349	EN	48 55.4 N	13 16.7 W	GPS	3718					
06MT30/2 A2	445	03	LVS	101794	1616	BO	48 55.2 N	13 16.8 W	GPS	3726		3670		10	1,12,13
06MT30/2 A2	445	04	ROS	101794	1908	BE	48 55.2 N	13 16.8 W	GPS	3726					
06MT30/2 A2	445	04	ROS	101794	1938	BO	48 55.2 N	13 16.9 W	GPS	3726		1180		19	1-4,6,7,8,27,28
06MT30/2 A2	445	04	ROS	101794	2029	EN	48 55.1 N	13 16.7 W	GPS	3726					
06MT30/2 A2	446	01	ROS	101794	2242	BE	48 51.4 N	13 46.0 W	GPS	4495					
06MT30/2 A2	446	01	ROS	101794	2302	BO	48 51.3 N	13 46.2 W	GPS	4495		1049		16	1-4,6
06MT30/2 A2	446	01	ROS	101794	2341	EN	48 51.2 N	13 46.5 W	GPS	4495					
06MT30/2 A2	446	03	ROS	101894	0352	BE	48 51.6 N	13 46.2 W	GPS	4490					
06MT30/2 A2	446	03	ROS	101894	0513	BO	48 51.5 N	13 46.1 W	GPS	4490		4562	20	24	1-4,6
06MT30/2 A2	446	03	ROS	101894	0654	EN	48 51.5 N	13 46.1 W	GPS	4490					
06MT30/2 A2	447	01	ROS	101894	1426	BE	48 39.1 N	14 21.4 W	GPS	4552					
06MT30/2 A2	447	01	ROS	101894	1549	BO	48 38.6 N	14 21.3 W	GPS	4552		4603	20	23	1-4,6,7,8,27,28
06MT30/2 A2	447	01	ROS	101894	1733	EN	48 38.0 N	14 21.5 W	GPS	4552					
06MT30/2 A2	448	01	ROS	101894	2054	BE	48 44.2 N	14 55.6 W	GPS	4707					
06MT30/2 A2	448	01	ROS	101894	2222	BO	48 43.9 N	14 45.3 W	GPS	4707		4743		23	1-4,6,7,8,27,28
06MT30/2 A2	448	01	ROS	101994	0011	EN	48 43.5 N	14 44.8 W	GPS	4707					
06MT30/2 A2	449	01	ROS	102094	0901	BE	48 21.1 N	17 20.4 W	GPS	4143					
06MT30/2 A2	449	01	ROS	102094	0950	BO	48 20.9 N	17 20.7 W	GPS	4143		2200		22	1-4,6,7,8,27,28
06MT30/2 A2	449	01	ROS	102094	1051	EN	48 20.9 N	17 21.0 W	GPS	4143					
06MT30/2 A2	449	02	ROS	102094	1110	BE	48 20.9 N	17 21.1 W	GPS	4127					
06MT30/2 A2	449	02	ROS	102094	1222	BO	48 20.9 N	17 21.3 W	GPS	4127		4170		23	1-4,6,7,8,27,28
06MT30/2 A2	449	02	ROS	102094	1348	EN	48 20.7 N	17 21.3 W	GPS	4127					
06MT30/2 A2	450	01	LVS	102094	2026	BO	48 13.0 N	18 26.0 W	GPS	4510		1700		10	1,12,13
06MT30/2 A2	450	02	ROS	102094	2215	BE	48 12.5 N	18 25.6 W	GPS	4510					
06MT30/2 A2	450	02	ROS	102094	2322	BO	48 11.8 N	18 25.3 W	GPS	4510		4539		23	1-4,6,7,8,27,28
06MT30/2 A2	450	02	ROS	102194	0018	EN	48 11.7 N	18 26.1 W	GPS	4510					
06MT30/2 A2	450	03	LVS	102194	0332	BO	48 12.1 N	18 26.3 W	GPS	4514		4391		10	1,12,13
06MT30/2 A2	450	04	ROS	102194	0622	BE	48 12.5 N	18 26.2 W	GPS	4444					
06MT30/2 A2	450	04	ROS	102194	0720	BO	48 12.4 N	18 25.8 W	GPS	4444		1599		17	1-4,6,7,8,27,28
06MT30/2 A2	450	04	ROS	102194	0808	EN	48 12.5 N	18 25.9 W	GPS	4444					
06MT30/2 A2	451	01	ROS	102194	1210	BE	48 06.3 N	19 10.0 W	GPS	4176					
06MT30/2 A2	451	01	ROS	102194	1237	BO	48 06.4 N	19 10.4 W	GPS	4176		1603		16	1-4,6,7,8,27,28
06MT30/2 A2	451	01	ROS	102194	1318	EN	48 06.4 N	19 10.7 W	GPS	4176					
06MT30/2 A2	451	02	ROS	102194	1331	BE	48 06.6 N	19 10.4 W	GPS	4183					
06MT30/2 A2	451	02	ROS	102194	1441	BO	48 06.5 N	19 10.5 W	GPS	4183		4238		23	1-4,6,7,8,27,28
06MT30/2 A2	451	02	ROS	102194	1610	EN	48 06.3 N	19 10.6 W	GPS	4183					
06MT30/2 A2	452	01	ROS	102394	0001	BE	47 53.1 N	20 55.3 W	GPS	4447					
06MT30/2 A2	452	01	ROS	102394	0120	BO	47 53.0 N	20 56.1 W	GPS	4447		4525	17	24	1-4,6,7,8,27,28
06MT30/2 A2	452	01	ROS	102394	0301	EN	47 53.1 N	20 56.7 W	GPS	4447					
06MT30/2 A2	452	02	ROS	102394	0350	BE	47 52.9 N	20 55.8 W	GPS	4448					
06MT30/2 A2	452	02	ROS	102394	0520	BO	47 53.3 N	20 55.8 W	GPS	4448	4249	4500	20	19	1-4,6,7,8,27,28
06MT30/2 A2	452	02	ROS	102394	0640	EN	47 53.3 N	20 56.6 W	GPS	4448					
06MT30/2 A2	453	01	ROS	102394	1200	BE	47 42.2 N	22 05.7 W	GPS	4434					
06MT30/2 A2	453	01	ROS	102394	1310	BO	47 42.0 N	22 05.6 W	GPS	4434		4303		24	1-4,6,7,8,27,28
06MT30/2 A2	453	01	ROS	102394	1429	EN	47 42.0 N	22 05.7 W	GPS	4434					
06MT30/2 A2	453	02	LVS	102394	1548	BO	47 42.3 N	22 05.2 W	GPS	4433		1800		10	1,12,13
06MT30/2 A2	453	03	ROS	102394	1740	BE	47 42.4 N	22 05.7 W	GPS	4433					
06MT30/2 A2	453	03	ROS	102394	1918	BO	47 42.4 N	22 05.5 W	GPS	4433		4505	19	27	1-4,6,7,8,27,28
06MT30/2 A2	453	03	ROS	102394	2050	EN	47 42.3 N	22 05.4 W	GPS	4433					
06MT30/2 A2	453	04	ROS	102394	2303	BE	47 42.2 N	22 05.5 W	GPS	4436					
06MT30/2 A2	453	04	ROS	102394	2343	BO	47 42.1 N	22 05.6 W	GPS	4436		2110		27	1-4,6,7,8,27,28
06MT30/2 A2	453	04	ROS	102494	0050	EN	47 41.8 N	22 05.6 W	GPS	4436					
06MT30/2 A2	454	01	ROS	102494	0303	BE	47 32.4 N	22 27.4 W	GPS	4467					
06MT30/2 A2	454	01	ROS	102494	0340	BO	47 32.4 N	22 27.3 W	GPS	4467		1500		19	1-4,6
06MT30/2 A2	454	01	ROS	102494	0440	EN	47 32.4 N	22 27.3 W	GPS	4467					
06MT30/2 A2	454	02	ROS	102494	0459	BE	47 32.6 N	22 27.4 W	GPS	4466					
06MT30/2 A2	454	02	ROS	102494	0618	BO	47 32.5 N	22 27.3 W	GPS	4466		4543		26	1-4,6
06MT30/2 A2	454	02	ROS	102494	0802	EN	47 32.5 N	22 27.2 W	GPS	4466					
06MT30/2 A2	455	01	ROS	102494	1010	BE	47 36.3 N	22 48.9 W	GPS	4177					
06MT30/2 A2	455	01	ROS	102494	1051	BO	47 36.3 N	22 48.8 W	GPS	4177		1899		20	1-4,6,7,8,27,28
06MT30/2 A2	455	01	ROS	102494	1201	EN	47 36.1 N	22 48.9 W	GPS	4177					
06MT30/2 A2	455	02	LVS	102494	1400	BO	47 35.8 N	22 48.7 W	GPS	4238		4210		10	1,12,13
06MT30/2 A2	455	03	ROS	102494	1649	BE	47 36.2 N	22 49.1 W	GPS	4238					
06MT30/2 A2	455	03	ROS	102494	1805	BO	47 35.9 N	22 49.0 W	GPS	4238		4304		27	1-4,6,7,8,27,28
06MT30/2 A2	455	03	ROS	102494	1952	EN	47 35.5 N	22 49.1 W	GPS	4238					
06MT30/2 A2	456	01	ROS	102494	2313	BE	47 29.3 N	23 33.3 W	GPS	3967					
06MT30/2 A2	456	01	ROS	102494	2344	BO	47 29.3 N	23 33.7 W	GPS	3967		1302		20	1-4,6
06MT30/2 A2	456	01	ROS	102594	0051	EN	47 29.5 N	23 34.1 W	GPS	3967					
06MT30/2 A2	456	02	ROS	102594	0104	BE	47 29.5 N	23 34.1 W	GPS	3964					
06MT30/2 A2	456	02	ROS	102594	0210	BO	47 29.4 N	23 33.6 W	GPS	3964		4030	19	27	1-4,6
06MT30/2 A2	456	02	ROS	102594	0346	EN	47 29.4 N	23 33.5 W	GPS	3964					
06MT30/2 A2	457	01	ROS	102594	0659	BE	47 22.9 N	24 15.8 W	GPS	3315					
06MT30/2 A2	457	01	ROS	102594	0724	BO	47 23.0 N	24 16.0 W	GPS	3315			866	11	1-4,6,7,8,27,28
06MT30/2 A2	457	01	ROS	102594	0757	EN	47 23.1 N	24 15.9 W	GPS	3315					
06MT30/2 A2	457	02	ROS	102594	0823	BE	47 23.1 N	24 15.7 W	GPS	3317					
06MT30/2 A2	457	02	ROS	102594	0919	BO	47 23.0 N	24 15.1 W	GPS	3317		3312	23	28	1-4,6,7,8,27,28
06MT30/2 A2	457	02	ROS	102594	1105	EN	47 23.1 N	24 17.0 W	GPS	3317					
06MT30/2 A2	458	01	ROS	102594	1523	BE	47 14.1 N	25 22.3 W	GPS	2886					
06MT30/2 A2	458	01	ROS	102594	1545	BO	47 13.9 N	25 22.3 W	GPS	2886			902	14	1-4,6,7,8,27,28
06MT30/2 A2	458	01	ROS	102594	1627	EN	47 14.0 N	25 22.3 W	GPS	2886					
06MT30/2 A2	458	02	LVS	102594	1755	BO	47 13.9 N	25 22.3 W	GPS	2894		2820		10	1,12,13
06MT30/2 A2	458	03	ROS	102594	1947	BE	47 14.0 N	25 22.2 W	GPS	2863					
06MT30/2 A2	458	03	ROS	102594	2040	BO	47 14.1 N	25 22.2 W	GPS	2863		2868	20	27	1-4,6,7,8,27,28
06MT30/2 A2	458	03	ROS	102594	2221	EN	47 13.5 N	25 23.1 W	GPS	2863					
06MT30/2 A2	459	01	ROS	102694	0144	BE	47 06.3 N	26 17.3 W	GPS	2430					
06MT30/2 A2	459	01	ROS	102694	0224	BO	47 06.3 N	26 17.2 W	GPS	2430		2373	12	28	1-4,6,7,8,27,28
06MT30/2 A2	459	01	ROS	102694	0341	EN	47 06.4 N	26 17.2 W	GPS	2430					
06MT30/2 A2	460	01	ROS	102694	0517	BE	47 04.4 N	26 39.8 W	GPS	2716					
06MT30/2 A2	460	01	ROS	102694	0601	BO	47 04.5 N	26 39.5 W	GPS	2716		2717	19	28	1-4,6,7,8,27,28
06MT30/2 A2	460	01	ROS	102694	0717	EN	47 04.5 N	26 39.4 W	GPS	2716					
06MT30/2 A2	461	01	ROS	102694	0853	BE	46 59.4 N	26 59.8 W	GPS	2120					
06MT30/2 A2	461	01	ROS	102694	0934	BO	46 59.3 N	26 59.8 W	GPS	2120		2123	21	27	1-4,6
06MT30/2 A2	461	01	ROS	102694	1042	EN	46 58.8 N	27 00.0 W	GPS	2120					
06MT30/2 A2	462	01	ROS	102694	1232	BE	46 54.3 N	27 23.3 W	GPS	2770					
06MT30/2 A2	462	01	ROS	102694	1325	BO	46 53.9 N	27 23.3 W	GPS	2770		2803	17	27	1-4,6,7,8,27,28
06MT30/2 A2	462	01	ROS	102694	1438	EN	46 53.9 N	27 23.5 W	GPS	2770					
06MT30/2 A2	463	01	ROS	102694	1624	BE	46 49.4 N	27 50.6 W	GPS	2440					
06MT30/2 A2	463	01	ROS	102694	1705	BO	46 49.3 N	27 50.4 W	GPS	2440		2456	18	28	1-4,6,7,8,27,28
06MT30/2 A2	463	01	ROS	102694	1821	EN	46 49.4 N	27 50.6 W	GPS	2440					
06MT30/2 A2	464	01	ROS	102694	2018	BE	46 42.6 N	28 18.2 W	GPS	3450					
06MT30/2 A2	464	01	ROS	102694	2113	BO	46 42.6 N	28 18.1 W	GPS	3450		3464		28	1-4,6,7,8,27,28
06MT30/2 A2	464	01	ROS	102694	2245	EN	46 42.7 N	28 18.0 W	GPS	3450					
06MT30/2 A2	465	01	ROS	102794	1911	BE	46 20.4 N	30 00.7 W	GPS	3125					
06MT30/2 A2	465	01	ROS	102794	2045	BO	46 20.5 N	30 00.8 W	GPS	3125		3114	19	27	1-4,6,7,8,27,28
06MT30/2 A2	465	01	ROS	102794	2142	EN	46 20.5 N	30 00.8 W	GPS	3125					
06MT30/2 A2	466	01	ROS	102894	0026	BE	46 12.3 N	30 36.6 W	GPS	3625					
06MT30/2 A2	466	01	ROS	102894	0131	BO	46 12.3 N	30 36.8 W	GPS	3625		3643	18	27	1-4,6,7,8,27,28
06MT30/2 A2	466	01	ROS	102894	0308	EN	46 12.3 N	30 37.0 W	GPS	3625					
06MT30/2 A2	467	01	ROS	102894	0542	BE	46 04.2 N	31 12.8 W	GPS	3347					
06MT30/2 A2	467	01	ROS	102894	0640	BO	46 04.1 N	31 12.8 W	GPS	3347		3361	19	27	1-4,6,7,8,27,28
06MT30/2 A2	467	01	ROS	102894	0808	EN	46 04.2 N	31 12.9 W	GPS	3347					
06MT30/2 A2	468	01	ROS	102894	1323	BE	45 54.6 N	31 48.6 W	GPS	3601					
06MT30/2 A2	468	01	ROS	102894	1348	BO	45 54.4 N	31 48.6 W	GPS	3601		1401		24	1-4,6,7,8,27,28
06MT30/2 A2	468	01	ROS	102894	1443	EN	45 54.6 N	31 48.7 W	GPS	3601					
06MT30/2 A2	468	02	LVS	102894	1637	BO	45 54.6 N	31 48.4 W	GPS	3658		3602		10	1,12,13
06MT30/2 A2	468	03	ROS	102894	1857	BE	45 54.5 N	31 48.5 W	GPS	3639					
06MT30/2 A2	468	03	ROS	102894	1956	BO	45 54.5 N	31 48.6 W	GPS	3639		3695	18	28	1-4,6,7,8,27,28
06MT30/2 A2	468	03	ROS	102894	2141	EN	45 54.4 N	31 48.4 W	GPS	3639					
06MT30/2 A2	469	01	ROS	102994	0741	BE	45 41.5 N	32 18.4 W	GPS	3588					
06MT30/2 A2	469	01	ROS	102994	0809	BO	45 41.5 N	32 18.1 W	GPS	3588		1101		14	1-4,6,7,8,27,28
06MT30/2 A2	469	01	ROS	102994	0904	EN	45 41.6 N	32 17.2 W	GPS	3588					
06MT30/2 A2	469	02	ROS	102994	0919	BE	45 41.6 N	32 17.2 W	GPS	3573					
06MT30/2 A2	469	02	ROS	102994	1005	BO	45 41.7 N	32 16.7 W	GPS	3573		3611	18	28	1-4,6,7,8,27,28
06MT30/2 A2	469	02	ROS	102994	1150	EN	45 41.6 N	32 16.5 W	GPS	3573					
06MT30/2 A2	470	01	ROS	102994	1627	BE	46 31.6 N	32 45.5 W	GPS	3811					
06MT30/2 A2	470	01	ROS	102994	1659	BO	45 31.5 N	32 45.2 W	GPS	3811		1199		14	1-4,6,7,8,27,28
06MT30/2 A2	470	01	ROS	102994	1759	EN	45 31.3 N	32 44.7 W	GPS	3811					
06MT30/2 A2	470	02	ROS	103094	0822	BE	45 31.4 N	32 44.8 W	GPS	3770					
06MT30/2 A2	470	02	ROS	103094	0931	BO	45 31.5 N	32 44.5 W	GPS	3770		3827	19	28	1-4,6,7,8,27,28
06MT30/2 A2	470	02	ROS	103094	1108	EN	45 32.0 N	32 44.1 W	GPS	3770					
06MT30/2 A2	471	01	ROS	103094	1607	BE	45 19.5 N	33 18.2 W	GPS	3484					
06MT30/2 A2	471	01	ROS	103094	1635	BO	45 19.8 N	33 18.2 W	GPS	3484		1099		14	1-4,6,7,8,27,28
06MT30/2 A2	471	01	ROS	103094	1730	EN	45 19.9 N	33 18.3 W	GPS	3484					
06MT30/2 A2	471	02	LVS	103094	1918	BO	45 20.0 N	33 18.5 W	GPS	3512		3459		10	1,12,13
06MT30/2 A2	471	03	ROS	103094	2144	BE	45 20.1 N	33 18.4 W	GPS	3543					
06MT30/2 A2	471	03	ROS	103094	2252	BO	45 20.5 N	33 18.3 W	GPS	3543		3569	21	28	1-4,6,7,8,27,28
06MT30/2 A2	471	03	ROS	103194	0038	EN	45 21.4 N	33 18.4 W	GPS	3543					
06MT30/2 A2	472	01	ROS	103194	0259	BE	45 12.6 N	33 45.8 W	GPS	3674					
06MT30/2 A2	472	01	ROS	103194	0328	BO	45 12.5 N	33 45.6 W	GPS	3674		1228		14	1-4,6
06MT30/2 A2	472	01	ROS	103194	0425	EN	45 12.6 N	33 45.4 W	GPS	3674					
06MT30/2 A2	472	02	ROS	103194	0435	BE	45 12.5 N	33 45.3 W	GPS	3666					
06MT30/2 A2	472	02	ROS	103194	0548	BO	45 12.6 N	33 45.8 W	GPS	3666		3714		28	1-4,6,7,8,27,28
06MT30/2 A2	472	02	ROS	103194	0743	EN	45 12.4 N	33 45.5 W	GPS	3666					
06MT30/2 A2	473	01	ROS	103194	1104	BE	45 01.4 N	34 25.7 W	GPS	3973					
06MT30/2 A2	473	01	ROS	103194	1138	BO	45 01.2 N	34 25.4 W	GPS	3973		1075		14	1-4,6,7,8,27,28
06MT30/2 A2	473	01	ROS	103194	1227	EN	45 00.9 N	34 24.9 W	GPS	3973					
06MT30/2 A2	473	02	ROS	103194	1532	BE	45 01.6 N	34 25.7 W	GPS	3976					
06MT30/2 A2	473	02	ROS	103194	1645	BO	45 01.5 N	34 25.8 W	GPS	3976		4030	17	28	1-4,6,7,8,27,28
06MT30/2 A2	473	02	ROS	103194	1824	EN	45 01.2 N	34 25.7 W	GPS	3976					
06MT30/2 A2	474	01	LVS	103194	2359	BO	44 50.4 N	35 04.1 W	GPS	4118		1600		10	1,12,13
06MT30/2 A2	474	02	ROS	110194	0201	BE	44 50.5 N	35 04.8 W	GPS	4103					
06MT30/2 A2	474	02	ROS	110194	0322	BO	44 50.3 N	35 04.8 W	GPS	4103		4165	16	28	1-4,6,7,8,27,28
06MT30/2 A2	474	02	ROS	110194	0510	EN	44 50.4 N	35 04.9 W	GPS	4103					
06MT30/2 A2	474	03	LVS	110194	0706	BO	44 49.7 N	35 04.5 W	GPS	4096		4036		10	1,12,13
06MT30/2 A2	474	04	ROS	110194	0946	BE	44 50.2 N	35 04.2 W	GPS	4096					
06MT30/2 A2	474	04	ROS	110194	1017	BO	44 49.9 N	35 04.4 W	GPS	4096		1398		15	1-4,6,7,8,27,28
06MT30/2 A2	474	04	ROS	110194	1118	EN	44 49.5 N	35 04.6 W	GPS	4096					
06MT30/2 A2	475	01	ROS	110294	1304	BE	44 34.1 N	36 05.3 W	GPS	4094					
06MT30/2 A2	475	01	ROS	110294	1432	BO	44 34.5 N	36 05.6 W	GPS	4094		4160	10	28	1-4,6,7,8,27,28
06MT30/2 A2	475	01	ROS	110294	1613	EN	44 34.9 N	36 06.0 W	GPS	4094					
06MT30/2 A2	476	01	ROS	110294	2100	BE	44 16.8 N	37 02.3 W	GPS	4054					
06MT30/2 A2	476	01	ROS	110294	2213	BO	44 16.9 N	37 02.6 W	GPS	4054		3300		28	1-4,6,7,8,27,28
06MT30/2 A2	476	01	ROS	110294	2334	EN	44 16.8 N	37 02.5 W	GPS	4054					
06MT30/2 A2	476	02	ROS	110294	2353	BE	44 16.7 N	37 02.4 W	GPS	4060					
06MT30/2 A2	476	02	ROS	110394	0034	BO	44 16.8 N	37 02.5 W	GPS	4060		1298		16	1-4,6
06MT30/2 A2	476	02	ROS	110394	0133	EN	44 16.8 N	37 02.5 W	GPS	4060					
06MT30/2 A2	476	03	ROS	110394	0149	BE	44 16.8 N	37 02.5 W	GPS	4054					
06MT30/2 A2	476	03	ROS	110394	0308	BO	44 16.9 N	37 02.6 W	GPS	4054		4105	12	28	1-4,6,7,8,27,28
06MT30/2 A2	476	03	ROS	110394	0452	EN	44 16.6 N	37 02.3 W	GPS	4054					
06MT30/2 A2	477	01	ROS	110394	0926	BE	43 59.7 N	37 59.9 W	GPS	4306					
06MT30/2 A2	477	01	ROS	110394	1046	BO	43 59.7 N	37 59.8 W	GPS	4306		4383	19	28	1-4,6,7,8,27,28
06MT30/2 A2	477	01	ROS	110394	1240	EN	43 59.7 N	38 00.0 W	GPS	4306					
06MT30/2 A2	478	01	ROS	110394	1537	BE	43 49.5 N	38 39.0 W	GPS	3233					
06MT30/2 A2	478	01	ROS	110394	1636	BO	43 49.4 N	38 38.9 W	GPS	3233		3394	16	28	1-4,6,7,8,27,28
06MT30/2 A2	478	01	ROS	110394	1807	EN	43 49.4 N	38 38.7 W	GPS	3233					
06MT30/2 A2	479	01	ROS	110394	2114	BE	43 38.4 N	39 18.0 W	GPS	4542					
06MT30/2 A2	479	01	ROS	110394	2142	BO	43 38.3 N	39 17.5 W	GPS	4542		1501		14	1-4,6,7,8,27,28
06MT30/2 A2	479	01	ROS	110394	2246	EN	43 38.4 N	39 16.4 W	GPS	4542					
06MT30/2 A2	479	02	LVS	110494	0108	BO	43 38.6 N	39 17.9 W	GPS	4558		4521		10	1,12,13
06MT30/2 A2	479	03	ROS	110494	0407	BE	43 38.7 N	39 17.7 W	GPS	4529					
06MT30/2 A2	479	03	ROS	110494	0544	BO	43 38.2 N	39 16.9 W	GPS	4529		4598	18	28	1-4,6,7,8,27,28
06MT30/2 A2	479	03	ROS	110494	0741	EN	43 38.0 N	39 15.9 W	GPS	4529					
06MT30/2 A2	480	01	ROS	110494	1738	BE	43 25.3 N	39 58.1 W	GPS	4808					
06MT30/2 A2	480	01	ROS	110494	1930	BO	43 25.0 N	39 58.8 W	GPS	4808		4900	20	28	1-4,6,7,8,27,28
06MT30/2 A2	480	01	ROS	110494	2156	EN	43 24.7 N	39 59.9 W	GPS	4808					
06MT30/2 A2	481	01	ROS	110594	1125	BE	43 11.1 N	40 47.7 W	GPS	4766					
06MT30/2 A2	481	01	ROS	110594	1339	BO	43 11.6 N	40 48.3 W	GPS	4766		4854	12	28	1-4,6,7,8,27,28
06MT30/2 A2	481	01	ROS	110594	1547	EN	43 12.7 N	40 48.7 W	GPS	4766					
06MT30/2 A2	482	01	ROS	110594	1958	BE	42 57.1 N	41 35.2 W	GPS	4815					
06MT30/2 A2	482	01	ROS	110594	2148	BO	42 57.5 N	41 35.7 W	GPS	4815		4900	25	28	1-4,6,7,8,27,28
06MT30/2 A2	482	01	ROS	110594	2358	EN	42 58.0 N	41 36.4 W	GPS	4815					
06MT30/2 A2	483	01	LVS	110694	0529	BO	42 42.7 N	42 23.2 W	GPS	4793		2000		10	1,12,13
06MT30/2 A2	483	02	ROS	110694	0818	BE	42 42.9 N	42 25.8 W	GPS	4851					
06MT30/2 A2	483	02	ROS	110694	1015	BO	42 42.4 N	42 22.5 W	GPS	4851		4925	19	28	1-4,6,7,8,27,28
06MT30/2 A2	483	02	ROS	110694	1228	EN	42 41.7 N	42 19.3 W	GPS	4851					
06MT30/2 A2	483	03	LVS	110694	1420	BO	42 41.3 N	42 25.7 W	GPS	4844		4784		10	1,12,13
06MT30/2 A2	483	04	ROS	110694	1844	BE	42 43.0 N	42 26.5 W	GPS	4713					
06MT30/2 A2	483	04	ROS	110694	1917	BO	42 42.9 N	42 25.4 W	GPS	4713		1499		19	1-4,6,7,8,27,28
06MT30/2 A2	483	04	ROS	110694	2015	EN	42 42.6 N	42 23.7 W	GPS	4713					
06MT30/2 A2	484	01	ROS	110794	0307	BE	42 28.3 N	43 16.1 W	GPS	4853					
06MT30/2 A2	484	01	ROS	110794	0444	BO	42 27.9 N	43 12.9 W	GPS	4853		4959	15	28	1-4,6,7,8,27,28
06MT30/2 A2	484	01	ROS	110794	0710	EN	42 26.8 N	43 08.2 W	GPS	4853					
06MT30/2 A2	485	01	ROS	110794	1234	BE	42 13.1 N	44 08.7 W	GPS	4867					
06MT30/2 A2	485	01	ROS	110794	1437	BO	42 13.5 N	44 07.9 W	GPS	4867		4985	12	28	1-4,6,7,8,27,28
06MT30/2 A2	485	01	ROS	110794	1647	EN	42 13.9 N	44 07.3 W	GPS	4867					
06MT30/2 A2	486	01	ROS	110794	2028	BE	41 59.6 N	45 00.0 W	GPS	4807					
06MT30/2 A2	486	01	ROS	110794	2232	BO	42 00.5 N	45 02.2 W	GPS	4807		4908	18	28	1-4,6,7,8,27,28
06MT30/2 A2	486	01	ROS	110894	0050	EN	42 01.2 N	45 01.0 W	GPS	4807					
06MT30/2 A2	486	02	ROS	110894	0131	BE	41 59.7 N	45 00.4 W	GPS	4807					
06MT30/2 A2	486	02	ROS	110894	0228	BO	42 00.4 N	44 59.8 W	GPS	4807		1489		16	1-4,6,7,8,27,28
06MT30/2 A2	486	02	ROS	110894	0324	EN	42 01.2 N	44 59.1 W	GPS	4807					
06MT30/2 A2	487	01	ROS	110994	1711	BE	43 05.1 N	48 26.8 W	GPS	2837					
06MT30/2 A2	487	01	ROS	110994	1835	BO	43 04.2 N	48 26.4 W	GPS	2837		2854	16	28	1-4,6,7,8,27,28
06MT30/2 A2	487	01	ROS	110994	2006	EN	43 03.2 N	48 26.9 W	GPS	2837					
06MT30/2 A2	488	01	ROS	110994	2224	BE	43 08.9 N	48 44.0 W	GPS	2139					
06MT30/2 A2	488	01	ROS	110994	2342	BO	43 08.1 N	48 44.4 W	GPS	2139		2155	17	28	1-4,6,7,8,27,28
06MT30/2 A2	488	01	ROS	111094	0059	EN	43 07.6 N	48 45.0 W	GPS	2139					


7.1.2.1	SUMMARY OF SUB-SAMPLING SCHEMES, HYDROGRAPHIC STATIONS ON M30/2 

	A	B	C	D	E	F	G	H	I	J	K	L	M	N	O	P	Q	R	S	T	U	V
122																						
1    Stat cast	Salz	Salz	O2	Nähr	CFCs	CCL4	3He	3He	Seeg	3H	tCO2	Alk	13C	14C	14C	139J	ChIphy	BIO	BIO-Nr	CTD	Kommentar
2		BSH		Hel	UB	3He		18O	LVS	AMS		ID
3	436/1	36	24	24	24	28						3	3	3			0	3	1	24	DHI1	Kalibrierst CFC
4	436/2LVS																0				x	
5	436/3		24	24													0		25	48	DHI1	Kalibrierst
6	436/4			22													0		49	72	DHI2	Kalibrierst
7	437	11	7	7	7												0		73	78, 96	NB3	begin WOCE A2
8	438	11	9	10	10	7	7					8	8	8			0	8	79	88	NB3	
9	439/1																0				NB3, 	Cast aborted
																					software	
10	439/2	11	11	11	11												0		90	100	NB3	
11	440	11	17	17	17	14	14	8		8	8	16	16	16			0	8	101	117	NB3	
12	441	17	21	21	21	7	7	10			10						0		118	138	NB3	
13	442	17	24	24	24	7	7										0		140	163	NB3	
14	443	29	24	24	24	14	14	14			14					6	0		164	187	NB3	
15	444	29	24	24	24												0		188	211	NB3	
16	445/1LVT		10	10	10										10		0				x	
17	445/2	44	22	22	22	22	22	12		22	12	18	18	18			6		212	234	NB3	
18	445/3LVT		10	10	10										10		0				x	
19	445/4	44	17	17	17	7	7	8		10	8	17	17	17			4	7	235	253		
20	446/1	53	15	15	15												0		254	269	DHI1	
21	446/2																0				software	abort
22	446/3	53	23	23	23												0		270	292	NB3	
23	447	51	20	20	20	18	18		5			20	20	20			5	2	293	312	NB3	
24	448	51	20	20	20	14	14	14	12		14	20	20		6	7	5		316	335	NB3	BIO 375,383
25	449/1	34	22	22	22	17	17	11			11	18	18	18	6	6	6	5	339	351	DHI1	
26	449/2	34	22	22	22	16	16					12	12	13			0		352	374	NB3	
27	450/1LVF		10	10	10			7			7				10		0				x	
28	450/2	42	20	20	20	20	20	9		8	9	13	13	13			0		384	403	NB3	
29	450/3LVT		10	10	10										10		0				x	
30	450/4	42	15	15	15	17	17	7		7	7	9	9	9			0	5	407	423	DHI1	
31	451/1	33	15	15	15	11	11		9								0	5	424	439	DHI1	
32	451/2	33	21	21	21	17	17		13								0		440	460	NB3	
33	452/1	39	18	18	18	12	12	9		9	9	15	15	15			0		463	480	DHl1	
34	452/2	39	18	16	16	14	14	13		7	13	10	10	10			0	3	487	504	NB3	Kalibrierst
35	453/1		24	24	24	28				16							0		509	532	NB3	Kalibrierst CFC
36	453/2LVF		10	10	10										10		0				x	
37	453/3	24	21	21	21	16	16	12		8	12	17	17				0		533	556	DHI1	
38	453/4	24	21	21	21	12	12	5			5	9	9				0	5	557	580	DHI1	
39	454/1	50	18	18	18												0		582	599	NB3	
40	454/2	50	21	21	21												7		601	624	DHI1	
41	455/1	38	191	19	19	18	18	9			9	14	14 	14 			0	5	626	644	NB3	
42	455/2LVT		10	10	10										10		5				x	
43	455/3	38	23	23	23	21	21	8		8	8	14	14 	14 			0	1	646	669	DHI1	
44	456/1	35	20	20	20												0		671	690	NB3	
45	456/2	35	24	23	23			11	10		11						0		691	714	DHI1	LDEO, UB, HD 
																						Intercal
46	457/1	8	10	10	10	8	8										0		715	724	NB3	
47	457/2	8	24	24	24	13	13	7		8	7						0		727	750	DHI1	
48	458/1	8	12	12	12	8	8	8		8	8	8	8		4		0	3	751	762	NB3	
49	458/2LVT		10	10	10										10		0				x	
50	458/3	55	22	22	22	19	19	11		8	11	13	13		2	6	0		765	787	DHI1	
51	459	55	24	22	24	7	7	9			9						11		789	812	DHI1	
52	460	45	24	22	21	16	16	7			7						0		813	836	DHI1	
53	461	45	21	21	21					8							0		837	860	DHI1	
54	462	49	22	22	22	17	17	12			12	22	22			6	0	4	861	883	DHI1	
55	463	49	23	22	22	7	7		6	8							0		885	908	DHI1	
56	464	60	22	22	22	22	22	8		16	8	23	23	23			0	3	909	932	DHI1	
57	465	60	23	23	23	14	14	12			12	23	23				0	3	933	955	DHI1	
58	466	152	21	21	21	20	20		8								0		956	978	DHI1	
59	467	152	22	22	22	14	14	7		16	7						0		979	1002	DHI1	
60	468/1	43	22	22	22	13	13	8			8	14	14	14		5	0	4	1003	1024	NB3	
61	468/2LVT		10	10	10										10		0				x	
62	468/3	43	21	21	21	20	20	9			9	16	16	16		1	7		1027	1050	DHI1	
63	469/1	30	12	12	12	12	12												1051	1064	NB3	
64	469/2	30	22	22	221	16	16		8										1065	1087	DHI1	
65	470/1	186	14	14	14	10	10	4		16	4	14 	14					5	1089	1102	NB3	
66	470/2	186	22	22	22	18	18	8		16	8	23	23						1103	1126	DHI1	
67	471/1	195	14	14	14	10	10	8			8					4			1127	1140	NB3	
68	471/2LVT		10	10	10					16					10						x	Repro
69	471/3	195	23	23	23	24	24	10			10					2			1141	1164	DHI1	
70	472/1	194	12	12	12							12	12	12				3	1165	1178	NB3	
71	472/2	194	23	23	23	4	4					16	16	16					1179	1202	DHI1	
72	473/1	196	14	14	14	10	10	5			5								1203	1216	NB3	
73	473/2	196	23	23	23	21	21	13			13								1217	1240	DHI1	
74	474/1LVF		10	10	10										10						x	
75	474/2	1	23	23	23	18	18	9			9	16	16						1255	1278	DHI1	
76	474/3LVT		10	10	10										10						x	BIO+1279
77	474/4	1	15	15	15	10	10	7			7	14	14					6	1241	1254	NB3	
78	475/1	52	23	23	23	21	21					23	23	23			12	5	1296	1319	DHI1	
79	476/1	0	23	23	23	28		6	6	32									1320	1343	DHI1	Kal 3200m, 
																						Intercal HD, UB
80	476/2	52	16	16	16			7			7								1280	1295	NB3	
81	476/3	20	23	23	23	14	14	10			10								1344	1367	DHI1	
82	477/1	20	24	24	24	24	24	13			13	23	23					3	1368	1391	DHI1	
83	478	18	22	22	22	7	7												1392	1415	DHI1	
84	479/1	18	13	13	13	10	10	6			6	12	12			5		3	1416	1429	NB3	
85	479/2LVT		10	10	10										10						x	
86	479/3	10	23	23	23	21	21	12			12	14	14			1			1430	1453	DHI1	
87	480	10	23	23	23	23	23					23	23	23				2	1454	1477	DHI1	
88	481	4	24	24	24	24	24	15		24	15	24	24					3	1478	1501	DHI1	
89	482	4	24	24	24	25	25												1502	1525	DHI1	
90	483/1LVF		10	10	10										10						x	
91	483/2	15	24	24	24	25	25	10			10	16	16						1526	1549	DHI1	
92	483/3LVT		10	10	10										10						x	
93	483/4	15	16	16	16	17	17	9			9	14	14					3	1550	1565	DHI1	
94	484	26	23	23	23	24	24												1566	1589	DHI1	
95	485	26	22	22	22	25	25	12		16	12	22	22	22			10	2	1590	1613	DHI1	
96	486/1	56	24	24	24	19	19	12		11	12	15	15			6			1614	1637	DHI1	
97	486/2	56	16	16	16	10	10	8		5	8	16	16			5		5	1614	1653	NB3	
98	487	185	22	22	22	21	21	14			14	22	22	22		5		5	1654	1677	DHI1	
99	488	185	23	23	23	16	16	11			11	23	23					4	1678	1700	DHI1	End of section
100																						
101																						
102																						
103	Total	4266	1722	1737	1692	1062	978	474	77	311	468	694	694	359	158	65	78	123				WOCE-A2


7.1.2.2  SUMMARY OF DAILY STATION ACTIVITIES M30/2

15. Okt	16. Okt	17. Okt	18. Okt	19. Okt	19. Okt	21. Okt	22. Okt	23. Okt	24. Okt
436/1	437	444	446	Sturm	449/1	450/2	Sturm	452/1	454/1
DHI1	NB3	NB3	NB3	W9-11	DHI1	NB3	WNW 9	DHI1	NB3
									
436/3	438	445	447		449/2	450/4		452/2	454/2
NB3	NB3	DHI1	NB3		NB3	DHI1		NB3	DHI1
									
436/4	439		448			451/1		453/1	455/1
DHI2	NB3		DHI1			DHI1		NB3	NB3
									
	440					451/2		453/3	455/3
	NB3					NB3		DHI1	DHI1
									
	441							453/4	456/1
	NB3					Sturm		DHI1	NB3
									
	442					W10-11			
	NB3								
									
	443								
	NB3								

25. Okt	26. Okt	27. Okt	28. Okt	29. Okt	30. Okt	31. Okt	1. Nov	2. Nov	3. Nov
456/2	459	465	466	469/1	470/2	472/1	474/2	Sturm	477
DHI1	DHI1	DHI1	DHI1	NB3	DHI1	NB3	DHI1		DHI1
									
457/1	460		467	469/2	471/1	472/2	474/4	475	478
NB3	DHI1		DHI1	DHI1	NB3	DHI1	NB3	DHI1	DHI1
									
457/2	461		468/1	470/1	471/3	473/1		476/1	479/1
DHI1	DHI1		NB3	NB3	DHI1	NB3		DHI1	NB3
									
458/1	462		468/3			473/2		476/2	479/2
NB3	DHI1		DHI1			DHI1		NB3	DHI1
									
458/3	463								
DHI1	DHI1								
									
	464						Sturm		
	DHI1						WNW 9		

4. Nov	5. Nov	6. Nov	7. Nov	8. Nov	9. Nov	10. Nov	11. Nov	12. Nov
480	481	483/2	484	486/2	487			
DHI1	DHI1	DHI1	DHI1	NB3	DHI1			
								
Sturm	482/1		485		488			
NW 10	DHI1		DHI1		DHI1			
								
		483/4	486/1					
		DHI1	DHI1					
								
				Sturm				
				NNW9				
								
								
								
								
Sturm								
NW9								


7.1.3  STATION LIST LEG M30/3 SECTION A1W

EXPO-	 WOCE	STAT.	CAST	CAST	DATE	TIME	CODE	POSITION			CODE	BOTTOM	METER	MAX	BOTTOM	NO.OF	PARAMETERS/COMMENTS
CODE	 WHP-ID	NO.	NO.	TYPE		UTC		LATITUDE	LONGITUDE		DEPTH	WHEEL	PRES	DIST.	BTLS	
06MT30/3 A1/W	489	1	ROS	111694	1619	BE	51 35.5 N	53 32.7 W	GPS	447					
06MT30/3 A1/W	489	1	ROS	111694	1642	BO	51 35.3 N	53 32.8 W	GPS	447	421	420	20	23	1-6, 10/Test "DHI1" CTD+ROS
06MT30/3 A1/W	489	1	ROS	111694	1714	EN	51 35.2 N	53 33.0 W	GPS	447					
06MT30/3 A1/W	489	2	ROS	111694	1737	BE	51 35.1 N	53 33.2 W	GPS	447					
06MT30/3 A1/W	489	2	ROS	111694	1802	BO	51 35.1 N	53 33.4 W	GPS	448	420	414		23	1-8, 10/Test "NB3" CTD+ROS
06MT30/3 A1/W	489	2	ROS	111694	1840	EN	51 35.2 N	53 33.5 W	GPS	447					
06MT30/3 A1/W	490	1	ROS	111894	0903	BE	54 45.4 N	54 29.3 W	GPS	250					
06MT30/3 A1/W	490	1	ROS	111894	0913	BO	54 45.2 N	54 29.4 W	GPS	250	227	221	20	5	1-8, 23
06MT30/3 A1/W	490	1	ROS	111894	0927	EN	54 45.0 N	54 29.5 W	GPS	250					
06MT30/3 A1/W	491	1	ROS	111894	1115	BE	54 57.3 N	54 17.2 W	GPS	380					
06MT30/3 A1/W	491	1	ROS	111894	1129	BO	54 57.3 N	54 17.1 W	GPS	380	351	351	14	6	1-6, 9, 10, 23
06MT30/3 A1/W	491	1	ROS	111894	1152	EN	54 57.2 N	54 16.8 W	GPS	379					
06MT30/3 A1/W	492	1	ROS	111894	1331	BE	55 06.6 N	54 08.3 W	GPS	959					
06MT30/3 A1/W	492	1	ROS	111894	1355	BO	55 06.5 N	54 07.9 W	GPS	943	907	911	16	13	1-10, 23 
06MT30/3 A1/W	492	1	ROS	111894	1432	EN	55 06.3 N	54 07.7 W	GPS	930					
06MT30/3 A1/W	493	1	LVS	111894	1809	MR	55 15.9 N	53 57.6 W	GPS	2118	2041		40	10	1, 12, 13
06MT30/3 A1/W	493	2	ROS	111894	1949	BE	55 14.9 N	53 56.8 W	GPS	2063					
06MT30/3 A1/W	493	2	ROS	111894	2043	BO	55 14.4 N	53 56.7 W	GPS	2030	2017	2025	21	23	1-10, 23
06MT30/3 A1/W	493	2	ROS	111894	2148	EN	55 13.5 N	53 56.5 W	GPS	2037					
06MT30/3 A1/W	494	1	ROS	111994	0035	BE	55 25.2 N	53 49.6 W	GPS	2685					
06MT30/3 A1/W	494	1	ROS	111994	0132	BO	55 24.8 N	53 49.6 W	GPS	2686	2676	2701	16	24	1-10, 23
06MT30/3 A1/W	494	1	ROS	111994	0303	EN	55 24.2 N	53 49.6 W	GPS	2673					
06MT30/3 A1/W	495	1	LVS	111994	0545	MR	55 36.6 N	53 38.0 W	GPS	2930	2854		40	10	1, 12, 13
06MT30/3 A1/W	495	2	ROS	111994	0744	BE	55 36.7 N	53 37.2 W	GPS	2938					
06MT30/3 A1/W	495	2	ROS	111994	0848	BO	55 36.9 N	53 36.5 W	GPS	2940	2915	2936	18	23	1-10, 12, 23
06MT30/3 A1/W	495	2	ROS	111994	1011	EN	55 37.1 N	53 35.3 W	GPS	2933					
06MT30/3 A1/W	496	1	ROS	111994	1254	BE	55 50.8 N	53 23.3 W	GPS	3148					
06MT30/3 A1/W	496	1	ROS	111994	1356	BO	55 50.6 N	53 22.6 W	GPS	3144	3107	3140	9	24	1-10, 23/ROS quality test #1 
06MT30/3 A1/W	496	1	ROS	111994	1515	EN	55 50.3 N	53 21.5 W	GPS	3143					
06MT30/3 A1/W	497	1	ROS	112094	2352	BE	59 44.9 N	49 09.5 W	GPS	3246					
06MT30/3 A1/W	497	1	ROS	112194	0101	BO	59 44.8 N	49 10.5 W	GPS	3242	3209	3227	40	24	1-10, 23
06MT30/3 A1/W	497	1	ROS	112194	0236	EN	59 44.8 N	49 11.5 W	GPS	3246					
06MT30/3 A1/W	498	1	ROS	112294	0943	BE	59 03.7 N	49 56.9 W	GPS	3489					
06MT30/3 A1/W	498	1	ROS	112294	1111	BO	59 03.2 N	49 58.2 W	GPS	3492	3473	3506	20	24	1-10, 12, 23
06MT30/3 A1/W	498	1	ROS	112294	1257	EN	59 02.7 N	49 59.7 W	GPS	3497					
06MT30/3 A1/W	498	2	LVS	112294	1430	MR	59 02.6 N	49 59.7 W	GPS	3496	3419		40	10	1, 12, 13
06MT30/3 A1/W	499	1	ROS	112294	1923	BE	59 28.1 N	49 28.1 W	GPS	3416					
06MT30/3 A1/W	499	1	ROS	112294	2034	BO	59 29.0 N	49 27.2 W	GPS	3414	3402	3423	20	23	1-10, 23
06MT30/3 A1/W	499	1	ROS	112294	2204	EN	59 29.4 N	49 26.5 W	GPS	3415					
06MT30/3 A1/W	500	1	ROS	112394	0145	BE	59 59.1 N	48 54.0 W	GPS	3039					
06MT30/3 A1/W	500	1	ROS	112394	0248	BO	59 59.5 N	48 53.8 W	GPS	3035	3014	3031	30	23	1-10, 12, 23
06MT30/3 A1/W	500	1	ROS	112394	0418	EN	59 59.5 N	48 54.2 W	GPS	3043					
06MT30/3 A1/W	501	1	ROS	112394	0914	BE	60 10.6 N	48 41.0 W	GPS	2880					
06MT30/3 A1/W	501	1	ROS	112394	1023	BO	60 11.0 N	48 41.3 W	GPS	2886	2855	2899	17	24	1-10, 23
06MT30/3 A1/W	501	1	ROS	112394	1153	EN	60 11.9 N	48 42.1 W	GPS	2896					
06MT30/3 A1/W	502	1	ROS	112394	1352	BE	60 17.5 N	48 32.9 W	GPS	2767					
06MT30/3 A1/W	502	1	ROS	112394	1453	BO	60 18.0 N	48 34.2 W	GPS	2765	2742	2772	10	24	1-10, 12, 23
06MT30/3 A1/W	502	1	ROS	112394	1614	EN	60 18.4 N	48 35.6 W	GPS	2766					
06MT30/3 A1/W	503	1	LVS	112394	1709	MR	60 20.9 N	48 30.1 W	GPS	1574	1257		40	10	1, 12, 13
06MT30/3 A1/W	503	2	ROS	112394	1935	BE	60 20.8 N	48 31.3 W	GPS	1734					
06MT30/3 A1/W	503	2	ROS	112394	2030	BO	60 21.1 N	48 31.9 W	GPS	1666	1676	1692	29	17	1-10, 23
06MT30/3 A1/W	503	2	ROS	112394	1935	BE	60 20.8 N	48 31.3 W	GPS	1734					
06MT30/3 A1/W	504	1	ROS	112394	2313	BE	60 24.2 N	48 24.8 W	GPS	578					
06MT30/3 A1/W	504	1	ROS	112394	2335	BO	60 24.4 N	48 25.3 W	GPS	489	467	467	14	10	1-10, 23
06MT30/3 A1/W	504	1	ROS	112494	0006	EN	60 24.7 N	48 25.7 W	GPS	401					
06MT30/3 A1/W	505	1	ROS	112494	0214	BE	60 33.9 N	48 13.6 W	GPS	145					
06MT30/3 A1/W	505	1	ROS	112494	0227	BO	60 33.8 N	48 13.5 W	GPS	139	111	114	25	5	1-6, 9, 10, 12, 23
06MT30/3 A1/W	505	1	ROS	112494	0239	EN	60 33.9 N	48 13.4 W	GPS	130					


7.1.3.1  STATION LIST LEG M30/3 SECTION A1E

EXPO-	 WOCE	STAT.	CAST	CAST	DATE	TIME	CODE	POSITION			CODE	BOTTOM	METER	MAX	BOTTOM	NO.OF	PARAMETERS/COMMENTS
CODE	 WHP-ID	NO.	NO.	TYPE		UTC		LATITUDE	LONGITUDE		DEPTH	WHEEL	PRES	DIST.	BTLS	
06MT30/3 A1/E	506	1	ROS	112594	0004	BE	60 00.0 N	42 30.1 W	GPS	193					
06MT30/3 A1/E	506	1	ROS	112594	0019	BO	59 59.6 N	42 30.3 W	GPS	193	177	178	9	5	1-10, 23
06MT30/3 A1/E	506	1	ROS	112594	0029	EN	59 49.5 N	42 30.5 W	GPS	192					
06MT30/3 A1/E	507	1	ROS	112594	0227	BE	59 57.6 N	42 10.1 W	GPS	507					
06MT30/3 A1/E	507	1	ROS	112594	0245	BO	59 57.4 N	42 10.0 W	GPS	500	474	474	17	8	1-10, 23
06MT30/3 A1/E	507	1	ROS	112594	0302	EN	59 57.3 N	42 10.0 W	GPS	499					
06MT30/3 A1/E	508	1	ROS	112594	0424	BE	59 55.9 N	41 51.5 W	GPS	1827					
06MT30/3 A1/E	508	1	ROS	112594	0505	BO	59 55.2 N	41 51.6 W	GPS	1824	1789	1802	21	18	1-10, 23
06MT30/3 A1/E	508	1	ROS	112594	0558	EN	59 54.5 N	41 52.1 W	GPS	1822					
06MT30/3 A1/E	509	1	ROS	112594	0823	BE	59 53.0 N	41 30.3 W	GPS	1897					
06MT30/3 A1/E	509	1	ROS	112594	0928	BO	59 52.5 N	41 29.8 W	GPS	1899	1852	1876	18	20	1-10, 23
06MT30/3 A1/E	509	1	ROS	112594	1045	EN	59 51.6 N	41 29.2 W	GPS	1917					
06MT30/3 A1/E	510	1	ROS	112594	1304	BE	59 52.1 N	41 12.8 W	GPS	2031					
06MT30/3 A1/E	510	1	ROS	112594	1411	BO	59 52.0 N	41 13.4 W	GPS	2027	1992	2008	17	24	1-10, 23
06MT30/3 A1/E	510	1	ROS	112594	1513	EN	59 51.8 N	41 13.8 W	GPS	2025					
06MT30/3 A1/E	511	1	ROS	112594	1746	BE	59 50.2 N	40 52.3 W	GPS	2339					
06MT30/3 A1/E	511	1	ROS	112594	1858	BO	59 50.9 N	40 53.5 W	GPS	2327	2394	2315	18	19	1-10 / Data flow interrupts
06MT30/3 A1/E	511	1	ROS	112594	2019	EN	59 51.5 N	40 55.5 W	GPS	2282					during uptrace
06MT30/3 A1/E	512	1	ROS	112894	0124	BE	59 45.1 N	40 02.9 W	GPS	2702					
06MT30/3 A1/E	512	1	ROS	112894	0229	BO	59 44.5 N	40 03.7 W	GPS	2710	2701	2690	20	24	1-10, 23 
06MT30/3 A1/E	512	1	ROS	112894	0338	EN	59 44.1 N	40 04.4 W	GPS	2711					
06MT30/3 A1/E	513	1	ROS	112894	0724	BE	59 38.8 N	38 55.4 W	GPS	2953					
06MT30/3 A1/E	513	1	ROS	112894	0833	BO	59 38.8 N	38 54.8 W	GPS	2955	2919	2936	19	24	1-10, 23
06MT30/3 A1/E	513	1	ROS	112894	1021	BE	59 39.1 N	38 53.2 W	GPS	2958					
06MT30/3 A1/E	514	1	LVS	112894	1554	MR	59 31.2 N	37 38.4 W	GPS	3133	3051		40	10	1, 12, 13
06MT30/3 A1/E	514	2	ROS	112894	1744	BE	59 31.1 N	37 38.3 W	GPS	3132					
06MT30/3 A1/E	514	2	ROS	112894	1850	BO	59 31.4 N	37 38.6 W	GPS	3130	3099	3134	18	24	1-10, 12, 23
06MT30/3 A1/E	514	2	ROS	112894	2024	EN	59 32.1 N	37 39.5 W	GPS	3132					
06MT30/3 A1/E	515	1	ROS	112994	0109	BE	59 23.2 N	36 20.7 W	GPS	3120					
06MT30/3 A1/E	515	1	ROS	112994	0216	BO	59 23.5 N	36 22.0 W	GPS	3124	3101	3121	19	23	1-10, 23
06MT30/3 A1/E	515	1	ROS	112994	0342	EN	59 23.6 N	36 22.5 W	GPS	3122					
06MT30/3 A1/E	516	1	ROS	112994	0758	BE	59 15.6 N	35 03.9 W	GPS	3057					
06MT30/3 A1/E	516	1	ROS	112994	0908	BO	59 15.4 N	35 04.9 W	GPS	3049	3005	3038	20	22	1-10, 23
06MT30/3 A1/E	516	1	ROS	112994	1023	EN	59 15.1 N	35 06.1 W	GPS	3083					
06MT30/3 A1/E	517	1	ROS	112994	1500	BE	59 07.9 N	33 47.2 W	GPS	2286					
06MT30/3 A1/E	517	1	ROS	112994	1546	BO	59 07.9 N	33 47.3 W	GPS	2325	2249	2270	20	21	1-10, 23 / ROS Test # 2
06MT30/3 A1/E	517	1	ROS	112994	1649	BE	59 07.7 N	33 46.7 W	GPS	2313					
06MT30/3 A1/E	518	1	ROS	112994	1919	BE	59 03.2 N	33 02.2 W	GPS	2452					
06MT30/3 A1/E	518	1	ROS	112994	2041	BO	59 02.0 N	33 02.0 W	GPS	2449		2441	15	24	1-10, 23
06MT30/3 A1/E	518	1	ROS	112994	2150	EN	59 02.5 N	33 01.9 W	GPS	2435					
06MT30/3 A1/E	519	1	ROS	113094	0039	BE	58 58.3 N	32 17.8 W	GPS	1623					
06MT30/3 A1/E	519	1	ROS	113094	0130	BO	58 58.3 N	32 18.1 W	GPS	1760	1760	1757	20	19	1-10, 23
06MT30/3 A1/E	519	1	ROS	113094	0227	EN	58 58.4 N	32 18.8 W	GPS	1921					
06MT30/3 A1/E	520	1	ROS	113094	0503	BE	58 52.8 N	31 33.6 W	GPS	1503					
06MT30/3 A1/E	520	1	ROS	113094	0536	BO	58 52.8 N	31 33.8 W	GPS	1505	1478	1492	18	15	1-10, 23
06MT30/3 A1/E	520	1	ROS	113094	0625	EN	58 52.8 N	31 34.4 W	GPS	1511					
06MT30/3 A1/E	521	1	ROS	113094	0906	BE	58 48.0 N	30 49.2 W	GPS	1189					
06MT30/3 A1/E	521	1	ROS	113094	0942	BO	58 47.7 N	30 48.4 W	GPS	1250	1234	1233	20	15	1-10, 23
06MT30/3 A1/E	521	1	ROS	113094	1027	EN	58 47.6 N	30 47.8 W	GPS	1211					
06MT30/3 A1/E	522	1	ROS	113094	1305	BE	58 31.0 N	30 16.5 W	GPS	1748					
06MT30/3 A1/E	522	1	ROS	113094	1359	BO	58 30.5 N	30 16.4 W	GPS	1636	1670	1689	13	20	1-10, 23
06MT30/3 A1/E	522	1	ROS	113094	1457	EN	58 30.5 N	30 16.9 W	GPS	1886					
06MT30/3 A1/E	523	1	ROS	113094	1755	BE	58 14.1 N	29 44.1 W	GPS	2296					
06MT30/3 A1/E	523	1	ROS	113094	1852	BO	58 14.4 N	29 43.6 W	GPS	2286	2255	2276	18	24	1-10, 23
06MT30/3 A1/E	523	1	ROS	113094	2004	EN	58 15.1 N	29 42.9 W	GPS	2292					
06MT30/3 A1/E	524	1	ROS	113094	2338	BE	57 57.2 N	29 12.0 W	GPS	2232					
06MT30/3 A1/E	524	1	ROS	120194	0029	BO	57 57.7 N	29 11.3 W	GPS	2226	2239	2209	26	23	1-10, 23
06MT30/3 A1/E	524	1	ROS	120194	0145	EN	57 58.1 N	29 10.5 W	GPS	2225					
06MT30/3 A1/E	525	1	ROS	120194	0642	BE	57 40.2 N	28 40.2 W	GPS	2470					
06MT30/3 A1/E	525	1	ROS	120194	0757	BO	57 40.7 N	28 40.0 W	GPS	2470	2439	2455	20	24	1-10, 23
06MT30/3 A1/E	525	1	ROS	120194	0922	EN	57 40.9 N	28 39.5 W	GPS	2471					
06MT30/3 A1/E	526	1	LVS	120194	1044	MR	57 22.9 N	28 07.5 W	GPS	2655	2576		40	10	1, 12, 13
06MT30/3 A1/E	526	2	ROS	120194	1641	BE	57 22.5 N	28 07.2 W	GPS	2662					
06MT30/3 A1/E	526	2	ROS	120194	1732	BO	57 22.4 N	28 08.0 W	GPS	2666	2623	2654	16	24	1-10, 23
06MT30/3 A1/E	526	2	ROS	120194	1850	EN	57 22.2 N	28 07.6 W	GPS	2640					
06MT30/3 A1/E	527	1	ROS	120194	2215	BE	56 54.8 N	27 50.5 W	GPS						
06MT30/3 A1/E	527	1	ROS	120194	2332	BO	56 54.9 N	27 48.2 W	GPS	2933	2933	2867	40	22	1-10, 23/Data flow interrupts
06MT30/3 A1/E	527	1	ROS	120294	0116	EN	56 54.7 N	27 45.3 W	GPS	2888					during uptrace
06MT30/3 A1/E	528	1	MOR	120294	0455	BE	57 23.4 N	28 12.5 W	GPS						Dredging of Mooring "D2" 
06MT30/3 A1/E	528	1	MOR	120294	1500	EN	57 25.7 N	28 17.8 W	GPS						(failed)
06MT30/3 A1/E	529	1	ROS	120394	0003	BE	56 27.3 N	27 29.8 W	GPS	2773					
06MT30/3 A1/E	529	1	ROS	120394	0103	BO	56 27.2 N	27 29.6 W	GPS	2766	2749	2778	17	24	1-10, 23
06MT30/3 A1/E	529	1	ROS	120394	0218	EN	56 27.1 N	27 29.1 W	GPS	2769					
06MT30/3 A1/E	530	1	ROS	120394	0521	BE	55 59.4 N	27 08.8 W	GPS	2817					
06MT30/3 A1/E	530	1	ROS	120394	0624	BO	55 59.0 N	27 09.0 W	GPS	2796	2789	2784	26	22	1-10, 23
06MT30/3 A1/E	530	1	ROS	120394	0750	EN	55 58.4 N	27 11.0 W	GPS	2802					
06MT30/3 A1/E	531	1	ROS	120394	1047	BE	55 31.9 N	26 47.7 W	GPS	3208					
06MT30/3 A1/E	531	1	ROS	120394	1157	BO	55 31.8 N	26 48.1 W	GPS	3198	3185	3202	22	24	1-6, 9, 10, 23
06MT30/3 A1/E	531	1	ROS	120394	1324	EN	55 31.4 N	26 48.5 W	GPS	3209					
06MT30/3 A1/E	532	1	ROS	120394	1626	BE	55 04.2 N	26 27.6 W	GPS	3380					
06MT30/3 A1/E	532	1	ROS	120394	1728	BO	55 04.3 N	26 28.1 W	GPS	3380	3346	3396	18	24	1-10, 23
06MT30/3 A1/E	532	1	ROS	120394	1850	EN	55 04.3 N	26 29.3 W	GPS	3381					
06MT30/3 A1/E	533	1	ROS	120394	2203	BE	54 36.6 N	26 07.4 W	GPS	3427					
06MT30/3 A1/E	533	1	ROS	120394	2319	BO	54 35.9 N	26 07.8 W	GPS	3441	3491	3462	18	24	1-6, 9, 10, 23
06MT30/3 A1/E	533	1	ROS	120494	0049	EN	54 35.1 N	26 08.3 W	GPS	3438					
06MT30/3 A1/E	534	1	ROS	120494	0322	BE	54 17.8 N	25 53.1 W	GPS	3132					
06MT30/3 A1/E	534	1	ROS	120494	0422	BO	54 17.6 N	25 52.5 W	GPS	3088	3053	3092	17	24	1-10, 23
06MT30/3 A1/E	534	1	ROS	120494	0540	EN	54 17.2 N	25 52.1 W	GPS	3061					
06MT30/3 A1/E	535	1	ROS	120494	0802	BE	53 59.1 N	25 38.9 W	GPS	3385					
06MT30/3 A1/E	535	1	ROS	120494	0924	BO	53 58.1 N	25 38.0 W	GPS	3610	3517	3514	20	24	1-10, 23
06MT30/3 A1/E	535	1	ROS	120494	1102	EN	53 57.3 N	25 36.8 W	GPS						
06MT30/3 A1/E	536	1	ROS	120494	1324	BE	53 40.4 N	25 24.8 W	GPS	3591					
06MT30/3 A1/E	536	1	ROS	120494	1437	BO	53 40.2 N	25 24.8 W	GPS	3598	3599	3627	17	22	1-10, 23
06MT30/3 A1/E	536	1	ROS	120494	1614	EN	53 40.0 N	25 24.7 W	GPS	3599					
06MT30/3 A1/E	537	1	ROS	120494	1903	BE	53 27.8 N	24 41.1 W	GPS	3585					
06MT30/3 A1/E	537	1	ROS	120494	2026	BO	53 26.9 N	24 41.2 W	GPS	3564	3598	3590	20	24	1-10, 23
06MT30/3 A1/E	537	1	ROS	120494	2210	EN	53 26.6 N	24 42.0 W	GPS	3533					
06MT30/3 A1/E	538	1	ROS	121294	0853	BE	53 10.2 N	23 31.3 W	GPS	3694					
06MT30/3 A1/E	538	1	ROS	121294	1011	BO	53 10.6 N	23 32.0 W	GPS	3695	3704	3735	17	23	1-10, 23
06MT30/3 A1/E	538	1	ROS	121294	1143	EN	53 10.0 N	23 33.0 W	GPS	3690					
06MT30/3 A1/E	539	1	ROS	121294	1556	BE	52 52.1 N	22 23.0 W	GPS	4009					
06MT30/3 A1/E	539	1	ROS	121294	1707	BO	52 52.2 N	22 23.4 W	GPS	4014	4011	4072	18	24	1-10, 23
06MT30/3 A1/E	539	1	ROS	121294	1851	EN	52 53.0 N	22 24.6 W	GPS	3990					
06MT30/3 A1/E	540	1	ROS	121294	2313	BE	52 33.8 N	21 14.0 W	GPS	3789					
06MT30/3 A1/E	540	1	ROS	121394	0029	BO	52 33.6 N	21 14.6 W	GPS	3786	3837	3816	15	24	1-8, 23
06MT30/3 A1/E	540	1	ROS	121394	0158	EN	52 33.6 N	21 15.2 W	GPS	3791					
06MT30/3 A1/E	541	1	ROS	121394	0614	BE	52 19.9 N	20 00.1 W	GPS	3412					
06MT30/3 A1/E	541	1	ROS	121394	0728	BO	52 19.8 N	20 00.6 W	GPS	3277	3416	3454	17	24	1-10, 23
06MT30/3 A1/E	541	1	ROS	121394	0854	EN	52 19.6 N	20 01.1 W	GPS	3316					
06MT30/3 A1/E	542	1	ROS	121394	1249	BE	52 20.1 N	18 52.0 W	GPS	4284					
06MT30/3 A1/E	542	1	ROS	121394	1419	BO	52 20.7 N	18 52.9 W	GPS	4227	4265	4300	16	22	1-10, 23
06MT30/3 A1/E	542	1	ROS	121394	1600	EN	52 20.2 N	18 53.3 W	GPS	4255					
06MT30/3 A1/E	543	1	ROS	121394	1929	BE	52 19.8 N	17 49.9 W	GPS	4314					
06MT30/3 A1/E	543	1	ROS	121394	2048	BO	52 19.4 N	17 49.7 W	GPS	4313	4328	4395	11	24	1-10, 23
06MT30/3 A1/E	543	1	ROS	121394	2232	EN	52 19.2 N	17 49.3 W	GPS	4319					
06MT30/3 A1/E	544	1	ROS	121494	0120	BE	52 20.1 N	16 59.7 W	GPS	3916					
06MT30/3 A1/E	544	1	ROS	121494	0233	BO	52 20.0 N	16 59.4 W	GPS	3919	3932	3939	18	24	1-8 / ROS Test # 3
06MT30/3 A1/E	544	1	ROS	121494	0413	EN	52 20.2 N	16 58.8 W	GPS	3917					
06MT30/3 A1/E	545	1	ROS	121494	0655	BE	52 19.9 N	16 11.9 W	GPS	3446					
06MT30/3 A1/E	545	1	ROS	121494	0805	BO	52 19.7 N	16 11.0 W	GPS	3452	3452	3488	20	24	1-10, 23
06MT30/3 A1/E	545	1	ROS	121494	0935	EN	52 19.5 N	16 09.9 W	GPS	3449					
06MT30/3 A1/E	546	1	ROS	121494	1134	BE	52 20.0 N	15 46.9 W	GPS	3256					
06MT30/3 A1/E	546	1	ROS	121494	1241	BO	52 19.9 N	15 45.8 W	GPS	3248	3284	3282	20	24	1-10, 23
06MT30/3 A1/E	546	1	ROS	121494	1403	EN	52 19.9 N	15 44.9 W	GPS	3239					
06MT30/3 A1/E	547	1	ROS	121494	1714	BE	52 20.0 N	15 30.0 W	GPS	2776					
06MT30/3 A1/E	547	1	ROS	121494	1810	BO	52 20.0 N	15 29.6 W	GPS	2736	2754	2784	19	24	1-10, 23
06MT30/3 A1/E	547	1	ROS	121494	1926	EN	52 20.0 N	15 30.0 W	GPS	2751					
06MT30/3 A1/E	548	1	ROS	121594	0000	BE	52 19.9 N	15 12.9 W	GPS	1265					
06MT30/3 A1/E	548	1	ROS	121594	0031	BO	52 19.8 N	15 12.9 W	GPS	1262	1246	1254	20	14	1-10, 23
06MT30/3 A1/E	548	1	ROS	121594	0105	EN	52 19.4 N	15 13.0 W	GPS	1266					
06MT30/3 A1/E	549	1	ROS	121594	0224	BE	52 19.9 N	14 55.8 W	GPS	839					
06MT30/3 A1/E	549	1	ROS	121594	0242	BO	52 20.0 N	14 55.5 W	GPS	837	819	819	21	9	1-6, 23
06MT30/3 A1/E	549	1	ROS	121594	0307	EN	52 20.0 N	14 55.9 W	GPS	842					
06MT30/3 A1/E	550	1	ROS	121594	0424	BE	52 19.9 N	14 38.5 W	GPS	411					
06MT30/3 A1/E	550	1	ROS	121594	0433	BO	52 20.0 N	14 38.5 W	GPS	410	395	396		5	1-6, 23
06MT30/3 A1/E	550	1	ROS	121594	0446	BE	52 20.0 N	14 38.5 W	GPS	410					
06MT30/3 A1/E	551	1	ROS	121594	0616	BE	52 20.0 N	14 15.4 W	GPS	336					
06MT30/3 A1/E	551	1	ROS	121594	0626	BE	52 20.0 N	14 15.5 W	GPS	337	317	318	19	4	1-6, 23
06MT30/3 A1/E	551	1	ROS	121594	0636	BE	52 20.0 N	14 15.5 W	GPS	338					


7.2  LIST OF MOORED INSTRUMENTS

7.2.1  LEG M30/1

SEDIMENT TRAP MOORING POSITIONS

Trap            Coordinates           Depth
code          N             W         (m)
--------  ---------     ---------     ----
IOS       49 00,00'     16 28,20'     4806
OMEX IV   48 59,51'     13 44,06'     4485
OMEX III  49 05,30'     13 23,40'     3670
OMEX II   49 11,47'     12 48,00'     1418


7.2.2  LEG M30/2

CURRENT METER MOORING POSITIONS

Trap            Coordinates           Depth
code          N             W         (m)
--------  ---------     ---------     ----
K1        46 21.70'     29 59.29'     3220
K2        45 56.66'     31 49.04'     3630
K3        45 20.36'     33 15.69'     3640


7.2.3  LEG M30/3

CURRENT METER MOORING 

Code            Coordinates           Depth
              N             W         (m)
--------  ---------     ---------     ----
D2        57 24.7'      28 13.5'      2587


7.3  LIST OF FIGURES

Fig. (1)      Track and Station map of Meteor leg M30/1
Fig. (2)      Track and Station maps of Meteor legs M30/2 (WHP-A2) and M30/3 
              (WHP-A1)
Fig. (3a)     Nitrate (including nitrite) profiles
Fig. (3b)     Phosphate profiles
Fig. (3c)     Silicate profiles
Fig. (4a)     24-hour running means of current meter data from OMEX 2 at 620 m from   
              Jan - Sept 1994 (day Nos. 11 - 260).
Fig. (4b)     24-hour running means of current meter data from OMEX 2 at 1070 m   
              from Jan - Sept 1994
Fig. (4c)     24-hour running means of current meter data from OMEX 3 at 580 m from   
              Jan - Sept 1994 (Day Nos. 11 - 260).
Fig. (4d)     24-hour running means of current meter data from OMEX 3 at 1450 m 
              from Jan - Sept 1994 (Day Nos. 11 - 260).
Fig. (4e)     24-hour running means of current meter data from OMEX 3 at 3280 m 
              from Jan - Sept 1994 (Day Nos. 11 - 260).
Fig. (5)      A rough estimate of seasonality in sedimentation of the mooring    
              OMEX 3 between January and September 1994
Fig. (6)      Chloroplastic pigments and heterotrophic activity within the 
              uppermost centimetre of the sediments
Fig. (7a)     Distribution of water samples along section WHP-A2
Fig. (7b)     Salinity distribution from bottle samples along WHP-A2
Fig. (7c)     Potential temperature along WHP-A2
Fig. (7d)     Density sigma-theta distribution along WHP-A2
Fig. (7e)     Density sigma-2 (reference 2000 dbar) distribution along section 
              WHP-A2
Fig. (8a,b)   Potential temperature (8a) and depth (8b) of the Labrador Sea
              Water core along 48°N for 1982, 1993 and 1994
Fig. (8c,d)   Salinity (8c) and density (8d) of the Labrador Sea Water core 
              along 48°N for 1982, 1993 and 1994
Fig. (8e,f)   Depth-averaged potential temperatures (top) and salinities 
              (bottom) along 48°N for 1957-1994
Fig. (9a)     Distribution of dissolved oxygen along section WHP-A2
Fig. (9b-d)   Distributions of silicate (8b), nitrate (8c) and phosphate (8d) a
              long section WHP-A2
Fig. (10)     F 113 (upper part) and CCl4 distribution on A2. Values given in 
              ppt. 
Fig. (11)     Selected tritium profiles for the Western Basin on section A2
Fig. (12)     CTD-sections A1/West, (b) potential temperature (°C), (c) 
              salinity, (d) density (sigma-t)
Fig. (13)     Pre and post cruise calibration 
              (a) Pressure at T = 10°C (Oct 94)
              (b) Pressure at T = 1.6°C (Oct 94)
              (c) Pressure at T = 8 - 9°C (Nov 95)
Fig. (13d)    Pre- and post-cruise calibration, Temperature
Fig. (14a)    Salinity residuals, versus CTD salinity, M30/3
Fig. (14b)    Salinity residuals,versus CTD stations,M30/3
Fig. (15)     Oxygen residuals of final fit versus CTD stations
Fig. (16a)    Distribution of water samples along WHP-A1
Fig (16b-c)   Distribution of the concentrations of dissolved oxygen (16b) and 
              silicate (16c) along WHP-A1
Fig. (16d-e)  Distribution of nitrate (16d) and phosphate (16e) along WHP-A1
Fig. (17)     Within 3 years the LSW in the Irminger Sea cooled down in the 
              order of -0.23°C. The 3-year cooling rate from the Iceland Basin 
              and the Rockall Trough area is in the order of -0.1°C.
Fig. (18)     Within 3 years the density of the LSW core increased by 0.018 
              kg/m3 in the Irminger Sea and by 0.012 kg/m3 in the area east of 
              the MAR.
Fig. (19)     A mean deepening of the LSW core of about 250 dbar was found for 
              the Irminger Sea and of more than 200 dbar for the Rockall Trough 
              area. For the Iceland Basin a deepening of only 53 dbar was found.
Fig. (20)     No striking change of the LSW core salinity appeared within the 3 
              years of observation.
Fig. (21)     Positions of XBT profiles for "Meteor" cruise M30/3
Fig. (22)     XBT sections (a) A1/West, (b) A1/East
Fig. (23)     CTD and XCTD temperature profiles of the upper 150 dbar (a) at 
              stat. # 542, (b) at stat. # 546
Fig. (24)     CTD and XCTD temperature profiles of deeper layers
              (a) at stat. # 542, (b) at stat. # 546
Fig. (25)     CTD and XCTD conductivity profiles of the upper 150 dbar
              (a) at stat. # 542, (b) at stat. # 546
Fig. (26)     CTD and XCTD conductivity profiles of the deeper layers
              (a) at stat. # 542, (b) at stat. # 546
Fig. (27a,b)  Results of oxygen measurements at calibration stations, (a) 
              #496,(b) #517
Fig. (27c)    Results of oxygen measurements at calibration stations, (c) #544
Fig. (28a)    Quality control samples, (a) nitrate + nitrite and silicate
Fig. (28b)    Quality control samples, phosphate
Fig. (29a,b)  Distribution of tritium (A,B)along a section across the Labrador S
              ea (M30/3,WHP-A1W).
Fig. (29c,d)  Distribution of 3H/3He age (C, D) along a section across the 
              Labrador Sea (M30/3, WHP-A1W).
Fig. (30)     CFC11 section (pmol/kg) of the northern part of the WHP-A1W 
              Labrador Sea section
Fig. (31)     CFC11 concentrations vs theta-1,5 for the stations in the Labrador 
              Sea (€) and the central Irminger Sea (x). This density range 
              characterizes the Labrador Sea Water (LSW)
Fig. (32)     CFC11 section (pmol/kg) along section WHP-A1E
Fig. (33)     Cumulated depth profiles of CT-ant for the western (left) and 
              eastern (right panel) basins of the North Atlantic Ocean along 
              WHP-A2 in 1994 
Fig (34)      Profiles of total carbonate concentrations for selected stations 
              (#515, #529, #541) of M30/3, section WHP-A1
Fig (35)      One year of ALACE data in the Labrador Sea at 1500 m depth. 



8  CONCLUDING REMARKS

The scientific complements of all three legs of this Meteor cruise takes 
pleasures in expressing their appreciation to Captains Kull and Bruns and their 
crews for the excellent and patient support and encouragement during our work at 
sea. FS Meteor proved again a very hospitable and productive floating 
laboratory. We also would like to thank the "Meteor Leitstelle", "Deutsche 
Forschungsgemeinschaft", the "Bundesministerium für Forschung und Technologie" 
and "Auswärtiges Amt" for the help, support and their contribution towards the 
success of this cruise. The support of many people in our home laboratories 
ensured our work at sea; they might not have liked to work in the North Atlantic 
in autumn at conditions we encountered but they nevertheless were essential to 
the outcome of this cruise.

All three chief scientists are pleased with the outcome of these German 
contributions to global programmes that after a long time of planning finally 
came to fruition in an international, productive and pleasant collaboration both 
at sea and ashore.

The goals of this cruise were supported by grants to individual research groups 
within the frame-work of the German contributions to OMEX, WOCE and JGOFS and by 
grants of the Deutsche Forschungsgemeinschaft (Ko900/3-1 and Ko900/4-1) for the 
cruise. This support is gratefully acknowledged. 



9  REFERENCES

AMINOT, A., and KIRKWOOD, D.S. (1995):
    ICES (fifth) Intercomparison Exercise for Nutrients in Seawater, ICES 
    Copenhagen, (in press).
ATLAS, E.L., GORDON L.I., HAGER S.W., and P.K. PARK (1971):
    A practical manual for use of the Technicon AutoAnalyser in seawater 
    analyses, Revised Tech. Rep. 215, Ref. 71-22, Oregon State Univ., 47 pp.
BENDSCHNEIDER, K. and R.J. ROBINSON (1952): 
    A new spectrophotometric method for the determination of nitrite in 
    seawater, J. Mar. Res., (11) 1, p. 87-96.
CULBERSON, D.H. (1991): 
    Dissolved Oxygen. In: WHP Operations and Methods, WHP Office Report WHPO 91-
    1, 15 pp.
DICKSON, R.R., J. MEINCKE, S.-A. MALMBERG and A.J. LEE (1988):
    The "Great Salinity Anomaly" in the Northern North Atlantic 1968-1982. Prog. 
    Oceanogr., 20, p. 103-151.
ELGIN, R. H. (1994): 
    An Evaluation of XCTD Performance with Design Improvements. Sippican, Inc., 
    Marion, Mass., USA, unpublished, 6 pp.
GRASSHOFF, K., EHRHARDT, M., and K. KREMLING (1983): 
    Methods of Seawater Analysis, Verlag Chemie, Second Edition.
HANAWA, K., P. RUAL, R. BAILEY, A. SY and M. SZABADOS (1995): 
    A new depth-time equation for Sippican or TSK T-7, T-6 and T-4 expendable 
    bathythermographs (XBT). Deep-Sea Res., 42, p. 1423-1451. 
KIRKWOOD, D.S. (1995): Nutrients: Practical notes on their determination in 
    seawater, Techniques In Marine Environmental Science, (TIMES series), ICES, 
    Copenhagen, (in press).
KIRKWOOD D. S. and A. R. FOLKARD (1986):
    Results of the ICES salinity sample-bottle intercomparison. ICES C.M., 16 
    pp.
KIRKWOOD, D.S., A. AMINOT and M. PERTILLÖ (1991): 
    ICES (fourth) Intercomparison Exercise for Nutrients in Seawater, 
    Cooperative Research Report No. 174. ICES Copenhagen, 83 pp.
KOLTERMANN, K.P. and A. SY (1994):
    Western North Atlantic cools at intermediate depths. International WOCE 
    Newsletter, 15, p. 5-6.
KORTZINGER, A., L. MINTROP, J.C. DUINKER (1996)
    On the penetration depth and the inventory of anthropogenic CO2 in the north 
    Atlantic Ocean (submitted to JGR)
LAZIER, J. (1995):
    The salinity decrease in the Labrador Sea over the past thirty years. In: 
    Climate on decade-to-century time scales, National Academy of Sciences 
    Press. Washington, D.C. (in press).
LAZIER, J., M. RHEIN, A. SY and J. MEINCKE (in preparation):
    Surprisingly rapid renewal of Labrador Sea Water in the Irminger Sea. 
MILLARD, R. C. (1993):
    CTD oxygen calibration procedure. WHP Operations and Methods, WHP Office 
    Report WHPO 91-1, Revision 1, 29 pp.
MURPHY, J. and J.P. RILEY (1962): 
    A modified single solution method for the determination of phosphate in 
    natural waters, Anal. Chim. Acta, 27, p. 31-36.
MURRAY, C.N., J.P. RILEY and T.R.S. WILSON (1968):
    The solubility of oxygen in Winkler reagents used for the determination of 
    dissolved oxygen. Deep-Sea Res., 15, p. 237-238.
PINGREE, R.D. and B. LeCANN . (1989): 
    Celtic and Amorican slope and shelf residual currents. Prog. Oceanog. 23: 
    303-338.
PINGREE, R.D. and B. LeCANN (1990): 
    Structure, Strength and Seasonality of the slope currents in the Bay of 
    Biscay region. J.mar.biol.Ass.U.K. 70: 857-885.
PFANNKUCHE, O. (1993): 
    Benthic response to the sedimentation of particulate organic matter at the 
    BIOTRANS station, 47°N, 20°W. - Deep-Sea Res. II, 40: 135-149. 
READ, J.F. and W.J. GOULD (1992):
    Cooling and freshening of the subpolar North Atlantic Ocean since the 1960s. 
    Nature, 360, 55-57.
SIPPICAN, Inc. (1992): 
    MK-12 Oceanographic Data Acquisition System, User's Manual. Sippican, Inc., 
    Marion, Mass.
SIPPICAN, Inc. (1994): 
    XCTD: Expendable Conductivity, Temperature, Depth Profiling System. Document 
    presented at Oceanology International 94, Brighton, 8-11 March 1994.
SY, A. (1991):
    XBT measurements. In: WHP Operations and Methods, WHP Office Report WHPO 91-
    1, 19 pp.
SY, A. (1993): 
    Field Evaluation of XCTD Performance. WOCE Newsletter, No. 14, pp. 33-37.
SY, A. and H.-H. HINRICHSEN (1986):
    The influence of long-term storage on the salinity of bottled seawater 
    samples. Dt. Hydr. Z., 39, p. 35-40.
SY, A. and J.ULRICH (1994):
    North Atlantic Ship-of-Opportunity XBT Programme 1990, Ber. BSH, 1, 134 pp.
TALLEY, L.D. and M.S. McCARTNEY (1982):
    Distribution and circulation of Labrador Sea Water. J. of Physical 
    Oceanography, 12, 1189-1205. 
WOCE Operations Manual, WHP Operations and Methods (1994),
    Part 3.1.3 : WHP Office Report WHPO91-1, WOCE Report No. 68/91, rev. 1
WOCE Operations Manual, WHP Operations and Methods (1994), 
    Part 3.1.2 : Requirements for WHP Data Reporting, Report WHPO90-1, WOCE 
    Report No. 67/91, rev. 2




A01 CTD AND BOTTLE DATA CHECK

About the '_check.txt', '_sal.ps' and '_oxy.ps' files:

The WHP-Exchange format bottle and/or CTD data from this cruise have been
examined by a computer application for contents and consistency. The
parameters found for the files are listed, a check is made to see if all
CTD files for this cruise contain the same CTD parameters, a check is made
to see if there is a one-to-one correspondence between bottle station
numbers and CTD station numbers, a check is made to see that pressures
increase through each file for each station, and a check is made to locate
multiple casts for the same station number in the bottle data. Results of
those checks are reported in this '_check.txt' file.

When both bottle and CTD data are available, the CTD salinity data (and, if
available, CTD oxygen data) reported in the bottle data file are subtracted
from the corresponding bottle data and the differences are plotted for the
entire cruise. Those plots are the' _sal.ps' and '_oxy.ps' files.


FOLLOWING PARAMETERS FOUND FOR BOTTLE FILE:

EXPOCODE        TIME            SALNTY          NO2+NO3
SECT_ID         LATITUDE        SALNTY_FLAG_W   NO2+NO3_FLAG_W
STNNBR          LONGITUDE       CTDOXY          PHSPHT
CASTNO          DEPTH           CTDOXY_FLAG_W   PHSPHT_FLAG_W
SAMPNO          CTDPRS          OXYGEN          CFC-11
BTLNBR          CTDTMP          OXYGEN_FLAG_W   CFC-11_FLAG_W
BTLNBR_FLAG_W   CTDSAL          SILCAT          CFC-12
DATE            CTDSAL_FLAG_W   SILCAT_FLAG_W   CFC-12_FLAG_W
          

A01E_A01W_HY1.CSV -> NO2+NO3_FLAG_W FOUND WITHOUT MATCHING PARAMETER.

All ctd parameters match the parameters in the reference station.
Station #498 exists in a01e_a01w_hy1.csv, 
    but does not have a corresponding CTD file.
Station #499 exists in a01e_a01w_hy1.csv, 
    but does not have a corresponding CTD file.
Station #502 exists in a01e_a01w_hy1.csv, 
    but does not have a corresponding CTD file.

No bottle pressure inversions found.
Bottle file pressures are increasing.

No multiple casts found in bottle data.



A02 CTD AND BOTTLE DATA CHECK

About the '_check.txt', '_sal.ps' and '_oxy.ps' files:

The WHP-Exchange format bottle and/or CTD data from this cruise have been
examined by a computer application for contents and consistency. The
parameters found for the files are listed, a check is made to see if all
CTD files for this cruise contain the same CTD parameters, a check is made
to see if there is a one-to-one correspondence between bottle station
numbers and CTD station numbers, a check is made to see that pressures
increase through each file for each station, and a check is made to locate
multiple casts for the same station number in the bottle data. Results of
those checks are reported in this '_check.txt' file.

When both bottle and CTD data are available, the CTD salinity data (and, if
available, CTD oxygen data) reported in the bottle data file are subtracted
from the corresponding bottle data and the differences are plotted for the
entire cruise. Those plots are the' _sal.ps' and '_oxy.ps' files (not available).

FOLLOWING PARAMETERS FOUND FOR BOTTLE FILE:

EXPOCODE       LATITUDE       OXYGEN          CFC-11
SECT_ID        LONGITUDE      OXYGEN_FLAG_W   CFC-11_FLAG_W
STNNBR         DEPTH          SILCAT          CFC-12
CASTNO         CTDPRS         SILCAT_FLAG_W   CFC-12_FLAG_W
SAMPNO         CTDTMP         NITRAT          CFC113
BTLNBR         CTDSAL         NITRAT_FLAG_W   CFC113_FLAG_W
BTLNBR_FLAG_W  CTDSAL_FLAG_W  PHSPHT          CCL4
DATE           SALNTY         PHSPHT_FLAG_W   CCL4_FLAG_W
TIME           SALNTY_FLAG_W

All ctd parameters match the parameters in the reference station.
Station #436 exists in a02a_hy1.csv, but does not have a corresponding CTD file.

No bottle pressure inversions found.
Bottle file pressures are increasing.

A02A_HY1.CSV -> CONTAINS STATIONS WITH MULTIPLE CASTS:

station -> 445:    station -> 453:    station -> 468:    station -> 474:
  2 casts.           3 casts.           2 casts.           2 casts.
station -> 446:    station -> 454:    station -> 469:    station -> 476:
  2 casts.           2 casts.           2 casts.           3 casts.
station -> 449:    station -> 455:    station -> 470:    station -> 479:
  2 casts.           2 casts.           2 casts.           2 casts.
station -> 450:    station -> 456:    station -> 471:    station -> 483:
  2 casts.           2 casts.           2 casts.           2 casts.
station -> 451:    station -> 457:    station -> 472:    station -> 486:
  2 casts.           2 casts.           2 casts.           2 casts.
station -> 452:    station -> 458:    station -> 473:   
  2 casts.           2 casts.           2 casts.   





WHPO DATA PROCESSING NOTES

A01
Date      Contact      Data Type    Data Status Summary
--------  -------      -----------  ----------------------------------------
11/05/96  Sy           BTL          Update Needed
          Cruise "Meteor" 30, leg 3, bottle data processing.
          
          Because of the very limited resources it was necessary to deviate 
          in some points from requirements outlined in WHPO 90-1.
          
          Otherwise different bottle data files ought to have been assembled 
          according specific needs and specific computer software. Thus 
          please, note the differences from WHP water sample requirements as 
          described in WHPO 90-1 (section 3.3). 
          
          Data are reported in terms of corrected samples, i.e. mis- or 
          double trips in the CTD rosette are corrected. No serious rosette 
          problems occured during this cruise.
          
          Clearly bad (wrong) bottle trips have been removed completely.
          
          Bad single measurements have been removed and marked by 4.
          
          Samples drawn from leaking (malfunctioning) bottles are not 
          reported except values seem to be more or less reasonable.
          
          BIO denotes the Bedfort numbering system we used.
          
          CTDRAW is not a real raw pressure. The values reported are 
          calibrated in our acquisition data stream (transformation in 
          physical units (dbar)) and stored in the bottle data file. CTDRAW 
          is corrected according laboratory calibration results (unloading 
          courve) and pressure offset correction from beginning of profile.
          
          CTDTMP is reported in ITS-90.
          CTDSAL has been corrected with in-situ salinity correction.
          Standard Conductivity used was C(15,35,0)=42.914.
          OXYGEN has not been yet converted to UMOL/KG. They are reported as 
          measured.
          
          Finally: if you find errors of any kind, discrepancies in the 
          data, etc, etc, please contact me. As anyone else I would like to 
          work with the best available version of Meteor 30/3 data.
                

A01
Date      Contact      Data Type    Data Status Summary
--------  -------      -----------  ----------------------------------------
03/09/99  Kappa        DOC          PDF DOC Directory Assembled
          ~a01ew_btl.data.proc.pdf
          ~a01ew_doc.pdf
          ~a01ew_notes
                
05/27/99  Diggs        CTD          Website Updated
                
12/12/99  Arnold       He/Tr/C14    Submitted
                
04/24/00  Kappa        Cruise ID    ar07 and EW designations deleted
                   
07/10/00  Huynh        DOC          pdf, txt versions updated, online
                   
04/23/01  Bayer        He/Tr/C14    Website Updated; Status changed to Public 
          Yes, all of our data submitted to WHPO is public. 
                
06/27/01  Uribe        CTD          Website Updated; EXCHANGE File Added
          CTD exchange files were put online.
                      
08/09/01  Uribe        BTL          Website Updated; Correct EXCHANGE File 
          Added  The bottle exchange file was made. The wrong file had been 
          online until this date.
                
12/17/01  Hajrasuliha  CTD/BTL      Internal DQE completed
          a01w_ar13_ar05_x_hy1.Exchange ->  
            NO2 NO3_FLAG_W found without matching parameter 
          Station #491 exists in a01e_a01w_hy1.Exchange, 
            but does not have a corresponding CTD file. 
          Station #492 exists in a01e_a01w_hy1.Exchange, 
            but does not have a corresponding CTD file. 
          Station #493 exists in a01e_a01w_hy1.Exchange, 
            but does not have a corresponding CTD file 
          A lot more of the same problem. 
          

A01
Date      Contact      Data Type    Data Status Summary
--------  -------      -----------  ----------------------------------------
12/17/01  Diggs        CTD          Website Updated; Data Merged into OnLine File
          All exhange and WOCE formatted CTD files corrected, reformatted 
          and placed online. Please see additional notes.
          
          CORRECTLY RE-FORMATTED ALL CTD FILES:
          
          This was necessary for the Exchange format conversion.
          
          Old zip archive of Exchange file only had one CTD cast (file):
          All old WOCE formatted CTD files with one exception had problems:
          Performed the following:
          ~ Changed all EXPOCODES to 06MT30_3 (no '/')
          ~ Changed all WOCE LINE names to A01E (from A1/E)
          ~ Corrected param header from 'DEG C' to DEG_C
          ~ Removed all double line feed characters
          ~ Removed all extra lines and ctrl-Z characters
          ~ Had to place NO_DATA values (-999) in NUMBERS column
          
          Code to rewrite files with -999 in NUMBERS column, remove dbl-lfs, 
          and ctrl-z characters is called 'add_number_ctd.pl' and it in my 
          home directory.
          
          Replaced both zip archives on website with correct ones, 
          thoroughly checked with JOA3.0.
                
03/07/03  Anderson     BTL  Website Updated; Data remerged into BTL file
          ~ missing data changed.  
          ~ Remerger updated CFCs, 
          ~ merged TRITUM, HELIUM, DELHE3, DELC14, TRITER, HELIER, DELHER, 
            and C14ERR. 
          ~ Copied QUALT1 flags to QUALT2 flags. 
          ~ Changed missing data from -9.0 to -999.0 for DELHE3 and DELC14. 
          ~ Put file online, made new exchange file, 
          ~ sent notes to Jerry.
          
          March 7, 2003  
          EXPOCODE 06mt30_3, WHP-ID a01ew  
          a01ew (06mt30_3) notes:
          
          ~ Remerged updated CFC11 and CFC12 from file meteor303.sea  and 
            added TRITUM, HELIUM, DELHE3, DELC14, TRITER, HELIER, DELHER, and 
            C14ERR from file 06mt303.sea found in 
            a01/a01ew/original/1999.12.12_A01EW_TRACER_RHEIN_ARNOLD 
            to online file 19990723WHPOSIOSCD.  
          ~ Changed missing values for DELHE3 and DELC14 from -9.0 to -999.0
          ~ Copied QUALT1 flags to QUALT2 
          ~ Put new file online, made new exchange file. 
          
          Sarilee Anderson
                
      

          
A02
Date      Contact      Data Type    Data Status Summary
--------  -------      -----------  ----------------------------------------
09/21/98  Anderson     CTD/BTL/SUM  Data Update; conversion to WOCE format
                
03/02/99  Diggs        CTD/BTL/SUM  Website Updated
                
04/14/99  Kappa        DOC          PDF DOC Dir. Assembled
          ~ a02_06MT30_2 notes.pdf
          ~ a02_06mt30_2doc.pdf
          ~ a02_06mt30_2hyd.hist
                  
04/30/99  Kappa        DOC          PDF Directory Updated; 
          a02_06MT30_2_cruzpln.pdf added
                
10/28/99  Koltermann   CTD/BTL      Website Updated; Status changed to Public
          As per your email on 10.15.1999 I have obtained the G316 cruise 
          from Lynne Talley's website and released all data for the following 
          cruises to the public domain:
          ~ 06MT30_2
          ~ 06MT39_3
          ~ 06GA276_2
          ~ 06GA316_1
                
11/15/99  Buck         DOC          Data Update; pdf version online
                
12/10/99  Klein        CFCs         Submitted  new data files
                
12/29/99  Newton       CFCs         Reformatted by WHPO
          New CFCs merged into .hyd file
          Notes on changes EXPOCODE 06MT30_2       WHP-ID A02    
          ~ merging in new CFC-11 CFC-12 CFC113 CCL4 in a02ahy.txt 
          ~ changed CFC-13 column label to CFC113
          ~ changed CTDRAW column label to CTDPRS
          ~ 2 samples in the new file being merged did not have corresponding
            samples in the existing file. Station 462, Cast 1, samples 11 and 3.
            29Dec99 DMN
                

A02
Date      Contact      Data Type    Data Status Summary
--------  -------      -----------  ----------------------------------------
02/22/00  Diggs        CFCs         Data Update
          Cruise 06MT30_2 (A02(a)) has had the new CFC values merged in.  
          All files and tables have been updated.
                
05/31/00  Kromer       DELC14lvs    Data Requested by jlk
                
06/06/00  Anderson     LVS          Data Update; BTL/SUM files reformated
          a02alv.txt
          
          .sum file does not have any information for type LVS.  Some info 
          appears in the Staion List in the .doc file, so using the .doc 
          Station List I added the LVS info that was available (only BO) to 
          the .sum file.  
          
          The .sum, .doc, and .sea files have stations 436-488.   The  .LVS 
          file from Arnold Matthias has stations after 488 (493, 498, 500, 
          503, 514, and 526.  I left these out because I don't know where 
          they belong.   
          
          The .doc Station List indicates LVS for station 436 but there is 
          no LVS data for 436 in the .LVS file.   
          
          Sta. 445 - the .LVS file has casts as 1 & 2, the .doc Station list 
          has casts 1 & 3.  Since the .sum and .sea, and .doc have the ROS 
          casts as 2 & 4, I changed the .lvs casts to 1 & 3. 
          
          Sarilee Anderson (sanderson@ucsd.edu)  
                
06/07/00  Diggs        LVS          Website Updated
          I have updated this cruise and added the 1st of many LVS files to 
          its index page.  The sumfile has also be replaced/updated and all 
          additional files and tables have been updated accordingly.
                

A02
Date      Contact      Data Type    Data Status Summary
--------  -------      -----------  ----------------------------------------
09/13/00  van Aken     SUM          Update Needed
          In two weeks time I will leave for a CLIVAR survey of the former 
          A1E section. As a preparation I have downloaded from WHPO  the 
          data of your two A2 surveys (Meteor cruises 30 and 39). It 
          appeared the the summary files still contain some errors in 
          position (probably typos) when you plot the cruise track from 
          these positions. A more serious error is that for meteor cruise 
          39-3 the nitrate and silicate data are in the wrong columns, or 
          have the wrong headers. And a remaining question is, are the 
          chemical data for cruise 39 indeed in micromol per liter instead 
          of kg?  Comparison of data from both cruises suggests (but not yet 
          beyond reasonable doubt), that in both cruises the concentration 
          units are similar.
                
10/30/00  Huynh        DOC          Website Updated
          data processing notes added to pdf/txt docs
                
06/20/01  Uribe        BTL          Website Updated; Data added to website
              
06/21/01  Uribe        CTD/BTL      Website Updated
          ~ CTD EXCHANGE File Added 
          ~ BTL EXCHANGE file modified.  
          ~ The exchange bottle file name in directory and index file was 
            modified to lower case.
          ~ CTD exchange files were put online.
                
09/17/01  Uribe        CTD/BTL/SUM  Website Updated
          New data received, replaced online data
          SUM, CTD and bottle data has been updated by newly received data. 
          Minor reformatting was done and bottle exchange code was re-run. 
          Old data was moved into the original directory.
                
12/21/01  Hajrasuliha  CTD          Internal DQE completed
          created *check.txt file for the cruise. Did NOT create .ps files.
          
12/21/01  Uribe        CTD          Website Updated, EXCHANGE File Added
          CTD has been converted to exchange using the new code and put 
          online. For station 488 a last line was added to the sumfile with 
          a BO to allow the code to create the file for that station.
                
      

          

