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CRUISE REPORT: SAVE1
(Updated APR 2011)



HIGHLIGHTS
Cruise Summary Information

           WOCE Section Designation  SAVE1
 Expedition designation (ExpoCodes)  316N19871123
                   Chief Scientists  Taro Takahashi/LDEO
                                     Peter B. Rhines/UW
                              Dates  1987 NOV 23  - 1987 DEC 13  
                               Ship  R/V Knorr
                      Ports of call  Recife, Brazil to Abidjan, Ivory Coast

                                                5° 28.5' N
              Geographic Boundaries  35° 11' W              9° 58' W
                                                10° 0.3' S
                           Stations  34
       Floats and drifters deployed  0
     Moorings deployed or recovered  0
 

                     Chief Scientists' Contact Information

                                Taro Takahashi
           Lamont-Doherty Earth Observatory of Columbia University,
       101 Comer • 61 Route 9W - PO Box 1000 • Palisades NY 10964-8000 • US
  Phone: (845) 365-8537 • Fax: (845) 365-8155 • Email: taka@ldeo.columbia.edu

                                Peter B. Rhines
     Prof. of Oceanography and Atmospheric Sciences School of Oceanography 
                      319 Ocean Science Bldg • Box 357940 
             University of Washington • Seattle, Washington, 98195
           Phone: 206-543-0593 • e-mail: rhines@ocean.washington.edu





                South Atlantic Ventilation Experiment (SAVE) Leg 1

                   Shipboard Chemical and Physical Data Report

                                  PRELIMINARY

                        23 November - 13 December 1987

                                  R/V Knorr


                           Data Report Prepared by:

                         Oceanographic Data Facility
                      Scripps Institution of Oceanography
                      University of California, San Diego

                                  April 1988




Sponsored by
National Science Foundation
Grant OCE-86 13330                                     ODF Publication No. 224






                                Taro Takahashi
         Lamont-Doherty Geological Observatory of Columbia University,
                                 Palisades, NY



                                Peter B. Rhines
               School of Oceanography, University of Washington,
                                  Seattle, WA





INTRODUCTION

The major objective of the South Atlantic Ventilation Experiment (SAVE) 
program is to investigate the rates of ocean circulation, mixing, 
ventilation, inter-ocean exchange and carbon-oxygen-nutrient cycling on an 
ocean-basin scale in the South Atlantic Ocean. Standard hydrographic 
measurements (temperature, salinity and the concentrations of dissolved 
oxygen and nutrient salts) as well as the observations on the distribution of 
transient and radioactive tracers and CO2 are made in order to provide strong 
constraints on time-averaged rates of circulation and mixing and to reveal 
transport pathways between the air/sea interface and the abyssal ocean.

Leg I of the SAVE program combines some features of a zonal section, such as 
western and eastern boundary currents, mid-ocean gyres and deep water 
regimes, with other features of meridional sections, in particular the 
equatorial crossing. It was ideally suited to look at the legendary 
bifurcation of water masses that are crossing the equator. Recent dynamical 
theories have given strength to the idea that water masses driven from high 
northern latitudes should arrive along a "Kelvin-wave" pathway at the 
equator, and then split with some fluid passing eastward along the equator 
and the rest continuing down the western boundary. The data obtained during 
this and other legs of SAVE and the prior Oceanus 133 sections should yield 
an increasingly sharper picture of the Brazil Basin water masses. This should 
tell us whether classical circulation models do or do not account for the 
interior circulation and tracer balance and the nature of the western 
boundary currents. This report summarizes shipboard observations and 
operations made during Leg 1 of the SAVE Program.


OVERVIEW OF THE EXPEDITION

The R/V Knorr departed at 11:30, November, 23, 1987, from Recife, Brazil, for 
Leg 1 of the SAVE program, and arrived Abidjan, Ivory Coast, at noon, 
December 13, 1987, During the 21-day leg, the following number of 
measurements were made aboard the ship:

     Salinity                               1,402
     Oxygen dissolved in seawater           1,174
     Nutrient salts dissolved in sea water  1,148 for each of nitrate,
                                            phosphate and silicate.
     Freons dissolved in seawater           723 for each of Freon-11 and -12.
     Total CO2 dissolved in seawater        743
     pCO2 in seawater                       640


The following number of samples were collected and processed aboard the ship 
for the shore-based measurements;

     Helium-3 in seawater                   360
     Tritium in seawater                    360
     Radium-228 in seawater                 155
     Carbon-14 in seawater                  121
     Krypton-85 in seawater                 39
     Argon-39 in seawater                   1
     
In addition, the atmospheric CO2 concentration, partial pressures of CO2, CH4 
and N2O in surface water and in air were measured continuously throughout the 
expedition. A set of underway samples, which include an XBT cast and a sample 
each for the determination of dissolved oxygen, nutrient salts and CO2 
concentrations and CO2 partial pressure in seawater, was collected twice 
between two regular stations.

The expedition was generally successful. The 36-bottle Rosette sampler and 
CTD functioned flawlessly throughout the expedition. However, it was marred 
by the loss of nine 270-liter Gerard samplers due to a failure of trawl cable 
at Station 32 located in the Romanche Fracture Zone at the equator and 17 
degrees 43 minutes West. The cable failed during the winding-up operation of 
a Deep Gerard Cast at a point of about 600 meters below the sea surface with 
a total length of about 5800 meters of cable out. Since the sea was calm 
during the entire station operation, the cable was not subjected to unusual 
stress before and at the time of failure. Furthermore, the cable had been 
used for sampling at depths exceeding 5800 meters at previous stations. 
Therefore, the break was tentatively judged as a result of metal fatigue 
after a long use since it was first installed in 1980 or thereabout. Since 
the Gerard samplers and failed cable fell onto a 6000 meter deep narrow 
valley floor of the Romanche Fracture Zone, and since the designated tensile 
strength of the new cable was found to be marginal to lift the weight of the 
lost cast (5800 meters of cable plus nine Gerard samplers), a recovery 
operation was not attempted.

A new 9000-meter trawl cable, which had been stored in the ships hold, was 
put on the winch immediately after the unfortunate cast, so that large-volume 
sampling operations can be continued using the remaining two Gerard samplers 
aboard. At the large-volume stations after Station 32, three casts of two 
Gerard samplers were deployed to collect subsurface samples down to about 
1000 meters and a pump to collect surface water samples. Because of the 
shortage of station time, no large volume sample was obtained below 1000 
meters in the Eastern Basin of the South Atlantic during Leg 1.


COMMENTS ON THE SHIPBOARD WATER SAMPLING PROCEDURES

During Leg 1, water samples were drawn from each 10-liter Niskin sampler by 5 
to 6 analysts and technicians each assigned to specific properties in the 
following sequence; Freons, helium-3, oxygen, total CO2, pCO2, tritium, 
nutrients and salinity. During the first half dozen stations, sampling 
operation of a 36-bottle Rosette took as much as two and a half to three 
hours due to varied sampling requirements. At Station 16, the sixth but the 
first daytime station after leaving Recife, an awning was erected over the 
staging area in order to protect the Rosette and water samples from rapid 
warming due to the blazing equatorial sun shine. Even under this protection, 
deep water samples, for example, warmed up by 13°C to about 17°C by the time 
when the water samples were drawn for chemical analyses of dissolved gases. 
It was feared that the gas concentration in the water in a Niskin bottle 
might have been altered by gas exchanges with the air introduced into the 
head space, and that the sample alteration might also have been exacerbated 
by increasing water temperature. Therefore, a number of time-series sampling 
experiments was conducted in order to assess the extent of sample 
alterations.

Figure 1 shows the results of a time variation of oxygen concentration in the 
water samples drawn from a low-oxygen water collected at about 300 meters 
deep by a single 10-liter Niskin bottle wire cast. The wire cast was selected 
so that the contact time of the sample water with warm near surface waters 
(up to 30°C) can be minimized. The head space, water temperature and the 
oxygen concentration in the drawn water samples are plotted as a function of 
time in Figure 1. At the time of the first draw of water sample for oxygen 
analysis, the water warmed up only by about 0.5°C from 11.97°C to 12.5°C. It 
is seen in Figure I that the oxygen concentration increased by about 0.04 
mL/L for the first 6 minutes, steadied (or decreased somewhat) at this level 
for the following 14 minutes, and then increased rapidly for the remaining 
duration of the experiment. All the oxygen measurements were made by the 
Winkler titration method immediately after the samples were collected. The 
observed initial increase appears to be real in view of the precision of ± 
0.01 mL/L or better estimated on the basis of the multiplicate determinations 
made during the expedition. Possible causes for the changes observed during 
the first 10 minutes will be discussed below. Two extreme cases may be 
considered. First, if the water in the Niskin sampler is not mixed 
vertically, the effect of sample alteration should be confined to the upper 
portion, and hence the water samples drawn from a spigot located near the 
bottom of the bottle should not show any change in the oxygen concentration 
until more than a half of the water was drained. Secondly, if the water in 
the sampler was mixed homogeneously as it was drained and at the same time 
took up oxygen from the air introduced into the head space, the oxygen 
concentrations in the water samples should increase with time as shown by the 
solid curves in the right-hand panel of Figure 1. Three model curves 
represent the cases for the assumed air-water gas transfer velocity values of 
0.01, 0.02 and 0.04 cm/mm respectively. The data appear to be broadly 
consistent with the middle curve, although they tend to be higher during the 
first six minutes and lower during the following 20 minutes or so. This 
behavior suggests that the water column in the cylindrical Niskin sampler 
might have been convecting as a result of heating through the outer wall, and 
that the water samples drained from the sampler might represent varying 
portions of a convective cell or different convective cells formed within the 
sampler. Convective motion could rapidly transport a parcel of contaminated 
water from the top of the Niskin sampler down to the bottom where the 
sampling spigot is attached.


Figure 1: A time-series study of the temperature and oxygen concentration in 
          the water samples drawn from a 10-liter Niskin sampler. The water 
          was collected at about 300 meters deep off the coast of Liberia 
          within an oxygen minimum layer. The in situ temperature of water 
          was 11.97°C


We have conducted a number of time-series experiments similar to that 
described above for oxygen as well as for CO2 using samples with varying 
degrees of saturations, and obtained the results consistent with those 
described above. It was observed that about 2 uM/kg of CO2 were lost from a 
deep water sample (about 1300 uatm pCO2) during the first 30 minutes of water 
sampling operations. Since the concentrations of nutrient salts were also 
measured and found to be invariant with time during the duration of 
experiments, the observed changes in dissolved oxygen and CO2 were not due to 
biological activities. We were unable to conduct experiments for Freons, 
since the Freon measurement system exhibited high backgrounds during Leg 1. 
Hopefully, a series of Freon time-series experiments will be carried out 
during the following legs.

Based upon the time-series experiments conducted during Leg 1, the following 
conclusions and recommendations may be made.

1) When a number of water samples are drawn from a Niskin sampler, the gas 
   concentrations may be altered by gas exchange between the water and the 
   air introduced into the head space. A column of cold water sample in the 
   Niskin sampler may be mixed convectively due to heating through the outer 
   wall during its exposure to warm waters near the sea surface and to warm 
   air. Thus a parcel of altered water near the top of the column may be 
   transported downward to a sampling spigot located near the bottom of the 
   column. Our observations suggest that the magnitude of sample alteration 
   is of an order of analytical precision for dissolved oxygen and CO2 
   determinations, if water samples were collected within 20 minutes after a 
   10-liter Niskin sampler was brought up onto the deck.

2) The magnitude of sample alteration increases rapidly with increasing 
   contrast in the partial pressures (or concentrations) of a gaseous species 
   between air and water samples. The worst case is Freons, since deep waters 
   contain virtually no Freons, whereas the shipboard air contains sometimes 
   much higher concentrations of Freons than clean marine air due to local 
   sources.

3) We recommend the following drawing order for water samples for gas 
   analyses; Freons, helium-3, oxygen and CO2. This should be followed by 
   tritium, nutrients and salinity samples.

4) Throughout Leg 1, the water sampling operations were conducted by a half 
   dozen analysts and technicians, who are specialized for collecting 
   specific water samples only for Freons, helium, CO2 or oxygen. This had not 
   only caused a traffic jam around the Rosette, but also drained the energy 
   of analysts and reduced the time available for chemical analyses. 
   Therefore, we recommend that, during the following legs, the operation 
   should be streamlined by assigning a few technicians exclusively for water 
   sampling, and that the analysts should be kept with their respective 
   analytical instruments without interruptions for water sampling.

5) Since an increasing variety of water samples for gas analyses will be 
   collected in future oceanographic expeditions, we recommend that a 
   development of advanced water samplers is important for preventing sample 
   alterations occurred by contact between the water and the air introduced 
   into the head space while water samples are drained.


DISTRIBUTION OF VARIOUS PROPERTIES


The major oceanographic features observed during the SAVE Leg 1 Expedition 
will be briefly described below.


Western Boundary Current and Central Water

a) Upper Layers:

We experienced strong southward current near the Brazilian shelf break (10°S, 
35°W), even though we were just south of the climatological stagnation point 
for the upper level circulation. The mean zero wind-curl line runs NW-SE from 
Capo Blanco just north of Recife toward Walvis Bay, and serves as a crude 
predictor for the bifurcation point of the zonal equatorial currents between 
southward and northward flowing boundary currents. Simple Sverdrup theory 
suggests that the bifurcation point will be shifted poleward by the non-zonal 
orientation of the zero curl line.

The isopycnals tilt upward toward the western boundary current in the shallow 
water, as expected from thermal wind balance. But below there is a more 
marked downtilt toward the boundary with 150 db being the pivot point for 
sigma theta and most tracers. The isopleths for total CO2 concentration bend 
upward above 150 db, whereas they bend sharply downward at greater pressures. 
The former appears to be the effect of the continental shelf, where CO2 is 
released from shelf sediments rich in carbon. The downward bending below 
about 150 db in part mirrors the tilt of isopycnals, but this is also 
observed even in density space. The downtiltlng boundary current is 
characterized by very low nutrients, high oxygen, fresh salinity, high Freons 
and low CO2, in plots of constant potential density surfaces as well as level 
surfaces. The feature is not easy to find in historical maps of properties. 
This thick region of shear appears to connect with the system of Equatorial 
countercurrents described by Cochrane et al. (JPU, 1979).

In the northwestern part of the SAVE Leg 1 section, there was a clear shallow 
salinity maximum, analogous to the Subtropical Underwater of the North 
Atlantic, a signal of high evaporation in the nearby tropics. There were 
strong double diffusive staircases visible in the region just below this 
salinity maximum.

b) Deep Layers:

The distribution of the total CO2 concentration below 500 meters along the 
SAVE Leg 1 tracks is shown in Figure 2. The section defined by Stations 11 
through 19 (i.e. the right half) represents a zonal section oriented nearly 
right angles to the Brazilian coast line, whereas that defined by Stations 19 
through 27 (i.e. the left half) is oriented diagonally across the tropical 
South Atlantic in the general direction of SW-NE. A western boundary 
undercurrent consisting of the North Atlantic Deep Water is clearly depicted 
by a low CO2 area (see the 2215 and 2220 uM/L contours) centered around 1800 
db near the western margin of the section. This low CO2 area coincides with 
the high Freon concentrations observed between 1700 and 1900 db in this area 
during the 1981 TTO/TAS Expeditions. However, because of high backgrounds in 
the Freon analysis system during the SAVE Leg 1, the previous observations 
could not be confirmed. Although signals for the boundary current are visible 
in the oxygen, nutrient salts and salinity data, the CO2 data appear to show 
the boundary current more clearly than other properties.


                       TCO2(uM/L), South Atlantic Ocean

                               SAVE Station No.


Figure 2: Distribution of the total CO2 concentration in the western South 
          Atlantic Basin along the SAVE Leg 1 tracks. The low CO2 area 
          centered around at 2000 meters near the South American coast (right 
          side of the figure) indicates the western boundary current 
          originated from the high latitude North Atlantic Ocean.


A low CO2 layer having similar CO2 values as those for the boundary current is 
seen further east in a pressure range of 1500 to 2000 db. This indicates the 
upper portion of the NADW, whereas another low CO2 area (defined by the 2230 
uM/L contour) observed around 3500 db at Stations 23 through 27 indicates the 
lower NADW.

There appears to be a small high CO2 zone depicted by a 2260 uM/L contour near 
34°W between 450 and 650 db (see the upper right hand corner of Figure 2). 
Since this water has high oxygen concentrations, it is suspected that this 
may represent a boundary current originating in the Southern Ocean.


Equatorial Region

a) Temperature, Salinity and CO2:

In the upper ocean the high salinity evaporation signal weakens 
northeastward, and the mixed layer depth decreases along the section. 
Extremely low salinity values and thin mixed layer were observed near the 
Liberian coast. Meanwhile, the 10°C isotherm deepens remarkably between 
Stations 23 and 26. The thermocline at the mixed layer base was very thin and 
sharp at 3°S. The equatorial zone shows many interesting extrema, but perhaps 
fewer number of clear "bullets" than expected. Continuous vertical profiles 
of oxygen, temperature and salinity show rugged structure down to at least 
1000 meters deep near the equator and there are strong features in the tracer 
distributions off the equator. This may corresponds to the subtherrnocline 
countercurrents observed by Firing and Cochrane et al. (JPO, 1979) off the 
equator in the Pacific Ocean.

The Equatorial Undercurrent is well resolved by various quantities measured. 
In Figure 3, the meridional distribution of the total CO2 concentration in the 
upper 1000 meters is shown across the equator. 1ie Equatorial Undercurrent 
centered around 100 db is clearly depicted by a downward bulge of isopleths 
exceeding 300 db. Below the Undercurrent signals, high CO2 deep waters are 
observed as outlined by the mushroom-shaped 2260 uM/L contour. Toward south of 
the equator, two high CO2 water masses are observed in a pressure range 
between 300 and 700 db and between 800 and 1000 db (see 2280 uM/L contour 
lines). The upper portion of the shallower CO2 high corresponds to the low 
oxygen water, and local minimum between the two CO2 maxima corresponds to the 
core of AAIW.

b) Oxygen Minimum Layer:

The oxygen minimum layer is observed near a sigma theta value of 26.8 (Figure 
4) nearly throughout the SAVE Leg 1 tracks. The minimum strengthens 
northeastward, ranging from 200 uM/kg near the Brazilian shelf to 60 uM/kg 
near Liberia. This layer disappears suddenly in the western boundary current, 
which is protected from this tropical influence.


Antarctic Intermediate Water (AAIW)

The Antarctic Intermediate Water mass is observed in the vicinity of 27.25 
sigma-theta density. In the Western Basin of the South Atlantic, the 
temperature-salinity signals for AAIW is very noisy, indicating interleaving 
of water layers and hence active erosion of the AAIW. The salinity signal for 
AAIW weakens eastward, but rather gradually from typically 34.4 to 34.6 ‰, 
The oxygen field also weakens gradually to the east (Figure 4). The 
associated nutrient maxima are intriguing: the silica maximum is located at 
deeper level than the salinity minimum.


Figure 3: Distribution of the total CO2 concentration in seawater in the 
          equatorial Atlantic Ocean along the SAVE Leg 1 tracks. The equator 
          was crossed at 17° 30' W. The downward bulge centered around 150 
          meters deep at the equator represents the equatorial 
          countercurrent.


North Atlantic Deep Water (NADW)

Progressing toward the northeast direction, the ledge of nearly uniform 
potential temperature on the theta-S relationship rotates clockwise, and the 
AAIW salinity minimum fills in. In the western regions, a distinct inversion 
of temperature is observed. This temperature maximum (i.e. cold AAIW above 
warmer NADW) disappears to the east. The salinity maximum associated with the 
upper NADW is gradually eroded toward east (see Figure 5, the station numbers 
increase eastward) with noisy interleaving approximately aligned along 
constant potential density surfaces.

The double oxygen maxima are observed at potential temperatures of about 
2.0°C and 3.5°C (Figure 6). This feature is absent near the western boundary 
and appears toward the middle of the Brazil Basin, suggesting an erosion of 
NADW by low-oxygen South Atlantic waters. There is a corresponding 'cutout" 
in the knee of the theta-S plots (located at about 2°C). The nutrients have 
minima that correspond to the double oxygen maxima, although their depth 
levels differ substantially. This may be due to the differing background 
vertical gradient upon which the perturbations lie (e.g. a linear gradient 
displaces the maximum of a Gaussian perturbation up the gradient). The double 
oxygen maxima have been noted by Wust, Reid and others, and appear to reflect 
the intensity of water mass formation at the respective levels of Labrador 
Sea Water and Denmark Strait Overflow Water.

There is a widespread silicate minimum beneath the AAIW maximum at about 1800 
db. Below, at a potential temperature of about 2.4°C, a weak relative maximum 
occurs that corresponds to the erosive mixing described above. The 
double-pronged structure of tracers in the tropical and equatorial Atlantic, 
with extrema appearing along the western boundary and the equator, is 
familiar as far back as the Meteor Expedition in the mid-1920's. It now has 
substantial dynamical motivation through the sink-source flows calculated by 
M. Kawase, F. Bryan and others.


Antarctic Bottom Water (AABW)

In the deeper regions of the Brazil Basin, the AABW appears as a weakly 
stratified water mass with weak tracer gradients through a depth of 1 km or 
more. The "lid" is heavily stratified with remarkable linear theta-property 
signature (see Figure 6). Here, and in the even more homogeneous eastern deep 
basins, one has a laboratory in which to study diapycnal mixing and vertical 
motion. Although logistics prevented us from conducting extensive surveys 
around the Romanche and Chain Fracture Zones, there is a need to know the 
rate and properties of the flow from the western into the eastern basins. 
Deep transports of 2 to 5 Sv predicted by box models (Schlitzer, JGR, 1987) 
would seemingly show intense circulation in these narrow passages, and need 
to be confirmed by direct observations.


Figure 4: The concentration of dissolved oxygen versus potential density 
          observed at various stations. The numbers indicate the station 
          numbers. The station numbers increase toward northeast; the 
          stations with numbers lower than 32 are located in the western 
          basin and those with greater than 32 are located in the eastern 
          basin.

Figure 5: The theta-salinity relationship observed at the SAVE Leg 1 
          stations. The numbers attached to the curves indicate the station 
          number. The station numbers increase northeastward, #11 being 
          located near the Brazil coast and #37 near the Liberia coast.

Figure 6: Potential temperature versus property plots for salinity, oxygen 
          and nutrient salts at the Brazil Basin stations, SAVE Leg 1. Note 
          double maxima features in the distribution of oxygen and nutrient 
          salts at about 2.0 and 3.5°C.



Data Tables and Plots
(R.T. Williams ODF/STS/SIO)


Most of the users of this preliminary report will be familiar with the 
techniques and methods used to acquire the data, for the most part identical 
with those employed in the TTO program. Calculated parameters have been 
generated from the same equations as used in the TTO final report.

Hydrographic data from Gerard casts is included with the rosette data in the 
report. The right column of the report gives the difference between the 
salinity from the 2 liter bottle mounted outside the Gerard barrel and the 
salinity from within the barrel. At the bottom of the station reports salt, 
oxygen, and/or nutrient values may occasionally be found without pressure or 
depth. These values have been considered suspect, and would not normally 
appear in the report; however, because the users of this report may be 
concerned with factors affecting the integrity of their shore based samples, 
the original values are reported. They may be keyed to the other data from 
the same level by subtracting 9000 from the sample number. There are other 
cases where missing oxygen and nutrients (and a "D" flag on a salinity) may 
indicate a bottle which was obviously leaking, a lanyard caught in a bottle 
lid, sampling error, or other problem about which additional documentation 
will be made available in the near future.

On the first station of leg 1, station 10 (9 stations were taken for 
inter-calibration prior to Knorr's arrival in Recife), neither the ship's 
precision depth recorder nor our rosette-mounted altimeter were working, so 
that bottom depth information is lacking. However, a small depth recorder on 
the bridge indicated a bottom at about 200 meters at the beginning of the 
cast. During the cast the bottom began to shoal rapidly, and it is my feeling 
that the deepest 4 or 5 bottles are all within a few meters of the bottom; 
that is, we were barely keeping the rosette out of the mud as the cast was 
brought up. By the end of the cast the depth was about 50 m. On the second 
station the altimeter was working so that the distance above bottom (dab) at 
maximum depth could be reported for the rosette cast. Without the ship's 12 
kHz equipment, the bottom depth and dab could not be reported for the Gerard 
casts. On all succeeding stations, the sonic depth and dab are reported for 
each deep cast in the heading of each station report, unless poor bottom 
conditions made the trace unreadable.



List of participants

Ship's Captain
            Richard Bowen - Woods Hole Oceanographic Institution

Chief Scientist
            Taro Takahashi
            Lamont-Doherty Geological Observatory

Co-chief Scientist
            Peter Rhines
            University of Washington

Lamont-Doherty Geological Observatory
            Michael T. Benjamin
            Richard P. Cember
            David W. Chipman Guy G. Mathieu

Princeton University
            Richard J. Rotter

Scripps Institution of Oceanography/ODF
            Marie-Claude Beaupre 
            James P. Costello 
            Timothy J. Field 
            Arthur W. Hester 
            Mary C. Johnson 
            Norma L Mantyla 
            Douglas M. Masten 
            Carl W. Mattson 
            James A. Wells 
            Robert T. Williams

Scripps Institution of Oceanography
            Peter K. Salameh

Texas A&M University
            Wilford D. Gardner

Woods Hole Oceanographic Institution
            Scot P. Birdwhistell 
            Lolita Surprenant
            
Brazilian Naval Observer
            Cpt. Emmanuel Bonfim de Jesus



CCHDO DATA PROCESSING NOTES

Date        Contact     Date Type  Summary 
----------  ----------  ---------  --------------------------------------
2011-04-08  Muus, Dave  BOT/SUM    Exchange, NetCDF, WOCE files online 
            Notes on Save Leg 1 rosette sample data.    EXPOCODE 316N19871123   
            110406/dm
            1. Temperature, salinities, oxygen and nutrients taken from ODF 
               data, whprpasave1, dated   
               Aug 25, 2005.
            2. CFCs and CO2 data merged from file SAVEsv.csv received from R. 
               Key  Dec 10,     2010.
               PCO2 values in file but no flags. Added flag 2 for all PCO2s.
            3. Station 16, Cast 1, Sample 16 684db: ODF deleted water samples 
               "Lanyard hangup?"        
                Salinity & oxygen high, nutrients low.
                SAVEsv.csv TCARBN 127 low, PCO2 785 low. Deleted.
            4. Deleted Station 24 Cast 3 Bottle 9 from SAVEsv.csv file. Cast 
                3 is Gerard cast, Bottle 9 
                is rosette bottle. Only sample values are CFCs.
            5. CTDTMP units ITS-68 not ITS-90.
            6. Station 41, Cast 1, Sample 32 Reversing Pressure 550db low. 
                Other values including 
                Reversing temperature look okay. Changed flag from 2 to 4.


