One possible explanation for this spectral 

 peak broadening is that an impulsive wind acted 

 over a local area and generated a transient in- 

 ertial motion. The interval that the wind stress 

 acted on the surface would have to have been 

 a sizeable fraction of the inertial period. There 

 are no wind observations available to support 

 this hypothesis. 



POST SEASON HYDROGRAPHIC DATA 



Two sections were occupied in the interim be- 

 tween emplacement and recovery of the in- 

 strumented arrays. The first (21-25 July), a 

 Labrador Sea section modified on the eastern 

 end to include an orthogonal traverse of the 

 West Greenland Current, was made immediately 

 after the instrumented arrays were set. The 

 second (3 August), an abbreviated standard sec- 

 tion Al, was completed just prior to recovery 

 of the instrumented arrays (See fig. 4 for loca- 

 tions). The vertical profiles of temperature and 

 salinity are displayed in figures 57 and 58. The 

 volume transport of the cold core of the Labra- 

 dor Current on the 21-25 July occupation was 

 1.65 X lO^m.Vsec. 



FALL HYDROGRAPHIC DATA 



Two sections were occupied on the fall cruise : 

 part of standard section A2 on 8 October and a 

 special section from 43-48N, 52-08W to 43-18N, 

 54-22W on 10 October (See fig. 5 for locations.). 

 The vertical profiles of temperature and salinity 

 are displayed in figures 59 and 60. The data were 

 not analyzed further. 



DIGITAL VS. ANALOG STD DATA 



An effort was made to compare STD data 

 read from the analog traces with that reduced 

 from the Digital Data Logger (DDL) records. 

 Values from a total of 775 levels selected from 

 29 different stations were used. The means and 

 standard deviations of the absolute values of the 

 differences between the analog values and the 

 DDL values were 



Temperature Salinity 



Mean of Differences 0.34C.° 0.091%o 



Standard Deviation 0.34C.° 0.090%o 



These differences were surprisingly large and 



may result, in part, from a depth error in the 



analog trace; the salinity pen of the analog 



trace was set to a zero depth while the under- 



water unit was soaking a short distance below 

 the sea surface. On the 29 stations considered, 

 this soaking depth ranged from 3 meters to 16 

 meters (It was necessary to keep the under- 

 water sensor at the greater depths during bad 

 weather.). 



To support the hypothesis that there was a 

 depth error on the analog trace, data from the 

 analog trace and the DDL were again compared. 

 This time the data were compared after adjust- 

 ing the analog trace levels for the soaking depth 

 of the underwater sensor. The resulting values 

 were: 



Temperature Salinity 



Means of Differences 0.13C.° 0.053%o 



Standard Deviation 0.12C.° 0.045%o 



This indicates that STD data read from the ana- 

 log trace may contain significant errors in depth. 

 These depth errors may be reduced if, at the 

 beginning of each cast, the pen of the STD ana- 

 log recorder is set to the actual soaking depth 

 of the underwater sensor rather than at zero. 



Even after adjusting for the depth error, sig- 

 nificant differences remain. The causes of these 

 are unknown, but it is more likely that errors 

 occurred in the frequency to millivolt conversion 

 and the graphic plotting of the deck unit rather 

 than in the analog to digital conversion and re- 

 cording of frequencies by the DDL and their 

 subsequent reduction by computer. 



CONCLUSIONS AND RECOMMENDATIONS 



The general agreement between the dynamic 

 topography relative to the 1000 decibar refer- 

 ence surface and the 3000 decibar reference sur- 

 face indicates that the use of the 1000 decibar 

 reference surface is probably satisfactory for 

 International Ice Patrol use. 



The large fluctuations in the volume transport 

 across standard section A3 compared to that 

 across standard section A2 implies that varia- 

 tions in the volume transport of the Labrador 

 Current along the eastern slope of the Grand 

 Banks may be caused by atmospheric or oceanic 

 changes that occur locally rather than farther 

 north along the Newfoundland or Labrador 

 coasts. 



Downwelling due to local wind stress was ob- 

 served to be one local influence that accelerates 

 the Labrador Current. An effort should be made 

 to discover other accelerating mechanisms that 

 could influence the Labrador Current. 



