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NOAA Technical Memorandum ERL PMEL-74
OBSERVATIONS OF CURRENTS, SURFACE WINDS AND BOTTOM PRESSURE IN SHELIKOF
STRAIT, AUTUMN 1984
A. T. RoachJ. D. SchumacherP. Stabeno
Pacific Marine Environmental LaboratorySeattle, WashingtonJuly 1987
UNITED STATESDEPARTMENT OF COMMERCE
Malcolm Baldrige,Secretary
NATIONAL OCEANIC ANDATMOSPHERIC ADMINISTRATION
Anthony J. Calio,Administrator
Environmental ResearchLaboratories
Vernon E. Derr,Director
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NOTICE
Mention of a commercial company or product does not constitutean endorsement by NOAA/ERL. Use of information from thispublication concerning proprietary products or the tests ofsuch products for publicity or advertising purposes is notauthorized.
Contribution No. 925 from NOAA/Pacific Marine Environmental Laboratory
For .ale by the Nalional lechnical Informalion Service. 5285 Pon Royal RoadSpringfield. VA 22161
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CONTENTS
ASSTRACT •••••••••••••••••••••••••••••••••••••••••••••••••••••••••••••• 1
1. INTRODUCTION •••••••••••••••••••••••••••••••••••••••••••••••••••••••••• 1
2. DATA AND METHODS ••••••••.•••••••••••••••••••..••••••••••••••••••••••.. 3
3. CIRCULATION ••••••••••••••••••••••••••••••••••••••••••••••••••••••••••• 5
A. Mean Conditions •••••••••••••••••••••••••••••••••••••••••••••••••• 5B. Current Characteristics •••••••••••••••••••••••••••••••••••••••••• 7
4. TIME SERIES SPECTRA••••••.••.••..•....•••.••••••••.•••.••••..••••.••.. 8
A. Currents ••••••••••••••.•....••••••••••••..•••••••..••...•••.•.••. 8B. Wind and Bottom Pressure Spectra •••••••••••••••••••••••••••••••• 10
5. TIME SERIES RELATIONS •••••••••••••••••••••••••••••••••••••••••••••••• 10
A. Currents ••••••••••••.••••••••.•••••••••••••••••••••••••••••••••• 10B. Current vs. Surface Wind •••••••••••••••••••••••••••••••••••••••• 12C. Currents va. Bottom Pressure •••••••••••••••••••••••••••••••••••• 13
6. SUMMAR.Y •••••••••••••••••••••••••••••••••••••••••••••••••••••••••••• •• 14
7. ACKNOWLEDGMENTS ••••••••..•.•••••.•.....••.••••••••••••••••..•••••.... 16
8. REFERENCES •..••••.•••••••••.•••••••••••••••...••....•••.•••••••••..•• 17
FIGURES .•.•••••••••.•••..•.•••.•...•••..•••••••••.••••••••..••••••••• 19
TABLES •••••••••••••••••••••.••.•••••••••••.•..••••••••..•.••.••••.••• 99
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OBSERVATIONS OF CURRENTS, SURFACE WINDSAND BOTTOM PRESSURE IN SHELIKOF STRAIT, AUTUMN 1984
A.T. RoachJ.D. Schumacher
P. Stabeno
ABSTRACT. An extensive array of current meters and bottompressure gauges was deployed in Shelikof Strait, Alaska, during1984/85 as part of the Fisheries Oceanography CoordinatedInvestigations (FOCI). FOCI is aimed at understanding thephysical and biological environment surrounding the early lifestages of the Pacific pollock (theragra chalcogramma). Thesedata, as well as calculated surface wind time series, wereanalyzed to investigate the influence of the Alaska CoastalCurrent (ACC) in this region. The ACC induced a strong mean flow(IS to 25 cm/s) during this season concentrated along the AlaskaPeninsula on the northern side of the Strait. Outside theinfluence of the ACC, mean currents were weak (5-8 cm/s). Thishighly variable flow bifurcated in the vicinity of the SemidiIslands, with 75% of the ACC volume flux flowing seaward out of adeep (200+m) sea valley which meets the shelf break at a sillsouthwest of Kodiak Island. This strong outflow can induce anestuarine type circulation through entrainment of bottom watercausing a mean inflow at depth. The remainder of the flowcontinues along the Alaska Peninsula. The currents were generallywell correlated in the vertical at each mooring, while thehorizontal correlations were weak, indicating the horizontalspatial scales of coherence were less than the 8 to 15 km mooringseparation. Surface winds from a location near the Barren Islands(200 km north of the Strait) showed the strongest relation tocurrents and transport. There was an indication that the windsdrove the pressure differences and thereby the currents, as therewas a significant correlation between bottom pressure differencesand currents.
1. INTRODUCTION
Fisheries-Oceanography Coordinated Investigations (FOCI) is a multi-year
study of the physical and biological environments surrounding the early life
stages of the Alaska Pollock (theragra chalcogramma) in Shelikof Strait,
Alaska. FOCI is conducted jointly by scientists at Pacific Marine
Environmental Laboratory and the Northwest and Alaska Fisheries Center in
Seattle, Washington. This memo presents analysis of current, bottom pressure
and surface wind time series from the winter of 1984/85.
Shelikof Strait is a region of complex topography (Fig. 1). The dominant
bathymetric feature is a deep sea valley which starts at the north end of
Kodiak Island and follows the axis of the Strait until it turns sharply
seaward east of the Semidi Islands, becoming orthogonal to the shelf break.
The sea valley ends at a 200 meter sill southwest of Kodiak Island. Shelikof
Strait is bounded by the mountainous Alaska Peninsula to the north and the
rugged Kodiak Island plateau to the south, both of which can have effects on
the local winds. The regional winds are strong and variable due to intense
cyclones crossing the North Pacific into the Gulf of Alaska. Large scale low
pressure systems lying southwest of Kodiak Island can cause regions of strong
convergence through the interaction of low-level, down gradient winds in the
Strait with the onshore geostrophic flow southwest of Kodiak Island (Macklin,
1984). The high variability of the wind field precludes areas of consistent
coastal convergence or divergence such as exist farther to the northeast or
southwest, respectively (Schumacher and Reed, 1986).
The Alaskan Coastal Current (ACC) enters Shelikof Strait primarily
through Kennedy Entrance south of Cook Inlet (Reed et al., 1980). The ACC
provides a source of low salinity water resulting from the large (23,000 m3 /s)
line source of freshwater input around the perimeter of the Gulf of Alaska
(Royer, 1979, 1982). This westward flowing current entrains slope water,
which is warmer in winter than the ACC water, before entering the Strait
(Schumacher et al., 1979). Flow bifurcates near the Semidi Islands, with one
branch continuing westward along the Alaska Peninsula and the other seaward
through the sea valley (Schumacher and Reed, 1986).
Deep slope water is the source of saline water at the southern end of the
sea valley, leading Reed et al. (1986) to use an estuarine-like model of
circulation to characterize this area. The warm, relatively fresh upper layer
flowing steadily southwestward overlies a cold and salty lower layer that
periodically reverses. My~ak et al. (1981) presented a seasonal analysis of
2
the variance for three current meter records from Shelikof Strait in the fall
and winter of 1976/77. They argued that the 2.5- to 5-day component of the
fluctuating flow was due to the baroclinic instability of the mean
southwestward flow.
This report describes the oceanographic conditions in and around Shelikof
Strait, Alaska during the fall of 1984. The basic statistics and time series
plots, as well as kinetic energy spectra, of all variables for the 34 current
meter, 4 surface wind, and 6 bottom pressure records are presented. In
addition, graphic representations of harmonic analyses for tidal currents and
of the distribution of variance by frequency band are discussed. Time series
relations are shown through correlation matrices and schematic diagrams of the
coherence squared of currents across transport sections. In the summary, the
major features of the circulation and volume transport through the Strait are
listed and questions for further study are posed.
2. DATA AND METHODS
We present a statistical analysis of the current meter records, bottom
pressure gauge records and surface winds spanning the period 25 Aug 1984 to 12
Jan 1985 (Table 1). The 34 current meters deployed were organized into 3
cross-sectional lines or sections (Figs. 1 and 2). Section 11 spanned the
Strait between Cape Kekurnoi and Kodiak Island (Moorings 1, 2, and 3), Section
12 contained the meters from moorings 4, 5, and 6 between Sutwick Island and
the Semidi Islands on the shallow continental shelf, while Section 13
(Moorings 7, 8, and 9) spanned the sea valley from the Semidis to Chirikof
Island (Figs. 3-5). These sections measure volume transport through Shelikof
Strait; beginning at Section 11 where the highest concentrations of pollock
eggs are found, then downstream either along the Alaska Peninsula (Section 12)
or seaward out of the sea valley (Section 13).
3
The current meters were Aanderaa RCM-4 instruments deployed on taut-wire
moorings. Six of these moorings (1, 3, 4, 6, 7, 9), located on the sides of
the transport sections, had Aanderaa bottom pressure gauges. All the
instruments were recovered and provided a raw time series of hourly samples,
except for the 26 m record from Mooring #2 which had faulty velocity data.
Data were smoothed using a 35-hour Lanczos filter with a 10% cosine squared
taper, and resampled at 6 hourly intervals. This filter passes more than 99%
of the amplitude at periods of greater than 55 hours, 50% at 35 hours and less
than 0.5% at 25 hours, effectively removing the tides. The pressure gauge
records were similarly filtered. Time series of the observed variables are
shown in Figs. 6-41. Detrended pressure gauge series were used to create
series representing the pressure differences both along and across the
continental shelf by subtracting one series from another. Figures 42 and 43
show the alongshelf and cross shelf pressure difference series respectively.
Other series of importance to this report are the surface and bottom transport
ser1es. The low-pass filtered, principal axis speed components for all the
records from 56 meters and above in each of the sections were multiplied by a
representative area and summed to provide an estimate of the volume transport
in the surface layer (Figs. 44-46). Similarly, the bottom records yielded a
lower layer transport estimate. Note that the upper layer is approximately
half way between the 56 m record and the one immediately below it (Fig. 2).
Tables 2, 3, and 4 present the vector mean flow, RMS error, principal
axes, variance and variance ellipse statistics for current meter records from
Sections 1, 2, and 3, respectively. The nomenclature used in referencing
instruments 1S the mooring number followed by the instruments' sequential
number from the surface and depth. 'Thus, the instrument on Section 1 with
faulty velocity data was 2 1/26. Table 5 presents similar statistics for the
surface winds, bottom and surface transports, and bottom pressure gauge
records.
4
Spectra were computed by removing the mean from each record, uSing a 10%
cosine taper and then dividing the variances by 0.875 to preserve the variance
lost by that taper. The Fourier Transform of each time series was boxcar
averaged to produce a spectrum such that the sum of the variances over all
frequencies equaled the total variance (Pearson, 1981). The band averaged
spectral energy for all nine moorings was also computed to get an overall
picture of the frequency distribution which would have been difficult to
ascertain from the spectra themselves. The bands used are detailed in
Table 17.
Four time series of gradient winds (Fig. 47) were generated from surface
atmospheric pressure fields using the METLIB package of programs. Surface
winds were generated from gradient winds using a rotation of the wind
direction by 15 degrees to the left and a 30% reduction in magnitude (Overland
et al., 1980). Synthetic winds may not replicate the small scale spatial
variability of the actual winds (Royer, 1981; Luick, Royer and Johnson,
1987). The wind series near the Barren Islands (northeast of Kodiak Island)
is designated as "BA", Shelikof Strait is "SH" and "SE" denotes the wind
series near the Semidi Islands. There are no observed wind time series
available.
3. CIRCULATION
A. Mean Conditions
Mean flow was in the along-channel direction at all three sections, with
the exceptions of Mooring #5 and some of the deeper records with weak
currents. Sections 1 and 3 were qualitatively similar with strong mean
outflow on the right hand side (RHS) of the Section (looking downstream along
the major axis) and weak and variable or reversing currents at depth on the
left hand side. The alongshore mean speeds at moorings 1 and 2 exceeded
20 cm/s alongshore in the surface layer, and were reduced to less than 6 cm/s
5
----- - ----
at a nominal depth of 200 meters (Fig. 48). Most of the current variance was
contained in the alongshore direction for Mooring 1, while the variance
ellipse was nearly circular for Mooring 2. Similar mean speeds were present
in the surface records at Moorings 7 and 8 on the RHS of Section 3
(Fig. 50). Currents at moorings 3 and 9 had weak and variable surface flow
overlying a mean inflow of 7 and 3 cm/s below 150 m, respectively.
The mean currents at Section 2 (Fig. 49) were weaker (8-10 cm/s) above
56 m than those at the sections across the sea valley. There was no
significant flow at 6_3/75 in the lower water column. All records on
Section 2 were nearly circularly polarized and there was a consistent decrease
of variance with depth at all locations.
The transport means suggested 70 to 80% of the water which flowed through
Shelikof Strait (Section 1) exited through the sea valley (Section 3). The
estimated mean transport through Section 1 was 0.82 Sverdrups
(1 Sv = 10 6 m3 /s), while 0.26 Sv flowed through Section 2 and 0.68 Sv through
Section 3. The transports balance to within 15%. The imbalance may be due to
inaccuracies in the transport calculation or failure of these sections to
include all significant flows in this region. In particular, a moderate 8 to
10 cm/s flow over the shallow shelf region southwest of Kodiak Island and east
of Mooring 9 could add about 0.1 Sv to the balance. Satellite tracked
drifters have gone between the Semidi Islands, indicating that area as one of
possible importance to the regional flow. A strong (>25 cm/s) flow through
the Islands, however, would contribute less than 0.05 Sv to the transport
balance. Most of the volume transport was concentrated in the surface layers;
65% at Section 1, 92% at Section 2 and 75% at Section 3.
Bottom pressure recorders were placed on either side of the Strait to
examine the mesoscale dynamics. Since the mean pressures are only indicative
of the instruments' depth, the statistic of most interest is the variance of
each record. The two series with the highest variances were on Section 2
6
(Moorings 4 and 6), while the least variable bottom pressure series was on
Mooring 9 (Table 5 and Fig. 41). Even though the mean flow through Section 3
was double that of Section 2, variability was four times greater in the
coastal region than over the sea valley.
The mean speeds for the along-channel surface winds showed a transition
from winds favoring coastal convergence near the Barren Islands and in
Shelikof Strait to statistically insignificant winds near the Semidi Islands
(Table 5). This transition results from the location of cyclone trajectories
in the Gulf of Alaska (Schumacher and Reed, 1986). These surface winds do not
reflect the orographic effects of the local winds, which can be accelerated
along the Strait and through gaps in the coastal mountains (Macklin, 1984).
B. Current Characteristics
Tidal currents contain a significant amount of kinetic energy in Shelikof
Strait. Selected tidal constituents were estimated from eight 29-day tidal
harmonic analyses of hourly current time series and are shown in Figs. 51-
53. The tidal currents were mostly semi-diurnal with M2 speeds averaging
15 cm/s at Moorings 1 and 2, reaching 20 cm/s at Mooring 3. The same
constituent had speeds of about 30 cm/s at Moorings 7 and 8 and 35 cm/s at
Mooring 9. Thus, both sections showed the strongest tidal currents on the
left hand side of the sea valley. There was less variability at Section 2,
with average M2 speeds of 20 cm/s. Moorings 6, 7 and 9 showed subsurface
maximums, which may be associated with an internal tide.
In Section 1, upper layer subtidal currents seldom reversed at Moorings 1
and 2. Reversals of up to nine days with speeds over 50 cm/s were common at
Mooring 3. Lower layer currents showed similar differences with mean outflow
at Moorings 1 and 2 and inflow on the Kodiak Island side of the Strait.
Currents on the sides of the Strait were predominantly along the major axis,
while currents at the center mooring (2) had significant rotary energy.
7
Upper layer currents at Section 3 were qualitatively similar to
Section 1. The flow was rectilinear on both sides of the sea valley and the
strong outflow which seldom reversed was on the right side of the Section
(Moorings 7 and 8). There were fewer reversals in the surface layers at
Mooring 9 than Mooring 3, but there was significant inflow in the lower layers
of Section 3. The autumn baroclinic spinup (Royer, 1982; Reed and Schumacher,
1981) was most apparent in current and salinity observations from Mooring 7.
The outflowing currents doubled in speed and salinity decreased by 1 ppt
during September through mid-October.
The mean current was generally weaker at Section 2 than at the Sections
across the sea valley. At Moorings 5 and 6 there was an autumn spin up with
increased alongshe1f speeds and reduced salinity which occurred simultaneously
with the transition at Mooring 7. Currents at Mooring 4 showed little effect
from the transition, remaining primarily alongshore, while currents at
Moorings 5 and 6 were directed offshore. This divergence was present after
the transition and may be a persistent feature.
4. TIME SERIES SPECTRA
A. Currents
The variance preserving spectra for all 34 current meters, 4 surface wind
and 6 pressure gauge records are presented in Figs. 54-65. In general,
fluctuations of the along-channel current were significantly larger than the
across-channel component at the edges of the sea valley (Moorings 1, 3, 7,
9). Current fluctuations were most energetic at the surface, with the notable
exception of Mooring 3. At that location (and to a lesser extent, at
Mooring 8), the variance increased in the deepest layer (Fig. 67). Comparison
with the band averaged frequency distribution shows this increase in variance
at depth was iri the diurnal~and two- to five-day bands (Fig. 68). There was a
60% decrease 1n total variance between the 26-m and 56-m records at
Mooring 6.
8
Spectra from Section 1 show the majority of kinetic energy at Moorings 1
and 3 to be along the major axis. There was a shift from low frequency energy
at the surface to higher frequencies at the bottom for both locations. There
was a surface intensification of the high frequency signal at Mooring 1, while
mid-frequency energy (five to ten days) increased till mid-depth then
decreased. There was, however, a consistent eight-day signal at all depths at
that location. The cross-channel component at Mooring 3 showed a uniform
distribution over the low frequencies separated from a significant
mid-frequency band of five to eight days. The spectra from Mooring 2 showed
the division of variance between the 220 0 T and 3l0 o T components to be nearly
equal. There was a concentration of energy in a cross-channel peak at three
days, whereas the energy centered at eight days contained an equal amount of
variance in both components.
Spectral peaks for the along- and across-channel components for Section 2
(250 0 T and 340 o T, respectively) were usually well separated. Often a strong
signal in one component meant less energy in the orthogonal component (e.g.
the twelve day peak at 5_1/26, Fig. 58). There was more along-channel energy
at low frequencies, especially at Mooring 6 (Fig. 59).
Along sea valley energy dominated all records from Section 3, except in
the surface layer of Mooring 8. The currents on the sides of the sea valley
had strong low frequency signals with a subsidiary peak at eight days.
Mooring 8_4/205 (Fig. 61) showed a four-day peak which may be associated with
inflow events. Section 3 had a lower percentage of its variance at higher
frequencies than Section 1, even though their spectral structures were similar
(Figs. 68, 70).
At the moorings in the center of each section, the currents are best
described using rotary spectra (Fig. 66). At periods greater than five days,
the current energy at Mooring 2 was equally divided between clockwise and
counterclockwise components. At shorter periods, there was significantly more
9
counterclockwise energy in the upper layer and more clockwise energy 1n the
lower layer. Current behavior at Mooring 8 was similar to Mooring 2 at depth,
but had significantly more counterclockwise energy over most periods near the
surface. Mooring 5 had no consistent pattern of rotational energy.
B. Wind and Bottom Pressure Spectra
The onshore/offshore component of the surface winds was consistently more
energetic than the alongshore component, except at a period of eight days
(Fig. 63). There was a significant alongshelf peak at that period in each of
the four wind series. There was a consistent low frequency signal (centered
at 17 days) in the cross-shelf component at all locations. The bottom
pressure gauges had a bimodal structure with the primary peak at twenty days,
which held most of the energy, and a secondary peak at five to six days
(Fig. 65).
5. TIME SERIES RELATIONS
A. Currents
Tables 6 to 16 present correlation matrices for current and transport
series versus surface winds, bottom pressures, and bottom pressure
differences. In general, correlations were greatest in the vertical, but weak
or insignificant across a section. For example, currents were correlated
within Mooring 2, but virtually no correlation existed across the strait
(Table 6). At Mooring 1 there was a tendency for the surface current to be
decoupled from the bottom current. The decoupling was more complete at
Mooring 3, where the currents above 106 m were well related to each other, as
were those below 165 m. Those two groups, however, were not significantly
correlated with each other (95% level). This surface-to-bottom difference was
also suggested in the time scale estimates (Fig. 71) (Allen and Kundu,
1978).
10
Correlations between the currents in Section 2 (Table 7) were generally
weaker than those in Section 1. The highest correlations in the vertical
existed at Mooring 6, but may have been due to less vertical separation of the
meters.
The greatest cross-channel correlations were found between Moorings 7 and
8 in Section 3 (Table 8). The correlations between currents in the upper
layer at Mooring 7 and 9 were negative, while currents in the bottom layers of
7 and 9 were positively correlated. This relation is interesting since
correlations were not significant between Moorings 8 and 9. The negative
correlations suggest the presence of eddy-like features (such as those found
in satellite imagery), while the positive correlations and time scale
differences imply such features are restricted to the upper water column.
Most of the time scales are comparable at about 100 hours, except those at the
bottom of Mooring 9, which dropped to half that value (Fig. 71).
At most frequencies, coherence squared estimates showed similar results
to those seen in the correlations; strong coherence in the vertical, weak or
non-existent coherence in the horizontal (Figs. 72-74). At Section 1, the
strongest coherences in the vertical were at the shortest periods. At longer
periods, the bottom flow decoup1ed from the surface, especially at the sides
of the channel. Diagrams combining Sections 2 and 3 showed more structure
(Figs. 75-77). Coherence was weak at the shortest period and, similar to
results from Section 1, the bottom current decoup1ed from the surface at the
longest period. There was coherence in the horizontal current structure ~n
the upper 106 m from mooring 6 to 8, particularly at about 17 days.
Correlations between transports are given in Table 9. At each section,
the surface and bottom transports were well correlated. We note that
transports were more highly correlated than currents because transport ~s mass
flux, a conservative property. Section 2 was best correlated with the
transport estimated upstream at Section 1. The lack of correlation between
11
Correlations between the currents in Section 2 (Table 7) were generally
weaker than those in Section 1. The highest correlations in the vertical
existed at Mooring 6, but may have been due to less vertical separation of the
meters.
The greatest cross-channel correlations were found between Moorings 7 and
8 in Section 3 (Table 8). The correlations between currents in the upper
layer at Mooring 7 and 9 were negative, while currents in the bottom layers of
7 and 9 were positively correlated. This relation is interesting since
correlations were not significant between Moorings 8 and 9. The negative
correlations suggest the presence of eddy-like features (such as those found
in satellite imagery), while the positive correlations and time scale
differences imply such features are restricted to the upper water column.
Most of the time scales are comparable at about 100 hours, except those at the
bottom of Mooring 9, which dropped to half that value (Fig. 71).
At most frequencies, coherence squared estimates showed similar results
to those seen in the correlations; strong coherence in the vertical, weak or
non-existent coherence in the horizontal (Figs. 72-74). At Section 1, the
strongest coherences in the vertical were at the shortest periods. At longer
periods, the bottom flow decoup1ed from the surface, especially at the sides
of the channel. Diagrams combining Sections 2 and 3 showed more structure
(Figs. 75-77). Coherence was weak at the shortest period and, similar to
results from Section 1, the bottom current decoup1ed from the surface at the
longest period. There was coherence in the horizontal current structure ~n
the upper 106 m from mooring 6 to 8, particularly at about 17 days.
Correlations between transports are given in Table 9. At each section,
the surface and bottom transports were well correlated. We note that
transports were more highly correlated than currents because transport ~s mass
flux, a conservative property. Section 2 was best correlated with the
transport estimated upstream at Section 1. The lack of correlation between
11
Sections 2 and 3 may have resulted from the combined (baroclini~and
barotropic) current components at Section 1 becoming separated downstream.
That is, the barotropic component may have followed the sea valley, while
surface intensified baroclinic flow continued through Section 2.
Ten-day averages of surface, bottom and total transport for each section
are shown in Fig. 78. In the surface layer, transport was comparable at
Sections 1 and 3 with concurrent maxima. The maxima at Section 2 lagged those
at the other two sections. Bottom transport was greatest at Section 1 except
for a short period in November. Since the depth at which upper and lower
layers were divided was not exactly the same at each section, comparison of
surface or bottom transport between sections is more difficult than examining
total transport. There were three periods, separated by weak flow, when total
transport at Section 1 or 3 exceeded 1 Sv. Transport at Section 1 exceeded
combined flow at 2 and 3 for only three of the 10-day averages. During two
20-day periods outflow at 3 alone exceeded flow at 1. Total transport at
Section 2 increased slowly to its maximum and lagged rapid increases in
transport at Sections 1 and 3.
B. Current vs. Surface Wind
Major axis currents showed their highest correlation with the Barren
Islands surface wind series, several hundred kilometers to the north.
Table 10 shows the maximum correlations and associated lags between each of
these time series. Their relationships varied strongly as a function of wind
angle, but stayed constant for 20-30° around the aXiS of maXimum
correlation. For most of the current series, the wind component for maXimum
correlation lay in the along channel/onshore quadrant. It appeared that local
winds played a minor role in current fluctuations during this study, but that
larger scale atmospheric circulation had an important effect.
r~
12 ,t.
I
Sections 2 and 3 may have resulted from the combined (baroclini~and
barotropic) current components at Section 1 becoming separated downstream.
That is, the barotropic component may have followed the sea valley, while
surface intensified baroclinic flow continued through Section 2.
Ten-day averages of surface, bottom and total transport for each section
are shown in Fig. 78. In the surface layer, transport was comparable at
Sections 1 and 3 with concurrent maxima. The maxima at Section 2 lagged those
at the other two sections. Bottom transport was greatest at Section 1 except
for a short period in November. Since the depth at which upper and lower
layers were divided was not exactly the same at each section, comparison of
surface or bottom transport between sections is more difficult than examining
total transport. There were three periods, separated by weak flow, when total
transport at Section 1 or 3 exceeded 1 Sv. Transport at Section 1 exceeded
combined flow at 2 and 3 for only three of the 10-day averages. During two
20-day periods outflow at 3 alone exceeded flow at 1. Total transport at
Section 2 increased slowly to its maximum and lagged rapid increases in
transport at Sections 1 and 3.
B. Current vs. Surface Wind
Major axis currents showed their highest correlation with the Barren
Islands surface wind series, several hundred kilometers to the north.
Table 10 shows the maximum correlations and associated lags between each of
these time series. Their relationships varied strongly as a function of wind
angle, but stayed constant for 20-30° around the aXiS of maXimum
correlation. For most of the current series, the wind component for maXimum
correlation lay in the along channel/onshore quadrant. It appeared that local
winds played a minor role in current fluctuations during this study, but that
larger scale atmospheric circulation had an important effect.
r~
12 ,t.
I
The highest correlation of the surface winds at each mooring was with the
bottom currents, except at Mooring 1. The amount of variance explained by the
wind in the deep currents was 40%. The corresponding relationship with the
more energetic surface currents was weak. The highest correlations were
between the onshore component of the wind and Moorings 7 and 8.
Transports were better correlated with winds than were currents, with
Section 3 yielding the best results (Table 11). Like the currents, the
strongest correlations were with the onshore component of the wind. We found
the strongest correlation with the winds rotated 40° clockwise from the
orographic axis, which is in agreement with recent findings from comparisons
of measured winds and gradient winds in the Northern Gulf of Alaska (Luick
et al., 1987).
C. Currents vs. Bottom Pressure
Correlations between currents versus along- and across-channel pressure
differences are presented in Tables 12 to 14. The correlations between the
pressure difference series themselves are in Table 15. In the sea valley, the
largest correlations were with currents on the right side, while there was
little or no correlation with currents on the left side. The pressure
differences which incorporated the pressure series from Mooring 1 were
negatively correlated with all current series except at Mooring 9. These
relations were strongest at Mooring 6, 7, and 8, although Mooring 2 showed
some relation to PGI-PG4. The best overall correlation was with the cross
shelf difference of PG6-PG9, which had high coefficients with all records
except currents at Moorings 3, 5, and 9. That cross-shelf pressure difference
accounted for up to 60% of the variance in the bottom currents on the right
hand side of Section 3. Section 1 current was best correlated with the
pressure differences measured at Section 3, while currents at the other two
sections were best correlated with the pressure differences measured
locally.
13
Transport versus bottom pressure differences (Table 16) echo the results
above. Transports through Section 2 and 3 were best correlated with local
across-shelf differences, while transport at Section 1 was only weakly
correlated with its local pressure. All along-channel pressure differences
had negative correlation to transport, except at the bottom layer of
Section 3.
6. SUMMARY
Analysis of current, bottom pressure and surface wind time series from 25
August 1984 to 12 January 1985 resulted in the following observations:
1) The non-locally forced Alaska Coastal Current (ACC) induced a strong
mean flow. Currents in the upper 100 m on the northern side of Shelikof
Strait (Section 1) were 15 to 25 cm/s toward the southwest; on the northern
side of the section between Sutwick and the Semidi Islands (Section 2) they
were 7 to 12 cm/s directed along the Alaska Peninsula; and on the western side
of the sea valley between Semidi and Chirikof Islands (Section 3) they were 10
to 25 cm/s seaward. Outside the direct influence of the ACC, mean currents
were weak. On the southern side of Shelikof Strait, mean currents in the
upper water column did not differ significantly from zero. On the southern
side of Section 2 flow was 1 to 6 cm/s, and on the eastern side of Section 3,
a 4- to 6-cm/s current flowed seaward. Entrainment of bottom water into the
ACC may have been responsible for the statistically significant mean
estuarine-like flow (Reed et al., 1986) into the sea valley, which was about
3 cm/s on the eastern side of Section 3 and 5 to 7 cm/s on the southern side
of the Strait proper. The current observations support earlier studies
(Schumacher and Reed, 1986) which suggest the ACC is bifurcated in the
vicinity of the Semidi Islands, one branch flowing seawards and the other
along the Peninsula.
14
2) The mean transports were 0.68 Sv and 0.26 Sv, flowing seaward and
along the peninsula, respectively. Using these transport values, we estimate
approximately 75% of the ACe volume flux flows seaward through the sea
valley. Autumn baroc1inic spin up was evident in transport and salinity time
series.
3) Fluctuations in currents were generally well correlated in the
vertical, particularly in the upper 106 m, while in the horizontal, they were
either weakly or insignificantly correlated. Scales of horizontal correlation
and coherence were less than the 8- to 15-km mooring separation. An exception
to the low coherences in the horizontal was observed between currents at
moorings 6 and 7, near the Semidi Islands, where coherence s~uared estimates
of about 0.60 existed at several frequencies.
4) Although a significant part of current and transport fluctuations
could be accounted for by surface winds, the nature of this relation is
unclear. The best relations between surface winds and currents were with a
wind 200 kilometers northeast and rotated 20° to 60° clockwise from its
orographic axis.
5) There was a significant correlation between the across channel
pressure difference and the currents (or transports). There was an indication
that the winds drove the pressure differences and thereby the currents. The
cross-channel pressure difference at Section 3 was the series that was best
correlated with the wind fluctuations along 245°T.
The 10-day averages of transport opened up many areas for further
investigation. First, there were three main peaks in the averages. The
complete record (340 days) at Section 3 will be examined to see if this
pattern continued, and if it was due to convergence and divergence of the ACC
by winds or by other mechanisms. A more careful examination of the apparent
lag of the transport at Section 2 is necessary to determine whether it was
significant and if so what caused it. The combined outflow through Section 2
15
and 3 exceeded the flow through Section 1 for most of the 10-dayperiods.
When transport through Section 1 exceeded that through 2 and 3 there followed
shortly thereafter a large excess through 2 and 3. Is the transport through
Sections 2 and 3 consistently larger than that through 1, except for short
periods where there is a piling up of water due to atmospheric conditions
followed by a relaxation?
7. ACKNOWLEDGMENTS
We wish to thank the many people who assisted in the field operations,
data processing and discussions. In particular, we thank the complements of
the NOAA ships FAIRWEATHER and DISCOVERER and the USCG ship FIREBUSH. Special
thanks to T. Jackson and W. Parker who prepared, deployed and recovered all
the equipment. L. Long and P. Proctor processed the time series with great
care and patience. Discussions with R. Reed, L. Incze, and R. Romea were
extremely helpful. This publication 1S a contribution to the Fisheries
Oceanography Coordinated Investigations (FOCI) of NOAA.
16
8. REFERENCES
Allen, J.S. and P.K. Kundu, 1978: On the momentum, vorticity, and mass
balance 1n the oregon shelf, J. Phgs. Ocean., Jan 78, pp. 13-27.
Luick, J.L., T.C. Royer, and W.P. Johnson, 1987: Coastal atmospheric forcing
in the northern Gulf of Alaska. J. Geophgs. Res., 92(C4), 3841-3848.
Macklin,S.A., J.E. Overland, and J.P. Walker, 1984: Low-level gap winds in
Shelikof Strait. 3rd Technical Conference on Meteorology of the Coastal
Zone. Amer. Meteor Soc. 9-13 January, 1984, Miami FL. Paper JC-7.4.
Muench,R.D., H.O. Mofjeld, and R.L. Charnell, 1978: Oceanographic conditions
in lower Cook Inlet; spring and summer 1973. J. Geophgs. Res., 83,
5090-5098.
Muench, R.D., J.D. Schumacher, 1980: Physical oceanographic and
meteorological conditions 1n the northwest Gulf of Alaska. NOAA Tech.
Memo. ERL-PMEL-22, 147 pp.
Mysak L., R.D. Muench, and J.D. Schumacher, 1981: Baroclinic instability in a
downstream varying channel: Shelikof Strait, Alaska. J. Phgs.
Oceanogr., 11(7), 950-969.
Overland, J.E., R.A. Brown and C.D. Mobley, 1980: METLIB--A program library
for calculating and plotting marine boundary layer wind fields. NOAA
Tech. Memo. ERL-PMEL-20, 82 pp.
Pearson, C.A., 1981: Guide to R2D2-Rapid retrieval data display. NOAA Tech.
Memo. ERL-PMEL-29, 144 pp.
Reed, R.K., R.D. Muench and J.D. Schumacher, 1980: On baroclinic transport of
the Alaskan Stream near Kodiak Island. Deep-Sea Res., 27, 509-523.
Reed, R. K. and J.D.Schumacher, 1981: Sea level variations in relation to
coastal flow around the Gulf of Alaska. J. Geophgs. Res., 86(7),
6543-6546.
17
------- --------- ------
Reed, R.K., J.D. Schumacher, and L.S. Incze, 1986: Water properties and
circulation in Shelikof Strait, Alaska during 1985. NOAA Tech. Memo.
ERL-PMEL-68, 35 pp.
Royer, T.C., 1979: On the effect of precipitation and runoff on coastal
circulation in the Gulf of Alaska. J. Phys. Oceanogr., 9, 555-563.
Royer, T.C., 1981: Baroclinic transport in the Gulf of Alaska. 1. Seasonal
variations of the Alaska Current. J. Mar. Res., 39(2), 239-250.
Royer, T.C. ,1982: Coastal fresh water discharge in the northeast Pacific.
J. Geophys. Res., 87, 2017-2021.
Schumacher, J.D. and R.K. Reed, 1986: On the Alaska Coastal Current in the
Western Gulf of Alaska, J. Geophys. Res. 91, C8, pp. 9655-9661.
Schumacher, J.D., R.K. Reed, M. Grigsby, and D. Dreves, 1979: Circulation and
hydrography near Kodiak Island, September to November, 1977. NOAA Tech.
Memo. ERL PMEL-13, pp. 49.
18
---- -~~---~
FIGURES
19
r-------------------------.------r,.....-------,::-r1T'""""T"600Nl600 W 150° 140°
o SO 100I I I I I
KILOMETERS
Isr
Figure l.--Location figure showing the study region, location of the currentmeter moorings and geographical place names.
20
u(]JTRANSPORT TRANSPORT TRANSPORTSECTION #1 SECTION #2 SECTION #3
MOORING 1 2 3 4 5 6 7 8 9
DEPTH (m)II 1111
* * *26 ~c:::J P P ~c:::J P P ~c:::J P P
56 ~~ P P ~c:::::J P P ~c:::::J P P
75 P
106 ~c:::::J P P P ~c:::::J
1 21 P P
165 1c:::J P P168 P185 ~c:::J
220 P rP P
240 ~c:::::J
BOTTOM DEPTH 255 235 235 70 115 85 195 215 180.(meters)
***II
1111
No speed data for 26 meter instrumentRotor fouling after 85 191
Meter failure after 85 094Tape failure after 85 012
Figure 2.--Schematic of the location of the current meters for each of themoorings, showing the division into transport sections and the coverageof the water column. Note that this figure is not to scale.
21
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Fig
ure
4l.
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lot
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tom
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rds,
The
ho
rizo
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ure
42
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serie
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lots
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ren
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serie
sg
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ate
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s.T
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efo
ur
are
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own
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43
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5
Fig
ure
44
.--T
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serie
so
fin
teg
rate
dtr
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ecti
on
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ths
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eb
otto
mse
rie
sis
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ing
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rds
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secti
on
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Fig
ure
2).
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lue
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its
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103
m3/s
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Fig
ure
45
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2.
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84
84
84
84
84
85
Fig
ure
46
.--S
ame
asF
igu
re44
A,
exce
pt
for
Secti
on
#3
.
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IDI
SM
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84
84
84
84
84
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Fig
ure
47
.--S
tick
vecto
rp
lots
of
the
geo
stro
ph
icw
ind
seri
es
gen
era
ted
from
surf
ace
atm
osp
her
icp
ress
ure
an
aly
ses.
The
vert
ical
ax
isis
dir
ecte
dal
on
gth
eA
lask
aP
en
insu
laat
225
T(o
cean
og
rap
hic
dir
ecti
on
al
con
ven
tio
n)
and
the
vert
ical
scale
isin
mete
rs/s
eco
nd
.
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dia
kIs
lan
dA
lask
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enin
sula
20km
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oi
,(i
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RE
NT
SPEE
DS
(cm
/s)
Sect
ion
#I:
She
likof
Str
ait
Maj
orA
xis
=22
00T
Fig
ure
48
.--M
ean
cu
rren
tsp
eed
sp
lott
ed
ona
cro
ss-s
ecti
on
al
plo
to
fth
ein
stru
men
tsfo
rS
ecti
on
#1
.T
hesp
eed
sare
incm
/san
dd
irecte
dal
on
gth
em
ajo
rax
isas
no
ted
onth
efi
gu
re.
An
aste
risk
ind
icate
sth
ere
po
rted
val
ue
do
esn
ot
exce
edth
eRM
Serr
or
for
that
locati
on
.
Agh
iyuk
Is.
Sem
idi
Is.
Sut
wik
Is.
Ala
skan
Pen
.
10km
20
I
MEA
NC
UR
RE
NT
SPEE
DS
(cm
/s)
Sect
ion
#2:
shel
fne
arSe
mid
iIs
land
sM
ajor
Axi
s=
2500
T
oI
JI
iI
>
100
Fig
ure
49
.--S
ame
asF
igu
re4
8,
exce
pt
for
Secti
on
#2
.
Ch
irik
of
Isla
ndS
emid
iIs
land
IOkm
,I
I/I
II
\1
I",
.
MEA
NC
UR
RE
NT
SPEE
DS
(cm
/s)
Sec
tion
#3:
She
likof
Sea
Val
ley
Maj
orA
xis
=19
00T
o.=
II
,
200
.-
50V
')L
- a> ... a> c ~ --10
0I
I.~
A__
3__
-10
ta-
W\0
015
0
Fig
ure
SO
.--S
ame
asF
igu
re4
8,
exce
pt
for
Secti
on
#3
.
TIDAL CURRENT SPEEDS MOORING #1
1_1126
1_2156 • 01_MAJQa: II K1_MAJ0
1_3/106 IIIlI N2_MAJ0w ~ M2_MAJa: 0 S2_MAJ1_4/165 • K2_MAJ
1_5/240
0 10 20 30 40CURRENT SPEED (em/s)
TIDAL CURRENT SPEEDS : MOORING #2
2_2156
Q • 01_MAJ
a: 2_31106 III K1_MAJ0 II N2_MAJ0w ~ M2_MAJa: 2_4/165 0 S2_MAJ
• K2_MAJ
2_5/220
0 10 20 30 40CURRENT SPEED (em/s)
TIDAL CURRENT SPEEDS MOORING #3
Qa:oowa:
• 01_MAJII K1_MAJ1m N2_MAJ~ M2_MAJo S2_MAJ• K2_MAJ
o 10 20 30CURRENT SPEED (emls)
40
Figure Sl.--Tidal current speeds generated from succesive 29-day harmonicanalysis for transport section #1.
70
TIDAL CURRENT SPEED MOORING #4
4_1/26 • 01_MAJQ
II K1_MAJa:0 II N2_MAJ0w lZJ M2_MAJa: 0 S2_MAJ
4_2156 • K2_MAJ
o 10 20 30CURRENT SPEED (em/s)
40
TIDAL CURRENT SPEED MOORING #5
5_1/26
Qa:0 5_2/560wa:
5_3/106
0
• 01_MAJII K1_MAJIII N2_MAJ~ M2_MAJo S2_MAJ
• K2_MAJ
10 20 30 40CURRENT SPEED (emls)
TIDAL CURRENT SPEEDS MOORING #6
Qa:oowa:
• 01_MAJII Kl_MAJIII N2_MAJ~ M2_MAJo S2_MAJ
• K2_MAJ
o 10 20 30CURRENT SPEED (emls)
40
Figure 52.--Same as Figure 51, except for transport section #2.
71
TIDAL CURRENT SPEEDS MOORING #7
7_1/26
C 7_2156a::00w
7_3/106a::
7_4/185
0
• 01_MAJIII K1_MAJII N2_MAJr;::a M2_MAJo S2_MAJ
• K2_MAJ
10 20 30 40CURRENT SPEED (emls)
TIDAL CURRENT SPEEDS MOORING #8
8_1/26
C 8_2156a::00W
8_3/121a::
8_4/205
0
• 01_MAJII K1_MAJIII N2_MAJ~ M2_MAJo S2_MAJ
• K2_MAJ
10 20 30 40CURRENT SPEED (em/s)
TIDAL CURRENT SPEEDS : MOORING #9
9_1/26
C 9_2156a::00W 9_3/121a::
9_4/168
0
• 01_MAJPI K1_MAJII N2_MAJ~ M2_MAJo S2_MAJ• K2_MAJ
10 20 30 40CURRENT SPEEDS (emls)
Figure 53.--Same as Figure 51, except for transport section #3.
72
.01 0.1 1.0
L1/26m
1
410
210
210
10
10
410
310
310
1
L2/56 m
L4/ 165 m
10 5PER.IOD III DAYS
.J - - - - - ... , , \ It
... ...! \/\/ \1
If\
----- , /, 'i·',Jl J
, ...... .1 .....".
:FR.EQUEllCY III CYCLES I DAY.01 0.1 1.0
- -,.,.,. "
L3/ 106 m150
50
100
100
200
300
200
100
300
MOORING #1 CURRENTSPECTRA
50L5/220 m
10 5 1
START 84240553 6- HOURLY DATA POI NTS10 DEGREES OF FREEDOM
MAJORminor
220 T310 T
Figure 54.--Spectra of the current meter records for Mooring #1 in both thevariance preserving format (to the left) and the spectral densityfunction. All series start on JD 240 in 1984 (25 August) and have 10degrees of freedom. The solid line represents the major axis componentand the dashed line represents the orthogonal minor axis.
73
2200r
310 or
410
310
210
10
10
410
310
210
._---' ....
100 10 5 1
PERIOD II DAYS
IREQUEICY II CYCLES/DAY.01 0.1 1.0
START 84240 MAJOR553 6- HOURLY DATA POI NTS mi nor10 DEGREES OF FREEDOM
MOORING # 2 CURRENTSPECTRA
IREQUEICY II CYCLES/DAY.01 0.1 1.0
;.200 2_2/56m
II1\IIIIII
160 III II II II I
120 I II II \I I
I
80 IIIII
~40 (
~I..l"-- 0IoIolI..lIII0lIIl 2_3/106m1-1
I:lC 1200lIIl~
~
~ 80I..lIIIIoIol
= 40C'IoIolI:lC~- 0
2_4/165m
40
0
2_5/220m40
0100 10 5 1
PERIOD II DAYS
Figure 55.--Same as Figure 54, except for Mooring #2.
74
.01 0.1 1.0
3-5185 m
3_126 m
-- --
95~ I
., -, "-, (,-."
" 1" \ illII I \~
95~ I
95~ I
IREQUEICY II CYCLES I DAY.01 0.1 1.0
3-3106 m
3_126 m
ri'-~"\II, \ ,
o +----4-._-.....--l--l-.....,4-''"''f.~__l__+_\1 " "-14-1+
50
100
100
150
200
220 T310 T
101\
, ~ (I,,\ ,\ ,'" \.
.... " \ I \' \.... ,,~
" ~
100 10 5 1
PERIOD II DAYS
START 84240 MAJOR553 6-HOURLY DATA POINTS minor10 DEGREES OF FREEDOM
MOORING # 3 CURRENTSPECTRA
110 5
3-5220 m
o +---+--+-+-f~I+I--~~''.-1-+-I-+++100
50
Figure 56.--Same as Figure 54, except for Mooring #3.
75
IREQUEBCY IB CYCLES I DAY.01 0.1 1.0
MOORING # 4 CURRENT SPECTRA
START 84240553 6- HOURLY DATA POI NTS10 DEGREES OF FREEDOM
MAJOR - 250 Tminor ---- 340 T
Figure 57.--Same as Figure 54, except for Mooring #4.
76
IREQUEHCY IH CYCLES I DAY.01 0.1 1.0
5_1 IREQUEHCY IH CYCLES I DAY.01 0.1 1.0
80 26m
'.95~ I 5_1
10460 26m
II
40 103
iOl~
102u 20 <l....- ~
~ ~u o-lliIl 0 ~olll lISo-l C"'lI:lIl 5_2
95~I5-2 t'rI
ollll> 56m 56m 10
4 ....80 ~ C"'l
~,
"tl\ ,.1;1r
0'~
103I:lIl 40
1""1-20 10
2
>",
0
5-3106 m
20 ...,...... ,.... ... ,
0100 10 5 1
MOORING # 5 CURRENT SPECTRASTART 84240553 6- HOURLY DATA POI NTS10 DEGREES OF FREEDOM
MAJOR -- 250 Tmi no r - - - - 340 T
Figure 58.--Same as Figure 54, except for Mooring #5.
77
IREQUEICY II CYCLES I DAY.01 0.1 1.0
10
110 5
PERIOD II DAYS
95~I
95~I
100
110 5PERIOD II DAYS
IREQUEICY II CYCLES I DAY.01 0.1 1.0
o+---o--O.....................L...I..I.1_........................................
6-375m I
~_"" Ii
'J \1__ / I.--
o +---+--+-+-+-H+f+--+--+-+-+-t-++t+100
20
40
80
20
60
20
100
MOORING # 6 CURRENT SPECTRA
START 84240553 6- HOURLY DATA POI NTS10 DEGREES Of fREEDOM
MAJOR -- 250 Tminor ---- 340 T
Figure 59.--Same as Figure 54, except for Mooring #6.
78
IREQUEICY II CYCLES I DAY.01 0.1 1.0
10
1
10
- ~---"".., ""\, ..~ ~\
'\..... ~
" I.
100 10 5
PERIOD II DAYS
IREQUEICY II CYCLES I DAY.01 0.1 1.0
1
~ - --_...... _/
7-3106 m
100 10 5
PERIOD II DAYS
o --_
~o+-----1_-...J-'--J....-.L.L..I....L..U._--I........L.....l....L..L.L.LLfo
.---_ ..... - ...'o +-----L----L......L...L.L..I....L..U._--I........L.....L....L..L.L.LLfo
50
50
50
50
100
150
100
100
MOORING # 7 CURRENT SPECTRA
START 84240553 6- HOURLY DATA POI NTS10 DEGREES OF FREEDOM
MAJOR - 190 Tminor --- 280 T
Figure 60.--Sa~e as Figure 54, except for Mooring #7.
79
IREQUEICY II CYCLES / DAY.01 0.1 1.0
IREQUEICY II CYCLES / DAY.01 0.1 1.0
100~L1
26m
954AI &_110
480 26m
10 340
0 102
<:I~
&_2 (\ It'I I I-l
56m,. ....... "' ~
40 lZln
./
954AI t"I'l/ &_4
104 ......
0 220 m n"tl
&-3 ~
10 3121 m
40 '" '" '" '" '" '" ", ..... \ 102
"'0
&_4 10
80 220 m
100 10 5 140
PERIOD II DAYS
0100 10 5 1
PERIOD II DAYS
MOORING # 8 CURRENT SPECTRA
START 84240553 6- HOURLY DATA POI NTS10 DEGREES OF FREEDOM
MAJOR - 190 Tmi nor ---- 280 T
Figure 61.--Same as Figure 54, except for Mooring #8.
80
--_.~---._--~_.
IREQUEICY II CYCLES I DAY.01 0.1 1.0
100 10 5 1PERIOD II DAYS
1
o ~
100 10 5
PER IOD II DAYS
9_1 IREQUEICY II CYCLES I DAY
100 26m.01 0.1 1.0
5095'" I 9_2 10
4
56m0 .- --_ ...... _"'"
10 3
-",- '"./ '" ~
" , '\100 ~ I 102
~L
'"l:l.t ~ ....U
\
..... 50- 10 <l~
~U• ~
""ill ~
0 ~~
i=l4 lZl""ill
('"j
9-3 l'P:Ipo
95'"I 9-3100 121 m 104 .....
~
121 m ('"j
0- Itl~ t;:Ii=l4
50 10 3Iol-I-0 --- -_..... - -- '" 10
2._-'", /'
9_4 '"' '"\
168 m \50 ' I"Y . 10
MOORING # 9 CURRENT SPECTRA
START 84240553 6- HOURLY DATA POI NTS10 DEGREES OF FREEDOM
MAJOR - 190 Tminor ---- 280 T
Figure 62.--Same as Figure 54, except for Mooring #9.
81
P'BEQUE.CY I. CYCLES I DAY.01 0.1 1.0
BARREN ISLANDS30
.01 0.1
95~I BARREN ISL.
1.0
10
10
10
---_ ....
95~I SEMIDI NORTH
95~I SHELIKOF ST.
1"\ I
\ II\ II-, 1\
\, \\( I.
-, I\ 1\\ II\ II\ II\ I \"\-, \
l
,1
11,,
1,
,\, \
1 \, ,1 \ 1
1 \,1
11,
SEMIDI NORTH
SEMIDI SOUTH
10
0t---1f--I-+-t+H+I---+-+-+-I-H+++
ot---1---'I-+-t+H+I---+-+~I-H+++
SHELIKOF STRAIT
30
10
20
20
10
20
10
-- _...... ,
95~ I SEMIDI SOUTH
1
", \
1 ', 'I,,
11
ot---1f--I-+-t+H+I---+-+~I-H-++l-100 10 5
PEBI 0 D I. DAYS
20
10
SURFACE WIND SPECTRA
START 84240 MAJOR - 225 T553 6-HOURLYDATAPOINTS minor --- 315T10 DEGREES OF FREEDOM
100 10 5PEBIOD I. DAYS
1
Figure 63.--Same as Figure 54, except for the surface wind serles.
82
1
1.0
PG
915
3m
51
0
0.1
1
1.0
510
0
.01
o10
10
5
0.1
PG
71
95
m
1
1.0
10
0
o1
I1
11
11
11
1I
11
11
11
11
.01
5
10
15
1
1.0
10
5
0.1
CY
CL
ES
/DA
Y
0.1
PG
319
0m
10
0
01
I1
11
11
11
1I
11
11
11
11
.01
5
PG
69
0m
~ l=l-t u ..... Q
15
u lZl~ t-
ll::I
il1
0~ l> H 0
'~ l::I
il~ - PE
R.IO
DIB
DA
YS
10
01
05
.01
510
15
1
11.0
1.0
10
5
0.1
10
5
0.1
PG
1
25
5m
PG
46
0m
011
11
11
11
11
11
11
11
11
1
.01
10
0
510
15
011
11
11
11
11
11
11
11
11
1
.01
510
0
10
15
(Xl
UJ
BO
TT
OM
PR
ES
SU
RE
GA
UG
ES
PE
CT
RA
ST
AR
T8
42
40
55
36-
HO
UR
LY
DAT
A.PO
INTS
10D
EGR
EES
OFm
EE
DO
M
Fig
ure
64
.--V
ari
an
ce
pre
serv
ing
spectr
ao
fth
eb
ott
om
pre
ssu
reg
aug
ere
co
rds.
95~I
PG1
PG9
PE
RIO
DIS
DA
YS
10
01
01
lO't
95~I
10
0
10
Z
10
1
<l ~ lil:l
1-4
~ •n I"It ..... n ttl
l::I
1
PG3
10
0.1
1.0
CY
CLE
SI
DA
Y
95~I
10
0
0.0
1
10
Z
10
1
10'
1
1.0
10
0.1
10
0
0.0
1
1.0
10
Z
10110
'
1
0.1
CY
CLE
SI
DA
Y
PG7
10
0.0
1
95~I
10
0<l ~ lil:
l1-
4
~ •n I"It ..... n ttl
l::I
1 1.0
PG6
0.1
10
95~I
0.0
1
10
0
10
1
10
Z
10'
1
1.0
0.1
PE
RIO
DIS
DA
YS
10
95~I
PG4
10
0
0.0
1
co .Il-
BO
TT
OM
PRE
SSU
RE
SP
EC
TR
AG
AU
GE
0.0
1ST
ART
84
24
05
53
6-H
OU
RLY
DAT
APO
INTS
10DE
GRE
ESO
ffR
EE
DO
M
0.1
CY
CLE
SI
DA
Y
1.0
Fig
ure
6S
.--S
pectr
al
den
sity
plo
to
fth
eb
ott
om
pre
ssu
reg
aug
ere
co
rds.
100 10 1 100 10 1
I95~ 5_1/26 I9:~___ ~'L1/26
PEBIOD III' DAYS
~103
~100 10 1 ... I
, r\ \
102 \
95~I I'i
2-2/56 103 ( I
101
102
101 I95~ 5_2/56 I95~ ~L2/56
'- 103 _...."--~ "
95~I 102
2-3/106 103
101
""102 n
I:Il
"i=I IIIllo
101
95~ I 95~I ..."\J III
" 5_3/106103
8_3/121 "N n"" " "CIIII -- t:l
"):l95~I 10
2\J 2-4/165..."
103
101
102
" 101 0.01 0.1 1.0
95~ III, 8_4/205
103
CLOCKWISE
95~ICOUNTER-CL OCKWISE
102
2_5/220103
101
/,
102~I I MOORINGS\
\ ,/\\J-'
101 2,5, & 8 0.01 0.1 1'i
I FREQUEII'CY III' CYCLES I DAYI
ROTARY SPECTRAII
0.01 0.1 1.0
Figure 66.--Spectral density plot for the rotary spectra of Moorings 2, 5, and8. All series start on JD 240 in 1984 and have 10 degrees of freedom. Thesolid line represents the clockwise components of the rotational spectrumand the dashed line represents the counterclockwise component.
85
VARIANCE vs DEPTH84240 - 85012 LoPass filtered
o 200 I 500 0 200 500 0 200 500 cm2j s2
MR3MR2MRI
O....,....------l_---L-_----L..._---l_---L-_---l-_.l.....----l-_-----'-_----,
30
240
I
t 150wo
.-E---
o 200 500 o 200 500 o 200 500 cm2j s2
015
.- / (E---I
75tw0
MR4 MRS MR6150
o 200 500 o 200 500 0 200 500 cm2j s2
0.- 30E---It 150w0
240MR7 MR9MRS
Figure 67.--Plot of total variance versus depth for all nine moorings. Unitsare cm 2 /s 2 •
86
FREQUENCY DISTRIBUTION MOORING #1
SEMI DIURNAL
o DIURNALz«d2 TO 6 DAYS
wa:LL 6 TO 13 DAYS
> 13 DAYS
• 1_5/240III 1_4/16511III 1_3/106~ 1_2/56o 1_1/26
o 10 20 30 40 50 60 70 80
PERCENTAGE TOTAL VARIANCE I BAND
FREQUENCY DISTRIBUTION MOORING #2
SEM I DIURN AL
o DIURNAL
~~ 2 TO 6 DAYS "awa:LL6 TO 13 DAYS
> 13 DAYS
• 2_5/220III 2_4/16511III 2_3/56~ 2_2156
o 10 20 30 40 50 60 70 80
PERCENTAGE TOTAL VARIANCE I BAND
FREQUENCY DISTRIBUTION : MOORING #3
• 3_5/185III 3_4/165m 3_3/106~ 3_2156o 3_1/26
DIURNAL ..
SEMI DIURNAL ....
> 13DAysE.~...~~~?
oz«~ 2 TO 6 DAYS
wfE 6 TO 13 DAYS·~~~jl
o 10 20 30 40 50 60 70 80
PERCENTAGE TOTAL VARIANCE I BAND
Figure 68.--Frequency distribution bar graph for the three moorings alongtransport section #1. The length of the bar represents the percentage ofthe total variance in the series that lies within a specified band.These plots were generated from spectra with 553 six~hourly data pointsand 30 degrees of freedom. Precise bandwidth information is contained inTable 17.
87
FREQUENCY DISTRIBUTION: MOORINGS #4 
SEM I DIURN AL
DIURNAL
0z«c:c 2 TO 6 DAYSdL1Ja:u.
6 TO 13 DAYS
>13 DAYS
0 20 40 60
Components along 250 T
• 5_3/106II 5_2/56m 5_1/26o[]] 4_2/56• 4_1/26
80
PERCENTAGE OF VARIANCE / BAND
FREQUENCY DISTRIBUTION MOORING #6
SEMI DIURN AL
DIURNAL
oZ<Cco 2 TO 6 DAYSdw0:::LL
6 TO 13 DAYS
> 13 DAYS
• 6_3/75II 6_2/56iii 6_1/26
o 20 40 60 80
PERCENTAGE TOTAL VARIANCE I BAND
Figure 69.--Same as Figure 68, except for transport section #2.
88
FREQUENCY DISTRIBUTION MOORING #7
DIURNAL
SEMI DIURN AL
oz<a:l
dllJa:lJ..6 TO 13 DAVS
> 13 DAVS
o 10 20 30 40 50 60 70 80
PERCENTAGE TOTAL VARIANCE I BAND
FREQUENCY DISTRIBUTION MOORING #8
SEMI DIURNAL
o DIURNAL '.-
~a:ld 2 TO 6 DAVSllJa:lJ.. 6 TO 13 DAVS
> 13 DAVS
• 7_4/185II 7_3/106m 7_2156~ 7_1/26
• 8_4/205• 8_3/121mI 8_2/56~ 8_1/26
o 20 40 60
PERCENTAGE TOTAL VARIANCE I BAND80
FREQUENCY DISTRIBUTION : MOORING #9
SEMI DIURNAL
o DIURNALZ<~ 2 TO 6 DAVSallJa:lJ..6 TO 13 DAVS "
> 13 DAVS ;...~..
o 20 40 60
PERCENTAGE TOTAL VARIANCE I BAND80
• 9_4/168II 9_3/121II 9_2156~ 9_1/26
Figure 70.--Same as Figure 68, except for transport section #3.
89
TIME SCALES FOR SECTION 1 MR # 1,2,3
200
C/)a: 150::::>0::I:Z
w 100.....J«0C/)
w 50~
i=
0
aa
a
- a a aa
aa a a a
a a
. I
""'i ~ "? .,. u:' ~ "? ~ u;' .. ~ t( .,. "?NN NNMMM,.,..,.,..
TIME SCALE FOR SECTION 2 MR # 4,5,6
200
C/)a:::::> 1500::I:
~
~ 100«0C/)
w 50~
i=
0
a a-
a a a
a a- a
,."
TIME SCALE FOR SECTION 3 MR # 7,8,9
200
C/)a:::::> 1500::I:Z
w 100.....J«0C/)
w 50~
i=
0
a a
a-r- a a a a a
a a a
a
I
RECORD NUMBER
at is the timevariables 1 and 2, respectively.data point (at 6 hrs).
90
Figure 7l.--Plot of the time scale for each record in hours. The integraltime scale (Allen and Kundu, 1982) is a measure of the time between"independent" observations of a non-random time series. The time scale,
n=n\' 0T = L
n=-ncoefficignts forinterval between
CE
NT
ER
PE
RIO
D=
2.38
DA
YS
=0.
42C
PO
BA
ND
WID
TH
=2.
280
TO
2.49
0
CE
NT
ER
PE
RIO
D=
3.21
DA
YS
=0.
31C
PO
BA
ND
SW
IDT
H=
3.03
0T
O3.
410
MR
1M
R2
MR
3M
R1
MR
2M
R3
\0 -
.90
.67
.87
.89
.74
.79
.63
.54
.81
.69
95
• •.5
4
.75
.76
.75
••
CO
HE
RE
NC
ES
QU
AR
ED
OF
CU
RR
EN
TS
:S
EC
TIO
N1
95%
LE
VE
LO
FC
OH
ER
EN
CE
=0.
527
99%
LE
VE
LO
FC
OH
ER
EN
CE
=0.
684
Fig
ure
72
.--S
ch
em
ati
co
fco
her
ence
squ
ared
bet
wee
ncu
rren
tm
eter
sfo
rse
cti
on
#1fo
rth
e2
.38
and
3.2
1d
ayb
and
s.S
oli
dli
nes
con
nec
tre
co
rds
wh
ere
there
issi
gn
ific
an
tco
her
ence
.An
est
imate
of
the
spectr
al
ban
dw
idth
isin
clu
ded
.
CE
NT
ER
PE
RIO
D=
7.67
DA
YS
=0.
13C
PO
BA
ND
WID
TH
=6.
740
TO8.
900
CE
NT
ER
PE
RIO
D=
4.18
DA
YS
=0.
24C
PO
BA
ND
WID
TH
=3.
89D
TO4.
520
\0 1'3
MR
1 .92
.69
.59
MR
2 .97
.92
.56
MR
3 .82
.82
.77
MR
1 .77
.82
.63
MR
2 .89
.81
.63
MR
3 .91
.85
.80
CO
HE
RE
NC
ES
QU
AR
ED
OF
CU
RR
EN
TS
:S
EC
TIO
N1
95%
LE
VE
LO
FC
OH
ER
EN
CE
=0.
527
99%
LE
VE
LO
FC
OH
ER
EN
CE
=0.
684
Fig
ure
73.-
-Sam
eas
Fig
ure
70
,ex
cep
tfo
rth
e4
.18
and
7.6
7da
yb
and
s.
CE
NT
ER
PE
RIO
D=
17.2
5D
AY
S=
0.06
CP
O
BA
ND
WID
TH
=13
.16
0T
O25
.09
0
CE
NT
ER
PE
RIO
D=
10.6
2D
AY
S=
0.0
9C
PO
BA
ND
WID
TH
=8.
910
TO
13
.12
0
MR
1M
R2
.98
MR
3
.95
MR
1
.90
MR
2M
R3 .95
\0 W.9
3
.67
.96
.63
.78
.75 •
•.76
.96
.74
.93
.91 •
•I
•C
OH
ER
EN
CE
SQ
UA
RE
DO
FC
UR
RE
NT
S:
SE
CT
ION
1
95%
LE
VE
LO
FC
OH
ER
EN
CE
=0.
527
99%
LE
VE
LO
FC
OH
ER
EN
CE
=0.
684
Fig
ure
74
.--S
ame
asF
igu
re70
,ex
cep
tfo
rth
e1
0.6
2an
d1
7.2
5d
ayb
and
s.
•
COHERENCE SQUARED OF CURRENTS: SECTIONS 2 AND 395% LEVEL OF COHERENCE = 0.52799% LEVEL OF COHERENCE = 0.684
CENTER PERIOD = 2.38 DAYS = 0.42 CPO
BANDWIDTH = 2.28 0 TO 2.49 0
MR 4 MR 5 MR 6 MR 7 MR 8 MR 9
• • •.56
.62• • •.85
• • •.54
• • •
CENTER PERIOD =3.21 DAYS =0.31 CPO
BANDWIDTH = 3.03 0 TO 3.41 0
MR 4 MR 5 MR 6 MR 7 MR 8 MR 9
• • 164.63 .63
.54
• •.79 .87 .64
•.59 .78
Figure 75.--Schematic of coherence between current meters for Sections #2 and#3 for the 2.38 and 3.21 day bands. Solid lines connect records wherethere is significant coherence.
94
COHERENCE SQUARED FOR CURRENTS: SECTIONS 2 AND 395% LEVEL OF COHERENCE = 0.52799% LEVEL OF COHERENCE = 0.684
CENTER PERIOD =4.18 DAYS = 0.24 CPDBANDWIDTH = 3.89 D TO 4.52 D
MR 4 MR 5 MR 6 MR 7 MR 8 MR 9
.65
.63
.65
.81
.94
.84
.61
.70.84
.62
CENTER PERIOD = 7.67 DAYS = 0.13 CPDBANDWIDTH = 6.74 D TO 8.90 D
MR 4 MR 5 MR 6 MR 7 MR 8 MR 9
•.97 .60 .91
.92.55
.61
.86.76
•.77
Figure 76.--Same as Figure 73, except for 4.18 and 7.67 day bands.
95
COHERENCE SQUARED FOR CURRENTS: SECTIONS 2 AND 3
95% LEVEL OF COHERENCE = 0.52799% LEVEL OF COHERENCE = 0.684
CENTER PERIOD = 10.62 DAYS = 0.09 CPDBANDWIDTH = 8.91 D TO 13.12 D
• •
MR 4 MR 5 MR 6 MR 7 MR 8 MR 9
.54 .64 173 .91
.77 .80
•
CENTER PERIOD = 17.25 DAYS = 0.06 CPDBANDWIDTH = 13.16 D TO 25.094 D
MR 4 MR 5 MR 6 MR 7 MR 8 MR 9.60
0 '".,
195.68 .82 .85 .84 .93
.57.61 "" .70
.68 .70 68.65 •• .. 0
• • •Figure 77.--Same as Figure 73, except for 10.62 and 17.25 day bands.
96
-----
1.50
-,Se
ctio
nI
----
Sect
ion
2..
....
...
Sect
ion
3I
1.00
-
......
... · · ·I ..
....
...
1_...
.....
. · · · ·.......
..
I
......
...
I
i··
.
II
I
,........ V) a..
::l
L.. "E
0.50
f~
:>
:--=
1I
V)
--I-
---
--
-,....
....--
-.
-•••
•••••
1I
I:
I---
.---
I-...
J,-
--I
LI
I:
Ia::
:-
•--
---
l:
Io
0.0
0;
L_
JL
__--J
I:L.
••••
••••
•
V') Z ~ I-
\0 -.J
0.00
1I
II
II
I,I
II
II
,
-0.5
0---
Res
idua
l[1
-(2
+3
)]1
Aug
1984
ISe
pI
Oct
TN
ovI
Dec
IJa
n19
85
TOTA
LT
RA
NSP
OR
T
Fig
ure
78
.--T
end
ayav
erag
eso
ftr
an
spo
rtth
rou
gh
each
Secti
on
.T
here
sid
ual
cu
rren
tre
mai
nin
gaft
er
the
tran
spo
rtth
rou
gh
Secti
on
1is
sub
tracte
dfr
omth
esu
mo
fth
at
thro
ug
hS
ecti
on
s2
and
3is
plo
tted
inth
eb
ott
om
pan
el.
TABLES
99
Table 1.--Duration and location of the current meter records showing theinstruments on each mooring.
Mooring Latitude Longitude Start lEnd Days Instruments(OW) (ON) JD eM BP
1 57.72 155.26 84235/85016 147 5 X2 57.60 155.01 84235/85016 147 53 57.51 154.77 84235/85015 146 5 X
4 56.45 156.98 84236/85207 337 2 X5 56.35 156.90 84236/85207 337 36 56.28 156.82 84236/85207 337 3 X
7 55.95 156.60 84237/85206 335 4 x8 55.94 156.36 84237/85206 335 49 55.91 155.15 84237/85206 335 4 x
100
Table 2.--Current meter statistics for Moorings #1, #2, and #3. The RMS erroris calculated as {S/{L/t)~} where S is the standard deviation of theseries, L is the length of the series in hours and t is the integral timescale after Allen and Kundu, 1982. The variance is calculated along theprincipal axes shown as U and V and is written as MAJOR/minor axisvariance. DIR ~s the ~xis of greatest variance and the ellipse is thequotient (MAJOR~/minor~).
Meter V{220T) U010T) Dir Variance Ellipse(cm/s) (cm/s) (OT) (cm 2 /s 2 )
1-1/26m 24.4 ± 3.1 -1.7 ± 0.5 214 506/23 4.7l-2/56m 22.1 ± 2.6 0.4 ± 0.4 220 411/12 5.9l-3/l06m 15.0 ± 2.3 0.4 ± 0.3 224 320/08 6.4l-4/165m 6.4 ± 1.8 -0.2 ± 0.2 223 215/02 9.7l-5/240m 4.2 ± 1.1 0.6 ± 0.2 227 81/02 6.6
2-2/56m 21.3 ± 3.5 3.5 ± 1.8 231 297/228 1.12-3/l06m 16.0 ± 2.9 3.6 ± 1.4 223 196/141 1.22-4/l65m 6.3 ± 2.0 1.6 ± 1.0 58 78/61 1.12-5/220m 2.0 ± 1.1 0.0 ± 0.9 74 45/45 1.0
3-l/26m 0.2 ± 3.2 0.3 ± 0.8 219 337/52 2.63-2/56m -0.5 ± 2.8 -0.2 ± 0.7 220 252/36 2.73-3/l06m 0.7 ± 2.2 0.8 ± 0.6 218 153/25 2.53-4/l65m -5.3 ± 1.0 0.0 ± 0.2 227 86/05 4.33-5/220m -6.7 ± 1.4 0.1 ± 0.2 225 139/05 5.3
101
Table 3.--Current meter statistics for Moorings #4, #5, and #6. Calculationsare the same as 1n Table 2.
Meter V{250T) U(340T) Dir Variance Ellipse(cm/s) (cm/s) (OT) (cm 2 /s 2 )
4-1/26m 11.4 ± 1.6 1.0 ± 1.0 247 130/72 1.34-2/56m 8.5 ± 0.9 1.3 ± 0.5 265 38/13 1.7
5-1/26m 9.5 ± 2.3 0.4 ± 2.5 150 170/189 0.955-2/56m 7.4 ± 2.3 1.5 ± 2.8 131 161/182 0.95-3/106m 5.2 ± 1.1 1.9 ± 1.3 116 51/52 1.0
6-1/26m 6.1 ± 3.6 -3.1 ± 1.6 241 273/121 1.56-2/56m 2.8 ± 1.8 -1.6 ± 1.1 234 105/59 1.36-3/75m 0.9 ± 1.1 -0.5 ± 1.1 223 63/45 1.2
102
"
Table 4.--Current meter statistics for Moorings #7, 18, and #9. Calculationsare the same as In Table 2.
Meter V(l90T) U(280T) Dir Variance Ellipse(cm/s) (cm/s) (DT) (cm 2/s 2 )
7-l/26m 23.0 ± 3.8 4.3 ± 1.5 201 369/116 1.87-2/56m 21.5 ± 3.9 5.0 ± 1.1 199 364/61 2.47-3/l06m 11.3 ± 2.8 3.2 ± 0.7 199 233/33 2.77-4/185m -0.4 ± 2.0 -1.6 ± 0.6 205 130/26 2.2
8-1/26m 21.1 ± 2.9 2.2 ± 1.7 186 241/163 1.28-2/56m 17.9 ± 2.8 1.4 ± 1.6 191 191/123 1.38-3/121m 8.6 ± 2.0 0.3 ± 0.9 204 142/53 1.68-4/205m -1.2 ± 1.8 -3.0 ± 1.3 219 137/58 1.5
9-1/26m 6.2 ± 2.9 5.7 ± 1.2 181 278/70 2.09-2/56m 5.5 ± 2.5 3.2 ± 1.1 181 220/57 2.09-3/121m 3.6 ± 1.9 -0.1 ± 0.7 189 173/31 2.49-4/168m -2.6 ± 1.0 1.9 ± 0.6 180 81/15 2.3
103
Table 5.--Statistics for the Geostrophic Winds, Integrated Transport andBottom Pressure Gauges. All calculations are done as in Table 2.
WIND STATISTICS
Location V{225T) U(3l5T) Variance Ellipse(m/s) (m/s) (m 2 /s 2 )
Barren Islands 2.8 ± 0.6 0.9 ± 1.3 21163 0.6
Shelikof Strait 2.3 ± 0.7 1.2 ± 1.3 21/66 0.6
Semidi IslandsNorth -0.2 ± 0.8 1.3 ± 1.1 28/52 0.7
Semidi IslandsSouth -0.5 ± 0.8 0.9 ± 1.2 32/55 0.8
TRANSPORT STATISTICS
Section Mean TR Standard Deviation Time Scale Variance(SV) (SV) (Hours) (SV)2
1 surface 0.53 ± 0.06 0.32 136.1 0.1051 bottom 0.29 ± 0.04 0.22 110.9 0.104
2 surface 0.24 ± 0.03 0.17 113.9 0.0302 bottom 0.02 ± 0.01 0.03 89.1 0.001
3 surface 0.51 ± 0.07 0.32 144.3 0.1033 bottom 0.17 ± 0.06 0.35 88.7 0.124
BOTTOM PRESSURE GAUGE STATISTICS
MOORING Depth P{Mean) Standard Deviation Variance Time Scale(m) (~':101+mb) (mb) (mb 2) (hours)
PG 1 255 2.62 5.87 34.4 116.3PG 3 190 1.98 5.46 29.8 153.2PG 4 60 0.85 7.50 56.2 136.7PG 6 90 1.05 6.76 45.7 130.1PG 7 195 2.11 5.55 30.8 169.9PG 9 183 1.97 4.20 17.6 289.0
104
~ o VI
Tab
le6
.--C
orr
ela
tio
nm
atri
xfo
rcu
rren
tm
eter
reco
rds
onS
ecti
on
#1
.T
heco
eff
icie
nt
isfo
llo
wed
byth
ela
gin
pare
nth
ese
s(i
nh
ou
rs)
wit
hco
lum
nla
gg
ing
the
row
.If
there
isno
nu
mb
er,
the
co
rrela
tio
nw
asn
ot
sig
nif
ican
tat
the
95%
con
fid
ence
lev
el.
Re
co
rd1-
11-
21-
31-
41-
52-
22-
32-
42-
53-
13-
23-
33
-43-
5T
1-1
/26
1.0
.95
.72
.31
----
----
---.
24
----
----
62.9
3
1-21
561
.0.8
3.3
6--
-.2
7--
----
-.2
5--
----
--56
.00
1-3
/10
61
.0.4
5.2
4-.
24
(6)
-.2
1(6
)--
----
---
----
52.8
6
1-4
/16
51
.0.5
7--
----
---.
27
-.2
8-.
25
-.2
6(2
4)
--52
.58
1-5
/24
01
.0-
.30
(24
)-.
27(
24)
----
-.2
2-.
27
(12
)-.
24
(12
)--
--52
.43
2-2
/56
1.0
.96
.80
.48
----
----
--15
5.62
2-3
/10
61
.0.8
7.5
5--
---
----
174.
29
2-4
/16
51
.0.7
3--
----
----
184.
57
2-5
/22
01
.0--
----
--*
94.5
5
3-1
/26
1.0
.94
.73
----
104.
55
3-2
/56
1.0
.86
----
104.
11
3-3
/10
61
.0--
--10
3.45
3-4
/16
51
.0.8
341
.82
3-5
/22
01
.044
.97
Tab
le7
.--C
orr
e1at
ion
mat
rix
for
curr
ent
met
erre
cord
son
Sec
tio
n12
.by
the
lag
inp
aren
thes
es(i
nh
ou
rs)
wit
hco
lum
nla
gg
ing
the
row
.co
rrela
tio
nw
asn
ot
sig
nif
ican
tat
the
95%
con
fid
ence
lev
el.
The
co
eff
icie
nt
isfo
llo
wed
Ifth
ere
isno
num
ber,
the
.... o (J\
Rec
ord
4-1
4-2
5-1
5-2
5-3
6-1
6-2
6-3
T
4-1
/26
1.0
.67
----
.25
(6)
----
--5
6.5
5
4-2
/56
1.0
----
.32
(6)
----
--6
3.6
9
5-1
/26
1.0
.78
.39
----
.25
86
.82
5-2
/56
1.0
.44
----
--11
0.55
5-3
/10
61
.0--
----
89
.45
6-1
/26
1.0
.89
.77
111.
95
6-2
/56
1.0
.87
88
.72
6-3
/75
1.0
62
.82
..... o .......
Tab
le8
.--C
orr
ela
tio
nm
atri
xfo
rcu
rren
tm
eter
reco
rds
onS
ecti
on
#2
.T
heco
eff
icie
nt
isfo
llo
wed
byth
ela
gin
pare
nth
ese
s(i
nh
ou
rs)
wit
hco
lum
nla
gg
ing
the
row
.If
there
isno
nu
mb
er,
the
co
rrela
tio
nw
asn
ot
sig
nif
ican
tat
the
95%
con
fid
ence
lev
el.
Rec
ord
7-1
7-2
7-3
7-4
8-1
8-2
8-3
8-4
9-1
9-2
9-3
9-4
T
7-1
/26
1,0
.93
.75
.50
----
--.5
3-.
28
(19
)-.
26
(30
)--
--13
3.25
7-2
/56
1,0
.85
.60
--.3
7(3
0).3
8(6
).5
6-.
33
(30
)-.
33
(30
)--
.21
138.
06
7-3
/10
61
,0.7
3+
.45
(30
).4
7.5
6.6
2(6
)-.
38
(30
)-.
45
(30
)--
.20
117.
70
7-4
/18
51
,0.3
4(2
4)
.48
.56
(6)
.6I(
12)
----
--.3
410
0.38
8-1
/26
1,0
.87
.54
.26
----
----
80
.03
8-2
/56
1,0
.72
.37
---
----
95
.22
8-3
/12
11
,0.5
1--
----
--8
0.6
8
8-4
/20
51
,0-.
34
(30
)-.
35
(30
)--
.21
93
.49
9-1
/26
1.0
.89
.57
.23
89
.74
9-2
/56
1,0
.69
.37
88
.20
9-3
/12
11
,0.6
374
.74
9-4
/16
81
,039
.35
Tab
le9
.--C
orr
ela
tio
nm
atri
xfo
rth
ere
lati
on
ship
of
the
inte
gra
ted
tran
spo
rtse
cti
on
sw
ith
each
oth
er.
The
lag
isin
par
enth
eses
aft
er
the
co
rrela
tio
nco
eff
icie
nt
and
isex
pre
ssed
inh
ou
rs.
Su
rfac
e1
Bot
tom
1T
ota
l1
Su
rfac
e2
Bot
tom
2T
ota
l2
Su
rfac
e3
Bot
tom
3T
ota
l3
t-'
a 00
Su
rfac
e1
1.0
Bot
tom
10
.67
1.0
To
tal
10
.91
0.9
11
.0
Su
rfac
e2
0.3
90
.42
0.4
41
.0
Bot
tom
2"i
lr0
.35
0.3
30
.56
1.0
To
tal
20
.39
0.4
40
.45
0.9
90
.66
1.0
Su
rfac
e3
0.6
70
.65
0.7
2"il (
0.3
0*
1.0
Bot
tom
30
.52
(6)
0.5
6(1
2)
0.5
9(6
)"it:
0.2
9(3
0)
*0
.65
1.0
To
tal
30
.65
0.6
50
.71
*0
.30
*0
.90
0.9
21
.0
..... o \0
Tab
lelO
.--C
orr
ela
tio
nm
atr
ixfo
rth
eal
on
gch
ann
elcu
rren
tsv
s.B
arre
nIs
lan
dw
ind
sre
solv
ed
alo
ng
ax
iso
fm
axim
umco
rrela
tio
n.
Sec
tio
n1
Sec
tio
n2
Sec
tio
n3
Moo
ring
Inst
r.r
lag
OIR
Moo
ring
Inst
r.r
lag
OIR
Moo
ring
Inst
r.r
lag
OIR
(hrs
.)(r
max
)(h
rs.)
(rm
ax)
(hrs
.)(r
max
)
1-1
.44
1228
5·4
-1.2
16
22
5·/
24
5·
1-1
.41
1826
50
-2.4
418
28
5·
-2.2
96
245·
-2.4
812
265
0
-3.3
924
28
5·
-3.5
318
265
0
-4.2
424
32
5·
-4.6
212
285
0
-5-.
23
022
5·
2-2
.33
1826
50
5-1
**
*8
-1.3
418
26
5./
28
50
-3.3
318
265·
-2*
*..::
-2.4
812
285
0
-4.3
818
265·
-3*
**
-3.6
018
285
0
-5.4
918
26
5./
28
50
-4.6
318
265
0
3-1
-.3
424
34
5·
6-1
.36
624
50
9-1
**
*-2
-.3
024
345·
-2.4
46
245
0-2
*0
345
0
-3*
..':*
-3.4
16
245
0-3
*0
305
0
-4.3
812
345·
-4.3
30
265
0/2
850
-5.3
312
34
5·
*N
otsi
gn
ific
an
tat
95%
lev
el.
Table 11.--Correlation matrix for the integrated transport sections andbottom pressure series vs. the surface winds.
Section 1 Section 2 Section 3
Surface 0.44(18) 245° 0.36(12) 225°/245° 0.48(12 ) 285°
Bottom 0.52(18) 285° 0.26(18) 245° 0.70(12) 285°
Total 0.49(18) 265° 0.36(12) 225°/245° 0.64(12 ) 265°
Coefficients for 245° to 285° vary by <0.1.
Bottom pressure as a function of Barren Island wind direction.
PG 1
PG 3
0.43(-6) 265°
0.38(-6) 265 0
PG 4
PG 6
0.54(6) 265 0
0.53(6) 265 0
110
PG 7
PG 9 ,"*'t
..... ~ .....
Tab
le1
2.-
-Co
rrela
tio
nm
atr
ixfo
rp
ress
ure
dif
fere
nces
vs.
Secti
on
#1cu
rren
tm
ete
rs.
dpC
ross
Str
eam
Bot
tom
Pre
ssu
reD
iffe
ren
cev
s.S
ecti
on
1C
urr
ents
Rec
ord
1-1
1-2
1-3
1-4
1-5
2-2
2-3
2-4
2-5
3-1
3-2
3-3
3-4
3-5
dp1-
3.2
8(6
).3
D(6
).2
4.2
7.3
3--
----
.34
(6)
----
--.2
7.2
6
dp4-
6.2
5.2
6.2
6.2
4--
.36
(30
).3
5(1
8)
--.4
0--
----
----
dp7-
9.3
8.3
5.J
2(
18)
.26
(42
)--
----
.45
.52
----
----
--dp
6-9
.39
.40
.39(
18)
.33
(42
)--
.46
(12)
.45
(6)
.53
(6)
.56
----
----
----
dpD
own
Str
eam
Bot
tom
Pre
ssu
reD
iffe
ren
cev
s.S
ecti
on
1C
urr
ents
Rec
ord
1-1
1-2
1-3
1-4
1-5
2-2
2-3
2-4
2-5
3-1
3-2
3-3
3-4
3-5
dp1-
4--
---.
26
-.3
0(3
0)
---.
54
-.5
3-.
51
-.4
0--
----
----
dp1-
6--
---.
22
----
-.5
4-.
51
-.4
8-.
33
----
----
--dp
1-7
----
----
---.
37
-.3
3-.
27
----
----
----
dp3-
9--
----
----
----
--.3
B(1
8)--
----
----
.... .... N
Tab
le1
3.-
-Co
rre1
atio
nm
atri
xfo
rp
ress
ure
dif
fere
nces
vs.
Sec
tio
n12
cu
rren
tm
eter
s.
~p
Cro
ssS
trea
mB
otto
mP
ress
ure
Dif
fere
nce
vs.
Sec
tio
n2
Cu
rren
ts
Rec
ord
4-1
4-2
5-1
5-2
5-3
6-1
6-2
6-3
~p1-3
----
----
----
----
~p4-6
.23
.27
.45
.54
.43
.51
.54
.53
~p7-9
--.2
4--
--.3
1{30
)--
.39
.42
~p6-9
--.2
0--
----
.51
.59
.56
~p
Dow
nS
trea
mB
otto
mP
ress
ure
Dif
fere
nce
vs.
Sec
tio
n2
Cu
rren
ts
Rec
ord
4-1
4-2
5-1
5-2
5-3
6-1
6-2
6-3
~p1-4
----
-.3
6(3
0)
-.4
1(4
2)
---.
56
-.6
0-.
52
~p1-6
----
---.
34
(42
)--
-.4
8-.
51
-.4
2
~p1-7
----
----
----
----
~p3-9
----
----
----
.36
.34
......
......
w
Tab
le1
4.-
-Co
rrela
tio
nm
atr
ixfo
rp
ress
ure
dif
fere
nces
vs.
Secti
on
#3cu
rren
tm
ete
rs.
apC
ross
Str
eam
Bot
tom
Pre
ssu
reD
iffe
ren
cev
s.S
ecti
on
3C
urr
ents
7-1
7-2
7-3
7-4
B-1
8-2
8-3
8-4
9-1
9-2
9-3
9-4
apl-
3--
--.3
H30
).3
2(2
4)
----
.20
(18
).2
7--
----
.35
(18
)
ap4-
6--
----
.22
--.3
5(6
).3
1(1
2)
----
----
--ap
7-9
.54
.62
.75
.81
.40(
12)
.57
.67
.79
(6)
----
--.4
2
ap6-
9.6
3.7
1.7
8.7
1.5
4(1
8)
.70
.73
.54
----
--.2
6
apD
own
Str
eam
Bot
tom
Pre
ssu
reD
iffe
ren
cev
s.S
ecti
on
3C
urr
ents
I7-
17-
27-
37-
48-
18-
28
-38
-49-
19
-29
-39-
4
I.
ap1-
4-
.51
-.5
1-.
54
-.4
4-.
44
-.5
8-.
56
----
----
--ap
l-6
-.5
0-.
52
-.5
6-.
44
-.4
5-.
56
-.5
6--
----
----
apl-
7--
---.
21
-.2
3-.
17
-.1
8-.
24
-.2
5--
-.2
1(1
8)
--.3
4(1
8)
ap3-
9.4
1(1
2)
.4H
i,)
.55
(6)
.58
(12
).3
2(1
8)
.43
(12
).4
2(1
2)
•51(
18)
---
--.3
7
.-. .... .po
Tab
lel5
.--C
orr
ela
tio
nm
atri
xfo
rre
lati
on
sb
etw
een
dow
nsh
elf
and
cro
sssh
elf
pre
ssu
red
iffe
ren
ces.
Cro
ssS
trea
mv
s.D
own
Str
eam
/Bo
tto
mP
ress
ure
Dif
fere
nce
Lip
l-3
Lip
4-6
Lip
7-9
Lip
6-9
Lip
l-4
Lip
l-6
Lip
l-7
Lip
3-9
Lip
l-3
1.0
--.2
1.2
3(1
8}
.35
.43
.58
-.2
0
Lip
4-6
1.0
--.5
Hl2
}-.
65
(6}
-.4
8(1
2}
----
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Table 17.--Bands used in the description of the frequency distribution of therecords (Figures 60 to 62). Also, the distance between pressure gauges(in kilometers) is given to show the separation in the pressuredifference series.
Target Band Period Frequency Spectral BandDays Cycles/Day Period/Frequency
Semi-Diurnal 0.50-0.54 1. 859-2.005 0.492-0.551/(1.815-2.033)
Diurnal 0.96-1.12 0.893-1.039 0.917-1.145/(0.873-1.091)
Two to six days 2.00-5.99 0.50-0.167 1. 96-6.73/(0.149-0.511)
six to thirteen 6.00-12.99 0.167-0.077 6.73-13.14/days (0.149-0.076)
Greater than 12.99 <0.077 13.14thirteen days «0.076)
DISTANCE BETWEEN PRESSURE GAUGES (IN KM)
Down-Shelf Differences Cross-Shelf Differences
PG 1 - PG 4 176.8 PG 1 - PG 3 36.8
PG 1 - PG 6 186.2 PG 4 - PG 6 20.5
PG 1 - PG 7 214.7 PG 7 - PG 9 29.8
PG 3 - PG 9 198.5 PG 6 - PG 9 58.8
116