TECHNICAL REPORT

DISTRIBUTION OF ICE IN BAFFIN BAY
AND DAVIS STRAIT

HENRY S. KAMINSKI

Applied Oceanography Branch
Division of Oceanography

FEBRUARY 1955

U. S. NAVY HYDROGRAPHIC OFFICE
=e WASHINGTON, D. C.

ABSTRACT

The distribution of sea and land ice in Baffin Bay and Bevis
Strait is presented by operational localities. The behavior
of the ice is discussed by meteorological and oceanographic
parameters. The ice condition charts, presented by months,
are compiled largely from data gathered by Hydrographic
Office observers over a period of years. Special emphasis
is placed upon those ice properties known to affect aircraft
trafficability. It is concluded that in certain areas, ice
topography tends to remain relatively stable, whereas in
other areas the topography tends to fluctuate with passing
storms.

FOREWORD

Interest in arctic problems requires shipping to enter
areas where sea ice restricts certain types of surface move—-
ments. In addition, with the use of aircraft over arctic areas,
there is need for information about distribution of ice in the
sea, with reference to the feasibility of emergency landings on
ice as well as planning and executing various operations in the
areas, This report has been prepared at the request of the U.S.
Air Force and depicts ice conditions, by month, for the Baffin
Bay—Davis Strait area.

Since the Hydrographic Office is charged with the respon-
sibility of developing and testing techniques for the observing
and forecasting of sea ice conditions, much of the developmental
work has been performed in conjunction with logistic operations.
Observations of ice in the Baffin Bay—Davis Strait area during
recent seasons have been reviewed critically for the preparation
of this report.

The author was killed in a plane crash near Paget Point,
Ellesmere Island on 16 April 1954, while participating as an ice
observer aboard a U.S. Navy ice reconnaissance patrol plane.

UT oe oP

Je Be COCHRAN
Captain, U. S. Navy
Hydrographer

He HOUTA A

atalt

DISTRIBUTION LIST

CNO (Op-03, 03D3, 31, 316, 32, 33, 332, Oh, 05, 533, 55)
BUAER. (2)

BUSHIPS (2)

BUDOCKS (2) |

ONR (Code 100, 102, 410, 416, 420, 430, bbl, b66)

NOL (2) 7

NEL (2)

(2).

COMOPDEVFOR (2)
COMSTS a

CODTMB (2
AROWA
SUPNAVACAD (2)
NAVWARCOL (2)
NAVPOSTGRADSCOL, Monterey (2)
COMDT COGARD (IIP) (2)
usceGs (2)
CG USAF (AFOOP)
CGAWS (2)
CGNEAC (2)
USAF CAMBRSCHLAB (2)
USWB (2)
CIA (2)
. BEB (2)
SIPRE (2)
ASTIA (2)
ARTRANSCORP
CE (2)
INTIHYDROBU, Monaco (2)
ARCRSCHIAB, COL, Alaska
ARCINSTNA (2)
WHOL (2)
SIO (2)
UNIV WASH (2)
TEXAS A&M (2)
CBI (2)

iv

PREFACE

This study concerns the distribution of sea ice and ice of land
origin in the Baffin Bay-Davis Strait region. Consideration is given
to ice as it normally appears in these areas in terms of space and time.
It should be emphasized, however, that the presentation of sea ice condi-
tions for any given period of the year, although substantially useful as
a guide, may have restricted value when applied to a specific field oper-
ation.

In order for a study of this nature to be applicable to a specific
operation, a broad scale investigation of the dynamic as well as the kine-
matic forces involved in the processes of sea ice formation, growth, de-
velopment, and distribution would be required. A well integrated approach
to the problem would include the determination of the thermohaline structure
of the waters (on a much larger scale than heretofore employed by this
Office), and a continuous study of air temperatures, wind, and precipitation.
This would establish not only the date of initial ice formation, but also
its rate of growth. The second step in the field investigation of ice
would include long-range aerial surveys of the ice throughout the area
of distribution for visual evaluations of the many topographic features
of the ice, significant ice forms, extent and concentration of the ice,
the location of certain types of sea and land ice, and its designation
in terms of textual and graphic presentation. This type of study of sea
ice conditions would furnish reliable data. It would provide the location
of sea ice suitable for forced or deliberate landing of aircraft and infor-
mation consonant with the requirements of any specific operation.

The formation and growth of sea ice is a function of oceanographic and
meteorological variables. These vary from year to year, so We may expect
different ice years. The distribution of ice over a given water area, with
respect to variance in topographical features, is also a function of the
meteorological parameters. Thus, th» magnitude and frequency: distribution
of pressure ridges, the number and quality of refrozen leads, and the pres-
ence or absence of open water areas are related and are subjected to the
impact of the pressures and stresses exerted on the ice by the passage of
many storms and pressure patterns of varying intensities. If the early
history of development and growth of winter ice is associated with rela-
tively long periods of calms, light winds, and few storms, the topography
of the ice will feature few pressure ridges, Conversely, if the early
history is associated with intense storm activity, the topography of the
ice will present a wild array of pressure ridges, compressed and irregular
ice, and a high degree of rafting. With respect to the latter, however,
there are greater numbers of frozen leads in varying sbages of growth, size,
and orientation.

The presentation of normal sea ice conditions, in the Baffin Bay—Davis
Strait region, is based largely upon the observations of personnel of the
U. S. Navy Wydrographic Office. Over the past years, they have flown several
hundred aerial ice reconnaissance surveys, either preliminary to, or in

direct support of surface operations in these waters. Also used as
material for this study were ship and shore observations of ice condi-
tions taken in recent years, and some historical data contained in
reports of the many exploratory voyages in these waters during this
and the past century.

This information should serve as a useful guide and reference in
determining feasibility of emergency landings on ice, and the planning
and execution of operations in these waters, particularly when modified
to reflect the deviations from normal of factors controlling the growth,
distribution, and behavior of sea ice.

Minor corrections have been made in the reprint of this report,
formerly identified as H.O. Misc. 15891 and printed in 1954.

vi

CONTENTS

Foreword. ° e e e e e ° e e ° e e e e © e es e e e e ° ° e @ e e e e iii
DUSt rut Ona sGeotoiiol e iiell el) (elliel elo) ve) te) Kell) c/l ole) (ellie) elifelion Ko} olla iv
BRE 61d 6 Glo OC O-OlO 6 G-OO1 oO On0 Geo Olo 0-0 6nO 0 0 O60 5 \ir
List of Figures GRoMartadies chiet ier aris 1 e1 ote! verre lel nelvc! talWoiNemcclmonveknenToumuV cL
A. Introduction. ..«-«ceesrsrce roto ee oe oe © © 6 8 ew OO 1
B, Baffin Bays ° e e ° @ e °o @ e oc e e ° e e @ e e °o e e e e e e ° 3
Thule and Approaches. ee 0 @ © © © @ 8 8 Oe ele ele lle 3
Wolstenholme g to Kap Yorke . «6 o o «© 0 © @ © © © 0 0 0 Oe 4
Kap York to Tasiussaq Bugt o © 0 @¢ © © © © © © © © © Oe Oe h
Melville Bugt ee 0 © © © © © © 0 8 e080 8 8 & 8 © © © OO me)
Tasiussaq Bugt to Diske Bugt. © 00 @ © © 809 © © © © © © OO 7
Outer ice from Tasiussaq Bugt to Disko Bugt » « « o e o e o Ul
Disko Bugt to Séndre Strdmf jord @ 6) “Oo: ei) 1: 6). 010) 40! “el Jie! ‘e) orre 8
Cape Chidley te Cape Dyer . oo. «0 eo oe eo eo ow oe 8
Cape Dyer to Bylot usler~l o 96 66 OOOO OOOO 0 OOO 6
Bylot Island to Ellesmere Island. . 2. . 0 «0 e0e eee 12
The Baffin Bay PARK G9 6.000.000 00000000006 0 13
Go (Gleglee IO 5 Goo Oo OOOO Ob Doo 0g Oo 16
Bibliography. o ® ° e eo e ° e e e ° e e e °o e e e @ e e e ° e e e e 32

FIGURES
Figure ; Page

1 - General Circulation. o o « 18

2- January Tce Distribution oc s oe «oo © 0) oe! «© 0) 0 «6 19
3 = February MOG WHE HUSEION, 5 5 5 OOO OOOO OOOO OO 20
L - March Ice Distribution © ja! 0) (@). ©) ..@.-0° 0))0).-0 © @ -.0'4 6)" .0 0). 0) 20) 10 21
5 - April Iss) Whine Go 4G oO Oo Oma Oooo ooo 22
6 ~~ May Ice Distribution °o 0 @@® 008 © @ © @ © 0 © © © © © 8 oO 8 23
7 — June Ice Distribution. «oo ee se ee es eo ew wwe ow |
8 - July lcamDitstaxioutloncs eo cltel mreliolins tel elleteliel ols) (eiiosolionie 25
Oey Mirsastmelcey Distillers ne delete, eee) eee te Malion meshes lame 20
10 - September HGS WAlsiaealer 6 oo 6b OOOO oO OOOO oO 27
IL = OPielasio NOS Whisper 5 6 ag oo OO Oooo OOO 28
12 = November Ice Distributions . . 2500s e se cee oe oe 629
13) —abecenber ice: Dusbribubianiosisetsi st (amic: tioljetie! elle olfelienis 1 ur 5O
1, = Place Name Location Chart. . .<2«ocece cece esv ee Jl

dle s

DISTRIBUTION OF ICE IN BAFFIN BAY AND DAVIS STRAIT
A. INTRODUCTION

A description of sea ice conditions in Baffin Bay and Davis Strait
would be incomplete without a brief discussion of the general disposi-
tion of the water circulation, and some of the external forces to which
they are exposed. Movement and structural peculiarities of the ice are
due chiefly to the geographical position of these waters and their
circulation.

The Baffin Bay—Davis Strait system of waters is complex. Currents
off the southwestern coast of Greenland, characterized by relatively
high salinities and temperatures, flow northward into the waters off
Disko and beyond. Tributary waters from Lancaster, Jones, and Smith
Sounds flow into northwestern Baffin Bay. From here the currents travel
southward along the coasts of Baffin Island and Labrador bringing in
polar waters, A great eddy-current system is formed in Baffin Bay. To.
the south, the warm north-setting, West Greenland Current is diverted by
the Hellefiske Bank and the Davis Strait ridge to the west, and south
toward the coast of Labrador and back into the Labrador Sea. Thus, slow
warm waters set against swift cold waters markedly influencing the forma-
tion of ice in the area.

The first area of the striking effect of the influence of the warm
currents is the Labrador Sea and along the shores of western Greenland as
far north as the southern approaches to Melville Bugt. South of the 66th
parallel, except for a few coastal indentations and fjords, the waters
rarely freeze. To the north of this latitude, except for the fjords and
bays, the ice arrives late, is generally weak, and is very unstable. The
westward and southward deflections of the large water mass by the Hellefiske
Bank not only keeps the inner waters of the Labrador Sea free of sea ice,
but also causes large quantities of sea ice at the southern periphery of
the Baffin Bay-Davis Strait pack to drift southwestward, thereby contrib-
uting to the great ice drift off the Labrador coast.

The second region where water circulation influences the behavior of
ice is the western part of Baffin Bay and Davis Strait from the area of
southern Ellesmere Island to Newfoundland. Here the cold currents exert
constant pressure on the ice, setting some sections of the Baffin Bay Pack
into eddy motions, and carrying large quantities of sea ice formed in
Baffin Bay and Davis Strait southward into the drift stream off Labrador.
Winter and polar ice discharged into Baffin Bay through the sounds enter
the pack, become part of it, and are carried southward, Disturbed sections
of the pack expose areas of water which rapidly refreeze, only to. break
again and resume the production of new winter ice. It grows and replen-
ishes the great drift of ice to the south in this manner.

Tide affects the ice in these regions. In areas of large tide ranges,
ice is piled against the shore. This is noted in the early stages of ice
formation and growth, At ebb tide, slush packed against the shore is

exposed to the influence of low air temperatures, thus freezing into
sheets of ice. At flood tide these sheets rise, break into smaller
fragments, and are driven against the shore where they are piled hap-
hazardly. Distortions in the bottom relief, tides, and, to a lesser
extent, normal dynamic currents cause local rip currents which, in

some local areas of bays and fjords, either prevent the formation of
ice or cause the ice to be thin and treacherous. Fast ice which forms
in some of the protected coastal indentations is fractured and open
cracks appear at spring tides. The effect of tides on the ice of these
waters generally is confined to limited areas and will be considered in
the appropriate sections of this study.

Davis Strait, the southern egress of Baffin Bay, plays a distinct
role in the cyclic history of the ice generated in these waters. Pres-—
sure systems moving into and across this area often cause great havoc to
the ice. Winds with accompanying sea and swell resulting from the passage
of low pressure systems across the Labrador Sea pound against the southern
boundaries of the pack, compact it, break up its peripheral ice, and narrow
the drift belt westward. Again, strong winds from the north exert immense
pressure on the pack, disrupt it, and expoSe large areas of open water to
the renewal of ice formation. When this occurs, Davis Strait becomes a
great flushing estuary through which discharges increasing masses of broken
fee. This changes the area of distribution and rapidly broadens the drift
pack to the south.

It was not intended that this study should consider the causes and
effects of sea-ice growth and formation. To do this would deviate from
the purpose and function. Occasionally in this report, reference is
directed toward the effect of some of the meteorological variables on
the behavior and physical characteristics of ice. This reference, then,
would contribute in small measure to the promotion of a more factual ap-
praisal of ice conditions and provide means for a more ready evaluation
of these conditions in terms of emergency descent and safe landing of air-—
craft.

This study did not intend to consider the behavior of ice, nor to its
cause and effect, within any specific area. However, in order to clarify
particular aspects of local ice conditions it was desirable to do so. To
have done otherwise would have involved considerations of a nature dissonant
with the purpose of this study.

Ice in Baffin Bay and Davis Strait does not form uniformly. Actually,
it can be considered not oniy a function of oceanographic and meteorological
variables, but also of latitude. Sea ice begins to form first in the upper-
most regions of Baffin Bay and spreads slowly southward into the waters of
Davis Strait. The freezing process continues southward, but takes place
first in the west and somewhat later in the east. As a result, coastal
waters in the north are frozen over with a fairly thick layer of ice, while
those to the south remain open and free of ice, Also, owing to the many
factors that influence its formation and distribution, ice is not uniformly

present even in many strictly confined regions of this area. Again, it.
is apparent that a balanced presentation of the distribution of ice mst
be made consisteitt with its development in space and time as well as its
many facets, Therefore, for the purpose of clearer presentation, the
region of Baffin Bay and Davis Strait has been divided into several
coastal and open water sections with a description of the ice from the
time of its initial significant appearance to ths period of initial dis-
integration.

Glacial ice in some forms is mech less dependent on the factors which
control the distribution of sea ice. Because of its nearly independent
nature, aspects peculiar to it are described in a separate section.

The symbols indicating ice features on the accompanying charts, are
those of standard Hydrographic Office ice chart presentations, Ice termi-
nology is that of H. 0. Pub. No. 609 "A Function Glossary of Ice Terminology."

B. BAFFIN BAY

Thule and Approaches - Generally, ice first begins to form in North
Star Bay in the beginning of October. In the latter part of the month,
it attains a thickness of as much as 15 inches and extends as a continuous,
almost flat layer, as far as Wolstenholme and Saunder Jer. To the north of
Saunder J it joins the fast ice formed earlier along the opposite shore.
As the Season progresses, the ice thickens and may reach 30 inches by the
end of November, In December it may attain a thickness of 40 inches,
growing thereafter month by month; in April and early May, it attains a
thickness of more than 70 inches.

The ice is thickest in the immediate vicinity of the shores, becoming
thin in the approaches to Wolstenholme and Saunder Yer where it has a depth
in the range of 4 to 5 feet. Small danger areas exist between Saunder 9
and the small islands of Kekertarssuit to the north, where the ice is often
very thin and disappears with first period of warming in the Thule area.

The ice of North Star Bay is quite smooth and flat. In some winters,
an upthrust of sea ice occurs in the shoal vicinity of the pier. Bergs
and bergy bits are present in the bay the year around and usually are
lodged in the ice. The greatest quantity of glacial ice is found in the
fjord itself and may be regarded as generally unsuitable for aircraft
landings.

Melting of the ice sets in during the latter part of May and puddling
is general in June. >

High winds may force the removal of most of the ice in North Star Bay
as early as mid-June; if the winds are absent, the ice will linger in the
bay as late as 10 July. The ice in the fjord north of Thule has a rough
contour, contains large quantities of glacial fragments, and is usually the
last to leave this coastal indentation.

Fast ice joins Saunder and Wolstenholme Jer and sometimes contains
many bergys and bergy bits. However, it seldom extends more than a mile
west of these islands, where the shifting Baffin Bay Pack is encountered.

Wolstenholme g to Kap York - Ice will begin to form along this coast
by 10 October. undisturbed, it will assume the character of fast ice,
in which cage it may extend seaward from 15 to 20 miles. Under these
conditions the topography of this ice is relatively flat, and pressure
ridges are few in number. The height of the ridges are 12 to 18 inches}
however, some will exceed 2 feet. Snow cover on this ice is fairly uni-
form and averages 3 to 5 inches with areas of 6 to 8 inches. Thickness
af the ice will vary from 2 to 3 feet in December and 3 to 4 feet by mid-
February, with local areas attaining a thickness as great as 5 feet.

This area seldom retains fast ice along its coasts. Strong offshore
winds tend.to cause long fractures parallel to the coast a short distance
from shore. When the fractures occur, a lead several hundred feet to more
than a mile in width will form from the vicinity of Kap York to Conical
Rock, northwestward to Wolstenholme %, and beyond. If the lead forms in
the period of February-March, rapid refreezing of the exposed water will
take place, so that within 2 weeks it will be covered with an ice layer of
approximately 18 inches, increasing to more than 2% feet in 3 weeks. On the
other hand, if the situation occurs during April, refreezing of the lead
will be progressively slower and probably will not exceed 12 inches. After
mid-May such a lead would remain open and the breaking pack ice would alter-
nately close and reopen it~ —

Parker Snow Bay is covered with flat, fast ice which is almost free of
any pressure ridges and remains in the bay independent of the ice along the
coast. ;

The inshore waters of this coastal section are infested with bergs and
bergy bits. Growlers are lodged in the ice in varying numbers. The greatest
numbers are in the vicinity of Conical Rock. The ice to the west generally
is infested with many bergs, some of which may exceed 200 feet in height;
although heights of 75 to 150 feet are most common,

Normally this fast ice breaks up in May leaving a wide shore lead.
Permanent fast ice still attaches to the coast from the vicinity of Kap
York to about 20 miles westward, It is irregular in its seaward projection,
varying from a few hundred to more than 1,000 yards. Tidal and basin
cracks cause large sections of this ice to break away until it is com
pletely removed by the end of June or first of July.

Kap York to Tasiussag Bugt - Fast ice first appears to the east of Kap
York in the early part of October, and gradually spreads along the coast to
the east and south. By the latter part of the month it reaches Nugssuag 9.
The boundary of this fast ice may be described as an are connecting Kap York
to Bushnans @, Bushnans G to a point 5 to 10 miles southwest of Bryants @,
extending southward to Thoms @, then to the western extremities of Holms and

Nugssuaq Ger. Thickness of this ice will be generally 3 feet by Jariuary
and 4 to 5 feet from mid-February to mid-April. Following this period,
gradual disintegration takes place and the ice will decrease in thickness
to 3 to 4 feet in May, and 3 feet in June.

Although fairly level and smooth, with comparatively few pressure
ridges (owing to its protected environment), the ice is heavily dotted
with bergs, bergy bits, and growlers. Some of the bergs will be as high
as 300 feet, although the average height is 150 to 200 feet. Greatest
banks of bergs are found off Kap York, immediately east of Bushnans
and south of Kap Melville, the east side of Thoms J, and the length of
the ice between Thoms and Holms fer. Growlers are found more frequently
between Holms and Nugssuag fer. Fewer growlers are found in the ice to
the north, the majority having drifted along the coastal waters to the
west of Kap York and Wolstenholme @.

Although there are great numbers of bergs and smaller fragments of
glacial ice, great stretches of flat ice which can be used for emergency
descent are present.

The fast ice begins to break and separate from the shore late in the
melting season. The area between Holms and Nugssuaq Per and north of
Holms % to the vicinity of Red Head, is the first to clear. This will
occur usually in the end of June. Cracks and puddles appear in the ice
by mid-July. The ice disappears by the end of July or early August
throughout this section of the coast except for Dedodes Fjord where bergs
and current eddies maintain remnant floes.

The coastal waters of Melville Bugt are never free of ice; glacial
ice remains following the removal of sea ice. In early August the gla- —
cier coast becomes very active, calving an abundance of glacial fragments
which spread seaward as much as 30 miles. These in turn follow the nor-
mal current pattern of the Melville Bugt waters and drift toward the
Crimson Cliffs and the waters to the west of Thule.

Melville Bugt - This bay is frozen over by the early part of November.
During the early weeks of its formation, passing storms tend to break the
ice and cause considerable rafting and ridging. Large quantities of this
ice apparently drift westward. The succeeding ice which forms rapidly
usually features less rafting and ridges. The ridges should be 2 to 4
feet with some exceeding 6 feat; however, they are separated by layers of
flat and fairly level ice which frequently have dimensions of several
thousand yards,

Calculations show that the ice in Melville Bugt generally should
reach a thickness of 2 to 3 feet by mid-January and 3 to 4 feet by March.
Locally, some of the ice will exceed a thickness of 5 feet. Ice continues
to grow slowly through April and, at times, into the early part of the
following month.

Snow cover is usually light, 4 to 8 inches with drifts of 12 to 18
inches,

The pack ice of Melville Bugt is seldom immobile. In February and
March, during the periods when this area is under the prolonged influence
of "flat" pressure systems, the pack is either stationary, or there is
very slow, local motion, At such times, the entire ice field becomes a
part of the fast ice which then appears to extend far beyond the normal
limits.

Of al] the ice in Baffin Bay, that portion in Melville Bugt appears
to be least subject to frequent breakup in the winter months. However,
fracture of the ice is a normal feature. Passing storms set the ice in
motion; leads may be expected to form along the margin of the fast ice,
on the lee side of bergs, and in areas where cracks resulting from thermo-
dynamic and kinematic influences are present in the ice,

Leads which form along the fast ice of Melville Bugt will be found
to the south of Thoms g. Their orientation parallels the fast ice and
attains widths of a few hundred yards to more than 2 miles, Their entire
length may exceed 10 miles. As a result of pressure from the north,
shorter leads develop in the northerly sector of the bay. Lenghhs of $
to 2 miles and widths of a few hundred feet to 1,000 yards are common.
Their orientation is along an east-west axis. Leads that form on the lee
side of bergs will. be of varying lengths as a result of pressure. Their
size will depend on the magnitude and duration of winds that pressed
against the ice. Generally, their width corresponds to the width of the
berg. Their length varies from a few hundred yards to more than a mile.

During January through March, the refreezing of exposed cracks and
leads begins immediately on exposure to the air. An exposed lead may
acquire a smooth layer of ice 18 inches thick within a little more than
a week, depending on the winds and temperatures. After a lapse of a few
more weeks, a lead of this sort may attain a cover of new ice more than 2
feet thick. The newly frozen leads in Melville Bugt may be free of snow
for considerable periods, therefore their movement can be detected from
the air, and their relative thickness and size can be judged. When the
lead is covered with snow, the snow layer generally will be light and
level °

The ice in Melville Bugt begins to break up on a greater scale in the
latter part of April. The first signs of the breakup are noticed along
the fast ice where the pack separates and forms the great lead known as
the Northabout Route. After a relatively mild winter the ice is fragmented
into blocks and floes in the region centered at 75°30'N and 67°00'W,
Giant floes and fields remain in inner Melville Bugt.° The ice in the area
of west of Nugssuaq and Holms fer and to the north as far as 74°20! also
will begin to break into smaller floes. Northwest of Duck fer polynyas
will form. Similarly, along a line connecting these islands with Conical
Rock, small irregular leads and polynyas will be present.

General fragmentation of the pack begins in the latter part of May
with accelerated breakup starting in the latter part of June. Inner
Melville Bugt, however, retains a number of giant floes and fields.
Puddling and rotting of ice begins off Nugssuaq and Holmes fer by the
end of June and becomes general throughout the area a few weeks later.
By mid-July large areas of open water are present. The Melville Bugt
pack, south of 75°N is fragmented inte brash, block, and small floes at
this time; the pack completely dissipates by the end of the month.

Tasiussaq Bugt to Disko Bugt - Bays and fjords in this section of
the Greenland coast become frozen by the end of November. The fast ice
advances seaward and rapidly engulfs all of the outlying rocks and is-
lands that dot these coastal waters. Their outer rim outlines the sea-
ward margin of the fast ice.

Thickness of the fast ice is generally 2 to 3 feet by early January
in the northern sector and by the latter part of January in the southern
sector. The ice will increase to feet thick and locally te 5 feet by
late February and March. Generally, the ice is flat and fairly smooth.
Pressure ridges are present most frequently near the margin of the ice.

Breakup by the fast ice begins as early as mid-May in Disko Bugt and
Vaigat, and by mid-June in the areas to the north. Sea ice is gone com-
pletely from these waters by mid-July. Only in the northern part of the
Sector there appear occasional remnants of ice as a result of the wind and
currents.

Climatological data indicates that snow cover varies quite extensively.
In the northern sector it usually is in the range of 6 to 8 inches and in-
creases to 12 inches in the south. Snow drifts, therefore, should be cor=
respondingly greater in the southern sector, Their estimated range is
from 12 to 15 inches in the north and 18 and 24 inches in the south.

The coastal waters abound in glacial ice; however, many of the inlets
and passages are free of glacial ice. Most of these inlets contain large
quantities of bergs, bergy bits, and growlers which break off the numer-
ous glaciers located at the head of the many fjords.

The Outer Ice from Tasiussaq Bugt to Disko Bugt - The sea ice west—
ward of the margin of the fast ice forms relatively late along this sector

of the coast. It is generally the least stable of any of the regions in
Baffin Bay except, perhaps, the area of the North Open Water. While the
freezing process envelopes all of Baffin Bay and Davis Strait in November,
the offshore waters from Disko Bugt to the vicinity of Tasuissaq Bugt
remain relatively free of sea ice. It is not until December that freezing
finally occurs.

As the freezing process begins and the waters acquire a thicker ice
layer, there remains, at distances of 10 to 20 miles offshore, a narrow

tongue of weak ice. This belt of weak ice is found the length of this
coastal section and varies in width from about 5 to 10 miles in the vicin-
ity of Tasiussaq Bugt to more than 25 miles at the approaches to Disko

Bugt.

Passing storms frequently open the ice and cause its general break-
up, Separating it into floes of many sizes and thicknesses. Large areas
of water are exposed which freeze rapidly and cover the area with layers
of new ice. Onshore pressure closes the ice causing considerable rafting
and ridging. Sea ice is usually in a state of great mobility and subject
to sudden and unpredictable changes. Sea ice appears last and is the
first to disappear from the eastern waters of Baffin Bay and Davis Strait.
A broad shore lead begins to replace it in early May when it begins to
eneroach the coastal waters of Disko and reaches Tasiussaq Bugt by early
June.

Disko Bugt to Séndre Strdmfjord - Coastal indentations and fjords
along this coast begin to freeze in the latter part of November and are

usually frozen completely by January. Because of the tidal currents, many
of the passages and some areas of the fjords are either open or are cov-
ered by a thin layer of ice. Ice forming in the fjords is usually flat
and smooth, It may attain a thickness of 3 feet or more by mid-February.

Breakup of the ice in the exposed sections usually begins in May.
However, in the fjords this occurs in the latter part of May and early
June. 4

Offshore, the Davis Strait pack may extend southward along the coast
from Disko Bugt to the northern approaches to Sgndre Strémfjord., The ice
first appears off Egedesminde in January, and extends southward to the
latitude of 66° or 66°30!N by February. Pressure from the south and south-
east will force the ice away from the coast and create a broad shore lead,
which may extend northward to the vicinity of Egedesminde.

In the northern part of the sector, the ice is similar to that found
off Disko; to the south it is composed mostly of new ice, broken into
block and small floes by winds, sea, and swell. In this area a broad
shore lead develops during the latter part of April. Occasional incur-
sions of the shore lead occur under strong, persistent pressure from the
northwest. This brings in ice from the fringe of the pack to the west.

Gape Chidley, Labrador to Cape Dyer, Baffin Island - Hast Hudson
Strait and the coastal area to Cumberland Sound are influenced by strong
tides where ranges may exceed 35 feet (Frobisher Bay). As a result of
the tides and the strong south-setting currents, a small amount of fast
ice is formed along the shores. Ridges exceeding 7 feet usually occur in
the ice when developed in the close confines at the head of the great
funnel-like bays. Otherwise, there is rafting because of piling by tidal
action during the early stages of formation and growth of the fast ice.

Fast ice which develops in the coastal waters exposed to the sea, normally
is confined to two narrow sections of this coast, the northern shores of
Loks Land to the Leybourne Islands group at the approaches to Cumberland
Sound, and Leopold Island to a few miles north of Exeter Bay.

There is no fast ice off Cape Chidley, the northern shores of East
Hudson Strait, or the islands guarding the appreaches to Lower Frobisher
Bay. Tidal currents prevent the formation of fast ice off Cape Chidley.
Only a narrow ice foot is found along the northern shores of east Hudson
Strait. The same is true of Resolution, Edgell, and Lower Savage Islands,
as well as the southern coast of Loks Land. The tidal ice foot is also a
prominent feature of Lower Frobisher Bay. Fast ice is encountered only
in the protected bays and sounds of this body of water. Although Upper -
Frobisher Bay is fairly locked in fast ice, swift tidal currents keep
many of the narrow channels open through the winter; still others acquire
a temporary thin layer of ice which breaks at high tides and under pres-
sure of winds. Ice over the tidal flats is extremely rough, rafted, and
ridged, Only the ice of Ward Inlet, Wayne Bay, and the center ice of the
upper bay is flat. Ice begins to form in this region in the latter part
of October and should cover Upper Frobisher Bay by mid-November. A thick-
ness of 3 feet is expected by January, and 4 to 5 feet by March.

The nearshore ice normaliy has a heavy snow layer, 6 to 12 inches,
with drifts of 2 to 3 feet; the flat ice has a more uniform and lighter
cover, 6 to 8 inches, with occasional drifts of 12 to 2h inches,

The outer margin of the fast ice north of Loks Land extends approx-
imately from Osbon Bay to almost 64°30'W, skirting a distance of 2 to 4
miles seaward of the north of Hall and Hudson Islands and Loks Land. Here
jit forms an embayment and turns eastward to within 4 or 5 miles of Monu-
mental Island and curves northward to within a few miles of Cape Murchison
and continues to skirt the coastal islands. The ice encloses Leybourne
Islands and turns into Cumberland Sound.

To the north, the fast ice generally is confined to the protected
waters. Its outer boundary extends from the northwest tip of Leopold Is-
land to the east side Muingniak Island and encloses the tay on the north-
east side of Kekertuk Island. The extent of the fast ice terminates at
this point. However, it resumes its coverage in the southern entry of the
passage on the west side of Angijak Island and envelopes the northern
shore of this island as far as its eastern terminus. From here, it pro-
ceeds northward to Cape Walsingham, thereafter curving into Exeter Sound,
almost jutting the coast to the north, and ending a few miles south of
Cape Dyer. This fast ice is similar to the ice to the south, It forms
in the latter part of October and very likely progresses seaward to the
described margin by the end of November, Its thickness is estimated to
be 3 feet by early January, increasing to 5 feet by March. However, not
all of the shore waters in this region freeze over completely. Tidal cur-
rents funneling through some of the passages tend to keep the islands north
of the Leybourne Islands free of ice, The ice-free areas are found in
_ passages having a north-south orientation,

The fast ice is generally flat and is normally free of glacial frag-
ments. A small number of bergs, and bergy bits on occasion drift into
some of the bays and ground. The ice begins to break along the margin in
the early part of June and the coast is clear in early July.

The snow layer on the ice in the vicinity of Loks Land, varies from
6 to 8 inches and decreases northward to 4 inches. These depths will vary
considerably as a result of drifting.

The ice seaward of the fast ice margin is in motion constantly. It
first appears locally in early November and moves eastward until it covers
the sea to within 50 or 60 miles of the Greenland coast at the latitude
of Cape Dyer. It turns southwestward toward Cape Chidley where it appears
in the early weeks of December as a belt of 40 to 60 miles in width.
Augmented by the ice from the waters to the north, the ice enters Baffin
Bay through the sounds of the Canadian Archipelago. The drifting pack
has a complex composition with ever-changing concentration and distribution.

During the winter and early spring months, the inner pack is composed
largely of medium and giant floes. Its periphery frequently is broken
into small floes and blocks because of the action of sea and swell and
sudden changes in pressure. Floes are frequently the product of consoli-
dation; they may contain ice of different ages and stages of growth.
Waters undergoing rapid refreezing often retain large distributions of
newly fragmented ice. Newly formed floes are broken and the process is
renewed.

Thus, the ice is unreliable from the point of thickness, dimension,
and topography. Locally formed ice is subject to frequent breakup, and
the process of consolidating the ice produces ridging. Floes drifting
from the north are often heavily ridged and hummocked.

During the latter part of March or April, ice drift increases. The
pack broadens considerably and changes radically in distribution and con-
centration. In May it reopens and the contribution from Baffin Bay dimin-
ishes. Thereafter, the area of ice rapidly decreases leaving ice patches
and belts by the latter part of June. The pack practically disappears by
August.

Glacier ice is found in this region during the entire year. Bergs
discharged from Disko Bugt drift within the boundary zone of the pack and
converge on Resolution Island. Those drifting off the coast of Baffin
Island are of many varities and represent products of the glaciers in
Melville Bugt, the region to the north of Thule, and the coast of Elles-
mere Island.

In the vicinity of Cape Dyer and southward to the latitude of Cumber-
land Sound, strong northerly winds produce east-west leads several miles
wide and 40 miles or more long. They are usually ice free; however, when
formed in March and April, they freeze over rapidly. The new ice formed

10

in these leads attain a thickness of 15 to 20 inches within a few weeks.
Storms and the south-setting currents break the new ice into small and
medium floes, mixing them with the surrounding ice. Pressure from the
west forces the pack seaward and exposes broad leads between the fast ice
and the pack, Also, within the pack irregular north-south leads are asso=
ciated with this western pressure.

The shore lead and the leads in the pack are short liveds the pack
closes against the fast ice when the pressure from the west abates.

Cape Dyer to Bylot Island - The fast ice along the coast of Baffin
Island resumes a few miles to the west and north of Cape Dyer, aligns the
eastern coast of the island, continues northward, and completely surrounds
Bylot Island. Forming first in the month of October in Eclipse Sound and
Navy Board Inlet, it rapidly develops eastward and southward to the vicin-
ity of Cape Dyer toward the end of October or early November. Its sea-
ward advance is broad and rapid. At height of development, the ice extends
8 to 10 miles at Bylot Island, broadens to 20 to 30 miles in the region
of Cape Christian and more than 30 miles in the vicinity of Home Bay,

At Padloping Island the ice undergoes very rapid growth during the
first month of development, and by mid-December measures as much as 30
inches in thickness, Hereafter, growth of the ice is retarded, but con~
tinuous. In the latter part of March, this ice may exceed 80 inches in
thickness, In early May the fast ice facing Cape Christian may attain a
thickness of 3 to 5 feet within the first 2 miles of its eastern margin.

The surface of the fast ice along this coast of Baffin Island is
rather flat. Pressure ridges are few; those formed in the ice during its
initial phases of growth are not prominent. Few attain greater heights
than 12'to 18 inches. However, some of the marginal ice, notably that to
the north of the latitude of Home Bay, is usually very heavily ridged,
especially along the edge which separates the fast ice from the pack.
Here pressure ridges reach considerable dimensions, often exceeding 10
feet. They may be found in the marginal zone of the ice for distances
of 2 miles,

To the north of Eclipse Sound and Pond Inlet, the area is covered
with a smooth layer of ice. However, the fast ice which encloses the east
and northeast coast of Bylot island has ridges resulting from the great
pressures exerted against the shores.

Lodged in the fast ice, throughout the length of Raffin and Bylot Is=
lands, a varied collection of glacier and polar ice is found. This glacial
ice is very sparse when compared to the eastern portion of Melville Bugt.
However, the fast ice contains certain types of glacial ice, flat tabular
bergs of relatively inconspicuious heights, extending 5 to 10 feet above
the surface of the sea ice, Ice of this type rarely is observed elsewhere
in these waters. Its detection from the air is difficult when the ice is
covered with fresh snow. .These fragments are not numerous and may be found

LL

in broken clusters of small sizes near the shore where they were grounded
prior to the formation of the sea ice. When lodged in ice over deep waters,
they exist singly and are larger in size, perhaps several hundred yards,

Snow is distributed uniformly throughout this region. The snow cover
is estimated to be 6 to 8 inches with drifts of 12 to 18 inches.

The boundary of the fast ice begins to recede in June, In early July
large sections of the ice break away becoming part of the great pack.
Many sections of the coast are ice free in the latter part of the month,
and in early August all of the ice disappears.

Bylot Island to Ellesmere Island - Fast ice is formed in the indenta-

tions of the southern coast of Devon Island. Currents and tidal influences
cause the ice to move continuously in the north side of Lancaster Sound,
This breaks the ice and forces it into Baffin Bay.

A half-mile belt of fast lice normally is found on the east coast of
Devon Island, from the southern side of Philpots Island to the entrance
of Lady Ann Strait where it narrows to the coast. Its surface is rela-
tively smooth except for a marginal zone in the northeast where ridges are
formed as a result of pressure from the north and northeast. The snow
layer is fairly uniform and corresponds to the snow layer found on the
ice to the south.

Shore waters off Devon Island begin to freeze in October. Fast ice
is firmly established in November. Its rate of growth and thickness is
comparable to that at Bylot Island. Breakup of the ice commences in the
latter part of June and is general by July. The coast is clear at the
end of July or early August.

Lady Ann Strait is free of fast ice. Locally formed ice breaks as
the result of gurrents and pressure from Jones Sound and Baffin Bay.
The floes are smaller and their concentration varies with changes in the
passing meteorological pressure systems.

Fast ice occurs on the squthern coast of Coburg Island, enveloping
the island, and closing Glacier Strait. It continues northward along the
coast of Ellesmere Island into Smith Sound. With the exception of Glacier
Strait and the coastal indentations in the islands, the ice is rough and
has pressure ridges. It contains large quantities of polar ice, which
drift into this area through Smith Sound. The margin of the fast ice ex=
tends a few hundred yards to the east of Coburg Island, arcing toward
Smith Sound at a distance of 10 to 15 miles from shore.

Sea and swell activity gradually breaks up the marginal zone of. this

ice and forces its boundary westward, Accelerated breakup of the ice takes
place in July. The shore is free of ice by the early part of August.

ae

The Baffin Bay Pack - The Baffin Bay Pack is east of the fast ice
which extends the jeneeh of the Baffin Island coast north of Cape Dyer
and Bylot and Devon Islands. It forms in the northern area during the
early weeks of October, expands southward and encloses all of the waters
of Baffin Bay and central and western Davis Strait in November, Its
composition and structure has many local variations. The Baffin Bay Pack
contains floes of different sizes, thicknesses, great pressure ridges,
young ice, polar ice, and ice of land origin. The pack grows in size
during winter, Stoms will cause fragment shifting of the pack and the
opening of great leads. New and winter ice are compressed and pressure
ridges are formed. Large sections of the pack drift southward through
Davis Strait, enter the Labrador Current, and the newly exposed water
areas acquire new layers of ice. Therefore, because Baffin Bay and Davia
Strait ice is replenished constantly through the season of growth, the
pack is vast and heterogeneous,

Because of geographic dissimilarities, the pack can be separated inte
two sectors: the southern sector extends from Cape Dyer to the latitude
of Home Bay,and the other section, to the north of this latitude, The
southern sector responds more readily to changes in pressure. Strong
northerly winds cause very broad east-west leads that extend nearly the
width of the pack. They may form singly, or in a parallel series separated
from each other by wide bands of densely concentrated floes, Winds of a
westerly component produce short, narrow, and irregular leads with a gen=
eral north-south orientation. Finally, the coastal blocking of Cumber-
land Peninsula and other controlling factors bring about the formation of
polynyas and many small leads in the area northwest and east of Cape
Dyer which will close upon the slightest change in the condition of the
pack.

During the months of intense ice production, January through mid-
April, newly opened leads readily freeze. Within. a few weeks they may
acquire a layer of ice 18 inches or more thick. However, renewed stresses
on the ice break up the new ice into floes of different sizes which mix
with the surrounding ice of the pack.

The western side of the pack ice contains floes of hummocked polar
ice and floes that are extremely rough and very heavily laced with pres~
sure ridges. Some of the ridges exceed 10 feet in helght. Also found in
this area are floes whose surface features resemble a consolidated mass
of crushed upended blocks. On the other hand, the eastern side of the
pack contains a high percentage of giant floes in which pressure ridges
are Widely separated; the surface of the ice between them is relatively
smooth. These floes have frozen within them smaller floes of thicker ice
whose ridges protrude above the surface and often escape detection owing
to the snow layer that covers them.

Thickness of the ice in this sector of the pack is variable. Older
ice, formed in autumn, attains a thickness of more than 30 inches by
January, and may exceed 4 feet by March. Within this pack thin ice is
found which formed recently in leads or polynyas.

18)

Snow cover is irregular. Older ice may have 8 or more inches of
snow, while new ice may have a few inches, or be snow free.

The northern sector of the Baffin Bay Pack is more stable than the
section to the south. Large expanses of the pack remain relatively immo-
bile for extended periods, This is particularly true of the central,
eastern, and northeastern portions where large expanses grow uninterrupted.
Exceptions are found in the north, in the reaches of the North Open Water,
and in the west where changes in the ice occur with regularity.

From January to April, the region of the pack's greatest stability
is composed principally of medium and giant floes and fields. The ice is
interspersed with pressure ridges 8 to 12 feet in height. Large areas of
relatively flat ice separate these ridges. Small ridges, ranging in
height from 1 to 2 feet usually are present in varying concentrations
within the flat ice. Relatively few bergs are found in this ice.

In January floes formed in the autumn may attain a thickness of 3
feet; it may increase to 3 to 5 feet by March and April. Snow cover gen-
erally is 6 to 8 inches with drifts of 12 to 18 inches.

To the west, the pack ice that drifts along the fast ice has greater
mobility and contains ice of varied types; polar ice, ice formed in
Lancaster Sound, and that which has formed or drifted into the North Open
Water. Glacier ice also is found in a larger proportion. Most of the
ice found along the Baffin Island ice is composed of medium and giant
floes and fields. Its surface is rougher and has more pressure ridges
than that to the east. East of Pond Inlet and Bylot Island, pressure
ridges have been observed to exceed 15 feet in height.

The ice is comparable in thickness, to that previously described
except in isolated areas that contain ice from Lancaster Sound or the
North Open Water.

The ice asually is disturbed in the pack east of Cape Byam Martin and
for 50 or 60 miles eastward of the Lancaster Sound egress. Here, unlike
the central pack, the ice is in a state of greater mobility and changing
concentration and composition. Leads appear to open readily and close
before any appreciable growth of new ice takes place. Here, too, is often
found ice which at one time was subjected to great pressure, producing
ridges exceeding 15 feet in height, or floes that were compressed and
crushed into masses of ice with rough surfaces.

The ice of the North Open Water is seldom stable in character; it
never attains great thickness because of frequent breakup. Winds, light
or strong, tend to clear great areas of this water and form polynyas which

soon acquire a cover of frazil crystals and young ice.

The destruction of the Baffin Bay Pack occurs along its entire periphery,
except for the ice which remains on the coast of Baffin Island. In June,

when melting starts, the pack boundary in the area of the North Open
Water contracts and moves southward. Its western boundary facing Devon
and Bylot Islands recedes eastward. The Melville Bugt Pack begins to break —
in the region of the Middle Passage, along a line connecting Upernavik
and Wolstenholme %. Along the coast of Greenland a broad shore lead
forms, gradually moves northward into Melville Bugt joining the Northabout
Route, and the great pack recedes westward. The drift of the fragmented
pack gradually narrows to the south and withdraws toward Cape Dyer. By
the latter part of July the pack is rotted and reduced in size. The fast
ice of Baffin Island, already deteriorated, is leaving its coastal anchor-
age. In August the pack becomes a floating mass of rotten floes that
rapidly fall apart into brash and block. By mid-September the pack dis-
appears.

During periods of optimum ice growth, passing storms greatly increase
the pressure on the Baffin Bay Pack. On such occassions large sreas of
the pack are forced open forming leads. Some of the leads rapidly acquire
fresh layers of hard ice while others close and form pressure ridges along
lines of contact. The ice of the newly frozen leads is readily recognized
from its smooth surface and color. The color of the newly formed ice
depends greatly.on its thickness. It was observed that the thickness of
dark and gray ice ranged 6 to 8 inches, of lightest gray ice 8 to 1 inches,
and almost white 14 to 18 inches. In the extremely cold months of February,
March, and April, ice formed during periods of relatively light winds
takes on a glass-like surface. This ice may reach a thickness of 20
inches within a two-week period.

Leads of the type described above are found in the northeast and cen=
tral part of the pack, They usually have a northwest—southeast orientation.
They frequently are irregular in size and may vary in width from a few
hundred feet to several hundred yards and attain a length of several
miles. Occasionally, they appear as a great network that may extend for
distances of 50 to 100 miles.

The leads that form in the western part of this section of the pack
undergo rapid changes; hence, the newly formed ice usually is broken up
before a lead attains appreciable size.

Under the influence of westerly winds, the northern sector of the
pack will separate from the Baffin Island fast ice, and a broad lead will
form from the vicinity of Home Bay to the latitude of Pond Inlet. Ite
width depends on the duration and magnitude of the wind force exerted
against the pack, It may vary from a few miles to more than 20 miles.
Its life, however, is short and the pack soon crushes against the fast
ice and creates great ridges.

Leads that form in the southern sector of the Baffin Bay Pack also
have a short life. The high mobility of the pack and the rapid changes
which occur as a result of different pressures, open and close leads
frequently.

15

C. GLACIER ICE

Baffin Bay and Davis Strait are the source of the majority of ice-
bergs of the northern hemisphere. The inshore water of Melville Bugt has
a massive glacier coast. Into the Melville Bugt waters great numbers of
bergs drift from the south. Here, even greater numbers of bergs originate.

Icebergs are present in Baffin Bay and Davis Strait during all sea-
sons, Their number and distribution varies with the season and the year.

There are approximately 100 active glaciers on the west coast of
Greenland; 20 of these are regarded as significant producers of bergs.
The bergs that are calved along the coast north of Disko Bay assume a
northabout drift in the coastal waters of Baffin Bay. They enter Melville
Bugt where they augment the thousancs of bergs that lie in the nearshore
waters.

Bergs vary in height, from rather insignificant masses 30 to 50
feet high to giants that occasionally attain heights of 400 feet. Their
shapes are as varied as their sizes. Few, however, are of the tabular
variety common to the Antarctic. Although approximately 7/8 of the mass
of the berg is submerged, measurements indicate that anywhere from 1 to
5 times the height of the berg actually is submerged.

Winds and surface currents have little influence on the direction
or speed of the drift of bergs because of the immense mass of the sub=
merged portion. Thebberg's rate and direction of drift is a function of
the magnitude of the speed and direction of the subsurface currents
acting upon it.

In addition to icebergs there is an abundance of other glacier frag-
ments (bergy bits and growlers). The number and distribution vary with
the distribution of the bergs and the intensity of the calving process
of the glaciers at the time of calving and at the time of mass disinte=-
gration of great numbers of the older bergs.

Some of the glaciers on the west coast of Greenland, such as
Jakobshavns Isbrae, may calve the year round. Those to the north, how-
ever, are active for a relatively short period. Glaciers located north
of Disko and south of Melville Bugt usually begin to calve in the latter
part of July, and those in Melville Bugt in the beginning of August
coincidental with the final removal of the fast ice. Glacier activity
reaches its height in the few weeks following initial calving. Soon vast
quantities of glacial fragments move out of the fjords and bays into
coastal waters and slowly drift northward. In Melville Bugt, coastal
waters fill with glacier debris as much as 30 miles to the seaward,

Toward the end of the month, the mass of floating glacial fragments,
in the forms of bergs, bergy bits, and’ growlers will have drifted into
the area of Kap York and westward along the Crimson Cliffs. The debris
of the glaciers, pulverized glacier ice, and growlers are subjected to
fairly rapid melting, leaving the heavier masses of ice. By mid-September,
when autumn begins to take full sway, great numbers of bergs that were

16

subjected to summer influences begin to disintegrate. Once again the
coastal waters are filled with growlers which drift toward the western
waters of Baffin Bay. In October, when the winter ice forms, the growlers
lodge in the new ice and drift where the winds and currents direct them.

Currents often ground icebergs into shallow waters. When grounded
near shore, they may serve as anchorages for the newly formed fast ice.
When carried by the currents into deep waters, the bergs continue their
independent course impeded slightly by the new ice. It is only when the
ice becomes formidable in itself, by means of its own hardness and size,
that a berg's drift may be appreciably affected; nevertheless, it is not
dominated by the drifting ice, Great pressures that force a violent
movement of sea ice will cause extremely hard and substantially thick ice
to crumble against the windward side of bergs and will create on their
lee side leads of considerable length. In the periods of intense cold,
such leads (unlike the leads that result from the separation of great
floes) quickly refreeze and create fairly broad lanes of smooth and flat

ice.

During the period when the waters of Baffin Bay and Davis Strait are
covered with ice, the greatest concentration of bergs is formed in Mel-
ville Bay and southward along Greenland coastal waters. Fewer bergs are
found along Baffin Island, although here are located many of the bergs
discharged from Kane Basin and the glaciers of southeast Ellesmere Island,

Alf

=

~ ITGENERAL CIRCULATION

|

°
ito)

+

°

[o)

wo

°

ite)

ive)

°

(=) |
ive)

°

Lo

ive)

°

(o)

~

tS
ve

ROMFIORO
ICE SYMBOLS

Some young oS)

ice in
winter ice

NORE st!

if
a hs] pA
—atary| WV
Kh SX Sq

\

~~| Leads off fast
1X} ice refreezing

dvancing
southward

|

Young ice broken
polynyasrefreezing

Figure 2

Js
K

ER OE
OY A iy Yi j Ke \ SS
aul i f z } Yy
£4 SOSSKEE
Y Ui, (oy eS
0 Lax NM J WY
x GY,
MA Wy Y) Ysa
ik Y S
4 “a as mene oR sy Ry rt
\ YRYLA LP

2)

/

«| Lead may
fast ice limit

ES

Stable ice |\15¢
ee

develop along

19

Icebergs (many) AX
ebergs (few) ZA
°
a||60
rowlers (many)
a

ergy bits and
jergy bits and
rowlers (few)

February
Thy

Unstable ice with

young ice

ICE OF LAND ORIGIN

tatted eo AAA
idged Ica AAA

ICE SYMBOLS
TOPOGRAPHY
lummocks 0

SS
Sid

h
KS

iD
S@NDRE sTROMFIOR!

pressure ridges
ent than to west

(Se
thes
hx V Wc

. Nis Il
4

broken

\ cf
SESS
TER OSA

iN!
iG
is
YX,

Leads and cracks frozen or

freezing;
less promin

A
>

LD
=

Ice unstable,
and in motion

ZN)

Yon

Se

ANZA
S aN
|

©
Oo
ol
©
et
=)
Ce]
~~
n
i=]
s
D>
i=]
i=
°
>

LS

Y LO
=
| °

~ ]

<
<>
<>
a

.

and ridged
=
Ice unstable

Lead open along fast ice]
Local areas of open
water in fast ice

west winds

when under pressure of
¥ Ice rough

Fast icel?@

|
Se

Ice rough, ridged
and unstable

Figure 3
20

‘

a
a

Icebergs (many) Ay
Icebergs (lew) ZA

leads
ICE OF LAND ORIGIN
Bergy bits and
growlers (many)
Bergy bits and
growlers (few)

'

mmocks 0
ER FEATURES

s5 2 23

TOPOGRAPHY
Hi

Leads covered with new
ice and freezing
over slowly

N-S belts of weak
ICE SYMBOLS
WA’

young ice:
beginning 20-30 miles

Fast ice in fjord
from entrance

Ztneaxc

0.5 to 0.
08 tol.

Leads frozen, pressure ridges
less prominent than to west

in constant state

of change

Ke am

Vg GZ

Figure 4

<>

op
SSR

SCS

NxM mY
ng WE &

oe

Young ice unstable

ne KO
y Los feet

>

>

>
15

Leads open
ice unstable

Region of heavy
Leads freeze over;
ice less stable

pressure ice
open water within

Small bodies of
fast ice

us)
=|
Cs}
a
oD
3
°
fa
o
o
ol
»
wn
Ls}
A

us]
©
to)

un]

orl
fa

Ice frequently
Marginal zone of

21

65°

a

ind

rey bits

freeze
th,
y latter

Fjord frozen from
S| 20-30 miles of egress
c

a
PSS3] WATER FEATURES Be

rage.
t rage
te rage
erage (no water) — [X25 Crack ere growers (few)
id
lynya

c
Cc
2
:

G@NORE gTROMFIORO

=

Leads and cracks
earl
f

y part of mon
reezing slowl

IN \

7 SSO WY @

QnKAt Ko sesny (As
Nes ens

hy
a=

VEG

Part of month
Ice unstable and d
in constant motion |?

Weak young ice, pol
y ynyas and
Occasional floes of rough ice

50)

=,

KaX

,| Open areas
i in fast ice

Flat floes |FAZRSS
and fields

Pressure
ice
x a
0,
B,
Broad lead
opens with
west winds

Figure 5
22

mn
m
eZ

20 to 50 miles from|/65°

Fjord frozen from
upper end

NORE STROMFIORD

2=
ef
Ss?

breaking up

CONCE!

developing

SALSA,
YoL2

Ice moving
south through
Davis Strait

Ze

Yr
Yi;

Figure 6

a
5

irs

i

)}
ah ESCH,
A ee

ZZ

Unstable ice

rough along
shear zone

Ice in motion
much ridging an

hummocking

23

Leads and polynyas
developing along fast
ice boundary

Floes off edge of
pack with off ice

Lead develops along
fast ice boundary
with offshore winds

pRE STROMFIORD

Ice in ser
motion

Central part of
fjord breaking up
by mid-June

Puddling of ice begin-
ning south of 73°N; ac—
celerated fragmentation
of fields and floes
throughout Baffin Bay and
Davis Strait; fast ice
leaving shores in south
and narrowing in the
ne Bul 2 ud mee uy mood =. CONCENTRATION ag Bead ICE OF LAND ORIGIN |
and polynya SPMGPOASUNG) oF coverage FREE] Rafted ico AA cebergs (many)
in size and number; pack 011 10 05 coverage Ridged lea AAA leeberas (few) ZA
Pataca case \ aBoOnexED I] PEreaO@ tetises
reaking an oundar . 08 to 1.0 coverage
Beceediig westward; zs y NS Lo coverage (no water) ebseay WATER FEATUR'S ey
boundary North Open
Water moving southward

70°

55°

50s

45°

"4,

Ui
s
d
Ss

4
SS
NS
table 2) W
isintegrating | /
ea ice OLD we
C4

Fast ice rotting and
breaking away from shores;
sea ice rapidly disintegrating

FROBISHER Bay
vO
y
S

'G
J
y

hs
2

\

LLL LLLP

GLIA LLLLLLL ALLL,

CONCENTRATION

5

Figure 8

25

S@NDRE STROMFIQRD

ICE SYMBOLS
TOPOGRAPHY

ICE OF LAND ORIGIN

ICE SYMBOLS
CONCENTRATION TOPOGRAPHY ICE OF LAND ORIGIN
Rafted Ico AA
Ridged lea AAA Icebergs (few) AA
Hummocks © — Bergy bits and
growlers (many)
3] WATER FEATURES ergy bits and.
Crack growlers (few)

Ice rotten and rapidly ~~ S
disintegrating; glaciers calving |¢ Poynys, CD

75° 70° 65°

<0.1 coverage
0.1 to 0.5 coverage
05 to 0.8 coverage
0.8 to 1.0 coverage

1.0 coverage (no water)

Figure 9
26

705 65° 60%) 55a. 50° = ag

FROBISHER Bay

oan)

ICE SYMBOLS

CONCENTRATION TOPOGRAPHY ICE OF LAND ORIGIN
<D.1 coverage Fes] — Rafted les AA leabergs (many)
0.1 to 0.5 coverage NS Ridged leo AAA — Icebergs (few) ZN
0.5 to 08 coverage [| Hummocks 0.0 Beray ip and ,

< . growlers (many
Sea ice dissipated in B Aaa BSS) warer rearunes tare a

1.0 coverage (no water) eee
i Crack growlers (few)
Baffin Bay; waters north ee

of Baffin Bay freezing over 2 Polynya CD

Figure 10
27

fa OO

SS

MFJORO

ICE SYMBOLS
CONCENTRATION TOPOGRAPHY ICE OF LAND ORIGIN
<0,1 coverage Rafted ico AAA Icebergs (many) du
Ridged Ica AAA Icebergs (few) ZA

Hummocks 0 © Bergy bits and
0.8 to 1,0 coverage Browlers (many)

a = A RSS2] WATER FEATURES ergy bits and
Young ice fo rming northern - LO coverage (no water) — ROSSI ack ewer” gromers (lew)
Baffin Bay and in protected| | Lead
bays and inlets Polynya GD

0.1 to 0.5 coverage
0.5 to 0.8 coverage

Figure li

28

NS

US

Young and new
ice frequently
broken

Young fast
ice developing
Seaward

Young ice advancing into

CONCENTRATION
<0.1 coverage
0.1 to 0.5 coverage

05 to 0.8 coverage
0.8 to 1,0 coverago

northern Labrador Sea;

1,0 coverage (no water)

{
fast ice along Baffin Island;]|.
North Open Water unfrozen ik
1 70° 65° 60° a)3}?
Figure 12

29

ICE SYMBOLS

TOPOGRAPHY
Rafted ea AA
Ridged lea AA,
Hummocks 0.0,

iesetee

WATER FEATURES.
Crack
Lead

Polynys CD
50°

NX

30°

65°

ICE OF LAND ORIGIN
Icebergs (many)
Icebergs (few) ZV

Brgy bits and

growlers (mary)

Bergy bits and

iowlers (lew)

December
ged Ico AA Icebergs (few) LA
mocks C) —Bergy bits andy

growlers (many)
ER FEATURES Bergy bits and
growlers (few)

ICE SYMBOLS
WAY

p>
ates

water) oe

Fast ice
y
O53". :
Pp
XS —

Young ice
near boundary
Many leads

Ice in
motion

n
S
i}
om
ra)
Ce}
fa
»
i=
o
o
i=}
i}
o
wn
tc}
i=}
|
>)
i}
>

and development

=I
a!
o
3)
Al
io)
=}
eI
i)
ral

ites <

cKO

ive)
oO

x

.

z
Zope

‘

&

FROBISH, i
eB ER Bay gy

o>

Be

g

Ridging alon
shear zone

Figure 13
30

80° 75° 70° 65° 60° Se 507 ae &
aie] als
d LERT | of WN
ie ie WS

of 7
) Humbotdt
Gletscher|

| Herbert »
a,

wi

“82 QNorth s
lggesy Soy
Conical Rock”

‘Ss rs
Sidebriks Fjord) ©
Bushnans o a
Thoms 9 <>
Melville oe

Jens ommelfinger
Soph Ge nig Thum)

Holsteinsbor’ <Zek
x f/
oe Exeter Bo:
oe ieee
dg gd? @ Cape Walsingham simlutak 6 °G AT
AS | > —
OY JO Angijak Island Se

Kekertuk Island gukKertorPe®

4

oo, >
| Edgell Island
Resolution Island

Pear Chidtey
4

Ungave Bay

j LABRADOR
Be re: 60°
70

Figure 14
31

BIBLIOGRAPHY

CANADA, DEPARTMENT OF MINES AND TECHNICAL SURVEYS, GEOGRAPHIC BRANCH.
Canadian Ice Distribution Survey; project presentation, Ottawa,
Canadas 1951.

DUNBAR, M. J. Eastern Arctic Waters, Canada, Fisheries Research Board,
Bulletin 88. Ottawa, Canada. 1951.

U. S. NAVY, HYDROGRAPHIC OFFICE, Manual of Ice Seamanship, He. 0. Pube
No, 551. Washington, D.C. 1950.

~- - - — Sailing Directions for Baffin Bay and Davis Strait, H. 0. Pube
Noo 7 ° Washington, D.Co 2d ed. 1951.

32

€L-t1 “OH

IysuUIWwDy “Ss Aasuayy -404sND

41D4sg S1ADG
puo Ang uljjoge ul
23] yo uolNngisasig roars

221 uo Buipuvy 4y043d41y

syuauin>y

224 jD12D19,

a>| - (UsaIsa,) PUD |UesI5)
>} - (usays09)

IIa up'!pouo’)

2>| = 4'1D4dS Stang

a3| - Avg uyjyog

€lL-41 “O'H

tysuiMDy “Gg Asuat{ s404sND

sip aig S1ADq

puo Aog uljyog ut
O32) yO UONNGINSIQ “abd

221 uo Buipupy syo4ds41y

s4ueuiny

2>| jo1s0(9

@3| - (Usaisa,,) pudjuse15
a>) - (usays09)

21y24y UDIPDUD>)

@2| - 4104Ig SIADG

22) - Avg ulyjog

168S1 "ISIW "UO “HH SO pelylsuept Buiguiad SNOIABIG

"pessnasip si uonngiss
“sip 93! jprapjh jonuuy “uOINNgi4jsip joNuuD joNsN
4iays Aq peqiuidsep asad sainjoa; d1ydo4sBodoy 42440,
*suoiipuo> Buisinda4s Ajjonuuo sapun Ajjoi2adsa soap
Sulpup| 4jD4duID |Sjqissod 40) paqiidsep si AydosBbodo;
2>| “passnosip 2ip eo oes yo uoNngisstp as
PUD UOINDINIID seIDM JO SINSIsG;DDIDYD |DsBUaC

(El -dl “© “H) “ssspy> py “dZe
"GS6l Asonunp “1ysUIuiDy “5 AlusH Aq “LIWALS SIAVG
GNV AVG Niddvd NI 3D! 4JO NOIWNGIYNLSIG
231440 21YdosBoiphyy Annoy "5 “A

{16851 “2S'W “U “H SO peytsuap: Buyuiud snoiAaig

“pessnasip si uongiiy
“SIP a3! jo1s0j6 jonuuy “UOINNGI4jsip jONUUD DASH
419s Aq Peqiussep 310 sainina;, 21ydo sBodoy 42410
"sUOI41puod Buisinoas A\jonuuv japun Ajjpoioedsa saain
Buipuo, 44043410 @/Gissod 10; peqiidsep s! Ayudosbodoy
32] “pessnosip aun eo: oes 4° “YOlNgiuisip aus
puo YUONJOINS4ID 42j;0™ jo SINS tsaysDIDYD JO 4auUec)

(EL-d1 °O “H) “s¥oyr> pl “daze
SS6l Asonuof “ysUIWDy “¢ Asst Aq ‘LIVALS SIAVG
ONY AVG Niddvd NI 3D! 3O NOILAGINISIG
22140 214do sBoupAty Anant a al

fl -G1l “OH
sysuiwoy “G Asus}, <404ynD

4ID4IG S1A0G
puo Ang ulyjog ui
92) yo YOHLNGIASIG. soyare

B21 uo Buipuo] sy04341y

sjuasn>

23] {013015

22] - (uaaysam) pup juaais)
2>| - (usassvQ)

21y24y UDIPoOUD>

s2| - s104ig Stang

1224 - Avg 4Iyj0E

€l-N1 (OCH

1 SUD > -°S Asuayy -10414ND

404g s 'aog

pun Ang uljjog ul
23) yo UOIENG4AISIG royals

221 uo Bulpud] syosd41y7

squasiny

a2) [p1D0/9

234 - (us2)5a,4) puD|Uues15
22) - (usassn3)

242" UOIPpDUD>)

@2| - s1D4yg StADG

224 - Avg ulyyoEg

“itt

168Sl “2S'W “UO “H se Ppetyiyueps Buryuid SNOIAaIg

"pessnasip st uoungiy
“Sip 231 jo1sD)/6 jonuuy “uONAqI4IsSIp joRMuUuD jONSsNO
stays Aq paqursep asp sesnjooy 21YWdosBodoy sayiGg
*sUOI4Ipuod Butsindas A} |p QuuD sapun A\jp12edsa $9240
Buipup|, 4042410 ajqissod 10) paqiidsap si AydniBodoy
2>| “passnosip ain a1 Des 40 UONAgiuistp ays
PUD UONDINIIID sIDM JO SIINSIS94D0IDY4D JOsQUED

(El -dL “O°H) “seoyr pl, “dZE
"SG6{ Aspounp ~ysuIwDy “5 Asus Aq ‘LIVALS SIAVG
GQNV AVG Nidadvad NI 3D! JO NOILNDINLSIG

221430 21YdosBoupAyy Kany *g “fh

168SL “25'W °U “H SO petyiuiuep: Buinuiid snoisaig

*Pessmrsip st UoINgess
“stp a3! joIsnj6 jonuuy *UONNAgGIaISIpP joNuUUD jOASsNn
2104 Aq Peqiusseap ain sainjoay 2iydosBodoy 4seYyid
*sUOlsIpuod Buisindes AjjpnuuL sapun Ajjpizedse soe4D
Buipup] 4yD45110 ayqissod 40) paqasep si AydoiBodoy
25] *Ppeassnosip ain 3931 es #O UYOUNGUISIP ays
puso YUONOIND4I5 4e@410™ 4° SINUS HID IDYD JOsBUeD)

(El -eL “O “H) “sepyr pl “AZE
SS6L Asonunp ysUIMDy “s Asuai4y Aq “LIVALS SIAVG

GNv Av@ NidjdvVO NI JDI JO NOUADIYLSIG

221440 aiydosBoupdAyy Aaony Gas

|
;
i

£L-s1 “OH

IySUIWDY “S Asuayy *4044ND

41D 45S stand
puo Ang uljjog ul
22] jo uonngiasig soyeta

291 Uo Buipupy 4443417

Syuesin>

a2} [p1DD|9

22>) - (Usaisay) pun jueaig
2>| - (use4sD9)

242*y uDIppUD>)

22} - s1D4Ig SIADG

22) - Avg ulyyog

Ell “O°'H

iASUIWDY “S Aiuay saouynd

siD4s s!aog
puo Ang uljjoo ut
O22) yO UONNNGINSIQ ‘oybt4
221 Uo Buipun] 44043417
Sjuadin>
>| (D1IDI|N
23) - (Usassay,) PUDjUaaI5)
22| - (usaysn 3)
2142.4y UDI PpoUD>)
22| - 410 44S S!1ADg
22) - Avg uyjyog

168Sl “25'W “OU “H S® palyuep! Buiyuisd snoinaig

*pessnasip Ss! uounqiy
“sip 92! jo1sp 46 jonuuy “uUONNgisasip jonuuD jonsn
a1auy Aq Peqiussep 33D seasnine; 214ydosBodoy 424410
*suoIsIpuod Buisindas Ajo ouuo Jepun A\joisadse sDouD
6buipup| 4jD25410 ejqissod 10) paqiidsep si 4ydosBodoy
22! “pessnosip aun e2 08S jO VOUNGiIsip ath
PUD YO'sD]NIND seiDM 4O SIMS14AYIDIDYD jOIeUued

(EL-dl “O °H) ‘s#t0y> pL “dZE
"GS6| Asonunp “WyxsuiuiDy *G Asual4 Aq ‘LIVALS SIAVA
GNv AVG Nids4vad NI 3D! SO NOINGIYLSIG

231449 21YdosBospAyy Annoy "5 “fh

168S1 “2S5'W "UY “H SO peyimuap: Buiyuisd snoinaig
"pessnosip si uonngiy
“SIP 931 jo1sn/6 jonuuy “UOIWAQI4IsiIp jONUUD jDNSN
siayy Aq pagiidsep ain sainioay I1ydosbodo, s98YyICO
*suoiipuod Buisindas AjjoNUUD sapuN Ajjp1Dadsa soeaID

6uipup; 4yO4d4ID B@}qissod 10; peqiidsep s! AuydpiBodoy
2?| “Pessnoasip ain 931 DES 49 UYOINNQGIISIP ats
PUD YONDINIIID sayOM j4O SINSIA~IDIDYD jO1@UeD

(Sl sal “O) HP sous pi soc
“iysuimoy "6 Asuaty Aq ‘LIVA1S SIAVA
NilddvVO NI 3D! 3O NOILATIYLSIG

231449 2I1YdosBoipAjy Andy "5 “1

“$S6L Asonuoe
GNy AV

SIE Ont

4 sUIWD > °S Asuay 7404sND

4104S s!aog

puo Ang uljjog ul
22| yo uoingiasig seyets

231 Uo Buipuoy yjyosd41y

spuadiin>)

@2} [D120|5)

@2) - (Use94504) PUD jUe2I¢)
22) - (usassD9)

2'y24y UDIPDUD>

@2| - 4$1D44g St1ADG

-2@9) - Aog uljyog

EL-S1 “O7H

My sUIUID > “Ss Aiuayy -104)ND

diD4ig S1ADG

puo Ang uljjyog ui
82) yO UOIINGUaSIg ‘airs

291 uo Bulpuny syosdsiy

syuesin>

22] jD1I0j{9

22) - (usaysay ) pup juesi5
@2| - (usa4sD9)

D24y UDIPoUD >)

22] - 41D4Ig StADG

a2) - Ang ulyjyog

sat

wHSnN

HAG

168S1 “2S'W "UO “H SD petyuuapt Buyuisd snoaaig

“pessnosip st uoungiiy
“SIP a2! jo1s0|6 jonuuy “UOINGI4Isip joONUuUD joONSsN
4194, Aq paqi2sep ain seinjoay d14dosBodoy seyig
*sUOIsIpuod Buisindes Ajjpquun sapun Ajjnidedsa soas0
Buipup| 4jD4341D ajqissod joy paqiidsep si Aydosbodoy
22] “passnosip 2up 83' Des 4O | UVOTINgGiystp aus
puo YUONONIIID 4840™ jo S3tystsgg304I045 jos2ues

(Cl -adL “O “H) “sHtoy> pL “dZE
“SS6L Asonuof “1ysuImMDy “s AsuaH Aq “LiVALS SIAVA
GNv AVG@ Nidsavd NI 35! SO NOILADIYNLSIG

221430 2'YdosBoupAyy Anny “5 “fh

168SL “25'W "UO “H SO pelyuuepr bu

svat o1aa
id SNO1AaIg

*pessnmoasip St UONAgHY
“SIP a3! jo1s0j;6 jonuuy *uOHAgISIp joNUUD jDNSn
siays Aq paquosap a21p sainioay siydosBodoy 484i
*sUOIyIpuad Buiiindes AjjponuuLD sapuAa Ajjptaedsa soauD
Buipuo| 4j049110 BIQissoG 10) paqnoasep st AydosBodoy
2>| “passnosip ein eo: oes 49 uounqiuistp aus
puo UONOINDIID 42@40™ yo SIMs tsggaDIDYd joseued

(El -aL "O “H) “semy> pL “OzE

SS6l Asonunp “iysuIMmOy “¢ Asay Aq “LIVALS SIAVG
GNV AV@ NidjsvO NI 3D! JO NONARINLSIG

221340 24YdouBopAyy AAON °*G “NN

\
4
i
‘
(
\
f
}
:

fa]teree ato) Ta

tysuimDy "SG Asuay :404snD

41D435 S1ADG
pun Avg uljjoe u!
OI] yO UONNGIaSIGQ: se{4ts

221 uo Buipuo| syOAD4Iy7

Syuasin>

22) jD1aDID,

22) - (Usaisay) puDdjusss5
a>| - (usa4s09)

DN l4y uo'pouno-)

@2| - 41D4sg S1ADG

a2) - Avg ulyyoE

€l-G1 ‘O'H

i4suIWwD > SC Aauay s404sND

41D4IG S!ADG
pun Ang uljjog ut
92, yO UONNNGiuNSIg “att
22) uo Buipuo; HyDsdsiy
Sjuaiin>
a2] jp1aDI9
22) - (Ussisay) pud|usaicy
93) - (usass05)
21424y UDIppuD->)
e2|- 4'04bC s'aoqg
22) - Avg uiyjyog

"Is iyy uO) “H4 sD Ppolymuspr Buiyuiad SNOIABIY

168S1

"pessnoasip s!
“SIP a2! jp1s0j6 jonuuy “uoNngisssip jonuuD
stays Aq peqiudsep aso sainjoay >214doiBodo, seyiC
*sUOIyIpuod Buisindas Ajo ouuo Jepun A\jpizedse sD2auD
6uipup; 4jyD434ID Bjqissod 40) paqiidsep si AydpsBodoy

uoINgias
joasn

22! “passnosip 2un 83! 08S YO YVOWUNGIUysIP aIY4
PUD YOUDOINIIID s9sDM JO SINSI49YDDIDYD |jDsBUEDd
(EL-dl “O “H) “s#oyr pl “dze

“SS6l Asonunp “tHsuiuDy “5 Asusly AG ‘LIVALS SIAVO
GNv AVY Nidsavad NI 3Dl 40 NOILNGIYLSIG
221340 21YddsBoipAyy Anny as Ip)

168S1 “2S'W "UO “H SO peymuap: Buiyuid sNOIAaig

“pessnosip si Uuoingiiy
“SIP @2! (DIasDj6 jonuuy “UOIINGI4iSIpP jONUUD jDASN
siayy Aq Peqissep 34D sainjoay, 21ydosBodoy 42410
*suoIsipuos Buisindas Ajjonuuv sapun Ajjpidadsa soaio
6urpup| 4jD4341D @}Qissod 104 Peqiosep si AydosBodoy
23) “P@ssnosip ain 931 pes yO UoINgiisip ay
puo YOO INDIID jo SINS AysDIDYS |O4euer)

(Cl-dL “O *H) ‘“Suspyr> pl “dZE
"I4SUIWID > °5 Aiuayy Aq ‘Livals SIAVG
Nid4vd NI 351 3O NOILASINISIG

221340 21YdosBoipAyy Kany sn

4ajDM™

“SS6| Asonuor
GNy Ava

£lL-L “OCH

IysUIWDY “Gg Asua}y -s044ND

sID4Ig S1A0G
puo Ang -ulyjog ut
83] yO UOLUNGIsIg saysty

221 uo Buipuo| $y sds

Sgueain>

82] [DIDI

22] - (usassay) pup |useic)
2>| - (usass09)

21y2 ny UDIPDUD>

32| - $1044 siaog

292) - Avg ulyjyog

SSS Ord

'ySUIWID > “SC Aiusay 4044)ND

Vto4S Siang

puo Ang ulyjog ut
85| yo UOIINGIAASIG foyats

291 uo Bulpuo| 4pOs sty

siueuny

>| jO120|9

23) - (Usessa,) pud|Usesig
a2) - (usa4sp 9)

D12ay UODIpoUD-)

e2| ° 4'1D4NS Stang

a2) - Avg ulyypog

KHAO THN

168Sl “2S'W -U “H SD pelyiuep: Bumuid sNoIAaig

“Ppessnasip si uoungiy
“SIP a3! jo1s0/6 jonuuy “UONNgGI4SIP jONUUD jDNSsN
s1auy Aq P2qis2sep 24D sssnjoay 21ydosBodoy 424410
*sUOIyIpuod Buisinda4 AjjoQUUD sapun Ajjoidodsa@ spe
Buipuo| 4jD4341D |Bjqissod 104 paqiidsap si AydoiBodoy
22>] “Passnrsip ain 23! Das 40 UONNgiuisip ays
PUD YONDINIIID 4BIDM JO SdIWsI49430IDYD JOIaUEqg

(€l-adl “O *H) “Stsoyr> pL “dZE
“tysutrupy *s Asuay Aq ‘Livals SIAVG
NilddvVQ@ NI 351 30 NOILNGIYLSIG

22440 2'Y4YdosBoupAyy Anny *¢ +

"SS6{ Asonuor
GNV Ava

“IS'IW "UH SO pelyyuep: Bunyuiud snginaig

168S1

“pessnosip si UONNGIY
“SIP ad! jorsn]6 jonuuy "UOLNgGIaistp jONUUD jDASNA
says AQ paqiursep ain sainjoay s14ydosBodoy seyiCg
*suolyIpuod Buisindes AjjonuuG sapun Ajjpinzedsa sep
Suipup] 4yD42110 ajqissod 10) pagi2sep si AydosBodoy
2>| “Ppessnosip aun a2: oes 4° “YOUNquisip aye
pus UONDINS415 4e40™ jo SINUS TID IDYD JOs2uUeD)

(El-dl “0 “H) “stpy> pL “dZe
SS6l Asonune *tysUIMDYy "Ss Asuayy Aq ‘LIVALS SIAVG

GNv¥Y AVY NiddvVO NI 3D! JO NONLADINISIG
221449 21YdDaBoupdAyy Anaony = tf

o_ con PRN a SP
CI
= a ag ttf
= a ee

—

ie ee

— =

ae

: : é r :
= Se .
oo ne = |

b Toe “ee