204
J. A. KITCHING AND F. J. EBLING
limits of the resulting depression would be controlled to some extent
by the lithology.
"The escape route for ice and material scoured out lay along the
original line of the valley through the Ballyisland townland, to the
north-east of Lough Ine. I n this valley there are clear indications of ice
movements with flow directions from west-south-west to east-northeast. Following the retreat of the ice in relatively recent geological
times, the depression would have stood first as an inland lake. Later it
became linked to the sea as a result of the rise in sea level."
The nature of the rocky shores of Lough Ine and the adjacent area
ranges from relatively hard sandstone to friable slate. The strata dip,
at an angle usually between 50" and 80", in the rough direction of magnetic north and this to some extent determines the profile of the shore.
Shores facing north tend to be formed along the bedding planes, sloping
moderately (as to the north of Castle Island) or steeply (as at North
Bullock Island). If the rock is hard, even south-facing shores can bear a
similar relation to the dip; for example, a t south-east Labhra where the
shore follows a bedding plane and an overhang is formed. Usually, however, south-facing shores are eroded and slope gently with a series of
ridges, gullies or platforms almost parallel to the water line. Most of the
shores facing east and west are fairly steep. Rocky boulders are abundant littorally and sublittorally on almost all shores of moderate or
gentle slope and also occur throughout much of the Rapids. At depths
greater than a few metres these boulders tend to become covered with
mud. We have not made any detailed studies of the gravel or muddy
bottoms occurring in the deeper parts of the north and south basins and
in the Western Trough. It is, however, worth recording that in the southeastern part of the South Basin relatively clean boulders extend into
deep water owing to the swirling action of the vortex produced by the
incoming tide.
Relatively little fresh water enters the lough from land drainage.
There is a small stream at the north end, and another a t the south-west
corner, where there is a shallow inlet known as the Goleen.
The open coast adjoining Lough Ine is characterized by cliffs, islands,
inlets and caves which are the product of still continuing marine erosion
acting on the steeply dipping Devonian slates.
The mouth of Barloge Creek, which is relatively narrow, is flanked to
the east by the south point of Bullock Island, and to the west by an
exposed rocky peninsula, known as Carrigathorna, where many of our
studies have been pursued. I n the mouth of the creek are three small
rocks (Cave Island) opposite a deep cave in the cliff of Bullock Island.
At low water Bullock Island is joined to the mainland by a strip of
shingle known as the Coosh; at high water this is submerged and Barloge
J. A. KITCHING AND F. J. EBLING
limits of the resulting depression would be controlled to some extent
by the lithology.
"The escape route for ice and material scoured out lay along the
original line of the valley through the Ballyisland townland, to the
north-east of Lough Ine. I n this valley there are clear indications of ice
movements with flow directions from west-south-west to east-northeast. Following the retreat of the ice in relatively recent geological
times, the depression would have stood first as an inland lake. Later it
became linked to the sea as a result of the rise in sea level."
The nature of the rocky shores of Lough Ine and the adjacent area
ranges from relatively hard sandstone to friable slate. The strata dip,
at an angle usually between 50" and 80", in the rough direction of magnetic north and this to some extent determines the profile of the shore.
Shores facing north tend to be formed along the bedding planes, sloping
moderately (as to the north of Castle Island) or steeply (as at North
Bullock Island). If the rock is hard, even south-facing shores can bear a
similar relation to the dip; for example, a t south-east Labhra where the
shore follows a bedding plane and an overhang is formed. Usually, however, south-facing shores are eroded and slope gently with a series of
ridges, gullies or platforms almost parallel to the water line. Most of the
shores facing east and west are fairly steep. Rocky boulders are abundant littorally and sublittorally on almost all shores of moderate or
gentle slope and also occur throughout much of the Rapids. At depths
greater than a few metres these boulders tend to become covered with
mud. We have not made any detailed studies of the gravel or muddy
bottoms occurring in the deeper parts of the north and south basins and
in the Western Trough. It is, however, worth recording that in the southeastern part of the South Basin relatively clean boulders extend into
deep water owing to the swirling action of the vortex produced by the
incoming tide.
Relatively little fresh water enters the lough from land drainage.
There is a small stream at the north end, and another a t the south-west
corner, where there is a shallow inlet known as the Goleen.
The open coast adjoining Lough Ine is characterized by cliffs, islands,
inlets and caves which are the product of still continuing marine erosion
acting on the steeply dipping Devonian slates.
The mouth of Barloge Creek, which is relatively narrow, is flanked to
the east by the south point of Bullock Island, and to the west by an
exposed rocky peninsula, known as Carrigathorna, where many of our
studies have been pursued. I n the mouth of the creek are three small
rocks (Cave Island) opposite a deep cave in the cliff of Bullock Island.
At low water Bullock Island is joined to the mainland by a strip of
shingle known as the Coosh; at high water this is submerged and Barloge