Australia: The Land Where Time Began |
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Regulation of Ice Stream Flow Through Subglacial Formation of Gas
Hydrates
A primary control of the stability of ice sheets are variations of the
flow of ice streams and outlet glaciers, but a comprehensive
understanding of the key processes that operate at the ice-bed interface
has remained elusive. For the maintenance of force balance in a
subglacial environment that is well-lubricated/high slip basal
resistance is critical, especially at sticky spots, local zones of high
basal traction (Alley, 1993). In this paper Winsborrow et
al. considered the influence
of subglacial gas-hydrate formation on the dynamics of ice streams, and
the potential of gas hydrates to initiate and maintain sticky spots. It
is documented by geophysical data that about 20,000 years ago a major
palaeoice-stream drained the Barents Sea-Fennoscandian ice sheet. In
this paper Winsborrow present the results of this study that reveal a
sticky spot covering an area of about 250 km2 that coincided
with subsurface shallow gas accumulations, fluid expulsion on the
seafloor and a fault complex that is associated with deep hydrocarbon
reservoirs. It is proposed by Winsborrow et
al. that gas that migrated
from these reservoirs formed gas hydrates under subglacial conditions of
high pressure and low temperature. The subglacial sediments were
desiccated and stiffened by the gas hydrate which thereby strengthened
the subglacial sediments which promoted high traction – a sticky spot –
which regulated the flow of the ice stream. It is common to find deep
hydrocarbon reservoirs beneath both present and past glaciated areas,
which implies that regulation of subglacial dynamics by gas hydrates
could be a widespread phenomenon.
The degree to which gravitational driving stress is resisted by lateral
shear at its margins, and friction at its base, largely determines the
flow if ice streams. The spatial distribution of subglacial traction is
critical to the overall stability of ice streams as lateral drag from
adjacent ice that is moving more slowly is the primary resistive force,
but this is not sufficient to balance the driving stress. As a
consequence, variations in the velocity of the ice stream will be caused
by variations in the basal friction, with the result that fast flow is
promoted by a well-lubricated weak bed. It is indicated by observations
from the Siple Coast ice stream, West Antarctica, that the basal shear
stress is focused disproportionately on localised areas of high basal
traction, so-called stick spots, which are surrounded by a deformable
bed that is weaker and well-lubricated (Alley, 1993). A critical role is
therefore played by the distribution and extent of sticky spots in
regulating the flow of ice streams, with the shutdown of ice stream flow
observed to follow on the widespread development of sticky spots (Tulaczyk
et al., 2000; Anandakrishnan & Alley, 1997).
If subglacial sediments are desiccated and stiff, or if freezing
conditions prevail at the ice-bed interface, sticky spots can form
(Alley, 1993; Stokes et al., 2007). The shear strength of subglacial
sediment is related directly to normal effective stress (ice load minus
water pressure, though pore-water pressure is referred to explicitly in
the case of basal sediments). As a result of this a significant increase
of sediment strength is caused by a small reduction of basal pore-water
pressure. There are 2 processes that can trigger this initial water
pressure change. Reorganisation of, or changes in, the availability of
subglacial meltwater ‘water piracy’ (Anandakrishnan & Alley, 1997;
Alley, Anandakrishnan, Bentley & Lord, 1994), is the first, or the
second, basal freeze-on that is caused by ice thickness changes, or the
increase by advection of cold surface to the bed (Tulaczyk, Kamb &
Engelhardt, 2000; Bougamont, Tulaczyk & Joughin, 2003; Christoffersen &
Tulaczyk, 2003). Winsborrow et al.
introduce a 3rd mechanism for the formation of sticky spots
based on observation from a palaeoice-stream bed on the continental
shelf of Norway: pore-water piracy and stiffening of sediment as a
result of the accumulation of subglacial gas hydrate.
Håkjerringdjupet is a cross-shelf trough in the southwest Barents Sea
that has been glacially overdeepened. Håkjerringdjupet drains ice
westwards from the mainland to an ice margin that was located at the
edge of the shelf (Ottesen, Dowdeswell, & Rise, 2005) at the time of the
Last Glacial Maximum (LGM) approximately 24,000 years ago, when an ice
sheet covered the entire Barents Sea and the Norwegian continental
shelf. The Troms-Finnmark Fault Complex dissects the trough, and a
complex glacial landform assemblage characterises the seafloor. Highly
elongated streamlined sedimentary deposits, more than 50 km in length
and with a width in the order of 500 m, which are aligned to the axis of
the trough. These are observed across the entire trough, except for the
northern part, west of the fault complex and mega-scale glacial
lineations (MSGLs), which formed beneath an ice stream that was flowing
rapidly (King, Hindmarsh & Stokes, 2009; Stokes & Clark, 1999). There
are 2 broad deposits with a wedge shape that have asymmetrical profiles,
steeper on the down-ice slopes, and on their surface are MSFLs. These
have been interpreted as being the grounding zone wedges (GZWs), which
had formed during standstills or readvances in the course of the retreat
of the ice margin (Ottesen et al.,
2008; Winsborrow et al.,
2012). Landform assemblages of MGSLs and GZWs have been identified
across wide areas of continental shelves that were previously glaciated,
their formation being attributed to the ice stream retreat that was
rapid and episodic (Dowdswell et
al., 2008).
The hummocky morphology of the northern part of the Håkjerringdjupet,
which is comprised of a broad depression bounded by the lateral margins
of the Troms-Finnmark Fault Complex and by an area of irregular hills
that are located beyond the western margin of the fault complex, which
is unusual for a palaeoice-stream. The depression, which has an area of
approximately 250 km2, represents an overdeepening of 90 m
from the seafloor to the east of the fault complex. Beneath the seafloor
depression the boundary between the bedrock and the glacigenic sediment
is also overdeepened and rough. The irregular hills have a maximum
elevation of approximately 80 m relative to the surrounding seafloor and
cover an area similar to that of the depression. Across much of
Håkjerringdjupet there is a uniform thickness and stratified acoustic
signature of older glacigenic sediments that were deposited prior to the
deglaciation (Rokoengen et al.,
1979), though they are largely absent from the depression, and within
the hummocky hills they have a thickness that is unusually great and
varying. Also, within the hills the older glacigenic sediments have a
seismic reflection pattern that is chaotic that is comprised of blocks
of sediment that are oriented randomly and are acoustically stratified.
Winsborrow et al. interpreted
this to be a glacitectonic hill-hole pair that formed from rafted
subglacial sediment and bedrock which have been displaced, creating a
source depression, which was transported with the overlying ice, being
deposited to form irregular hills, which is consistent with earlier work
(Sættem, 1994). According to Winsborrow et
al. glacitectonic rafting of
sediment/bedrock occurs along a decollement of low strength which may
represent the boundary between consolidated sediment and soft sediment,
or sediment that is frozen or non-frozen. Slow flow of ice is implied by
these processes in a subglacial environment that is high
traction/low-slip, which contrasts with the remainder of the bed of the
Håkjerringdjupet palaeoice-stream, which records rapid ice flow on a
subglacial environment of low-traction/high-slip. Sticky spots are
suggested in the geomorphic record to appear as a disruption to a
classic pattern of parallel MSGLs that have been formed by streaming ice
flow (Stokes et al., 2007).
Winsborrow et al. therefore
conclude that the glacitectonic source depression and sediments that
have been rafted are the geologic imprint of a sticky spot on the bed of
the Håkjerringdjupet ice stream.
Across the seafloor of Håkjerringdjupet there are many small circular
depressions, typically of less than 50 m diameter, and less than 7 m
deep that have been interpreted as pockmarks, which were formed by
focused flow of fluid through the seafloor. Winsborrow et
al. suggest the presence of
pockmarks is consistent with migration in the past of gas from
hydrocarbons in the reservoir below (Hovland & Judd, 1988). The highest
density and largest examples are found in the source depression, within
the fault complex, their distribution and size not being uniform.
Pockmarks can also be observed to the east of the fault complex, where
there is a tendency for them to be less dense and smaller. A sharp
boundary is present between seafloor areas with and without pockmarks,
and pockmarks are to a large extent not present in grounding wedges,
rafted sediments and the area of MSGLs in the southern part of the
trough.
It has been shown by seismic data that there are multiple faults in the
central part Håkjerringdjupet and high-amplitude, phase-reversed
reflections along the dipping layers that are classic indicators of
accumulations of gas and the migration along faults from deeper
reservoirs. The shallow accumulations of gas have been shown to be
restricted to the substrate beneath the pockmarked surface depression,
which is also the zone of maximum fault displacement. The fault
escarpment is less abrupt in the southern parts of the trough, with no
deep seafloor being observed and there is a lack, to a large extent, of
pockmarks and shallow gas accumulations. Winsborrow et
al. therefore infer there is
a link between gas migration from deeper reservoirs that is structurally
controlled and the formation of the Håkjerringdjupet sticky spot. Gas
was found by a discovery well drilled 15 km north of Håkjerringdjupet
(Wellbore 7019/1-1) in 2 reservoirs, Middle Jurassic and Lower
Cretaceous, and the Troms Fault Complex has been found to be associated
with major hydrocarbon reservoirs in the southwestern Barents Sea.
Thermogenic gas from deep reservoirs migrates upwards along faults and
permeable layers of sediments as it is not as dense as either water or
sediments. In the Arctic, gas migrating from leaking petroleum systems
may be trapped in the shallow subsurface as gas hydrates, ice-like
solids, that form under conditions of high pressure and low temperature,
the conditions present in marine sediments and permafrost (Sloan & Koh,
2008). At the present temperature and pressure conditions in
Håkjerringdjupet are just outside the boundary for the formation of
methane hydrate. Under glacial conditions, however, ice that was
grounded in Håkjerringdjupet, as is evidenced by subglacial bedforms
such as glacial lineations on a mega scale, produced the conditions of
high pressure and low temperature necessary for a thick zone, of
approximately 400 m, of methane hydrate stability beneath the ice
stream. As gas migrating into the zone of methane-hydrate stability
encountered pore water within the subglacial sediments and shallow
sedimentary bedrock that was under high pressure, the methane combined
with the pore water to form methane hydrate. Winsborrow et
al. say gas hydrate is
expected to have formed in high saturation patches that were localised
around faults and fractures and areas of porous sediment, given the
bedrock that was highly fractured and the heterogeneous nature of the
subglacial sediments within Håkjerringdjupet (Rokoengen et al., 1979),
instead of forming a continuous layer. The host sediments are desiccated
and stiffened by gas hydrate as a result of pore water piracy into the
gas-hydrate cage structure, connection of grains, and of the greater
strength and lower volume of the gas hydrate compared with its
constituent gas and ice (Walte et al., 2009; Winters et al., 2004; Hyodo
et al., 2013; Durham et al., 2003). In the McKenzie Delta, northern
Canada, sediments bearing gas hydrates display an increase in shear
strength of more than 8-fold when gas hydrate develops, from initial
shear strength of 0.8 to 6.7 MPa with 60 % hydrate saturation (Winters
et al., 2004). The strength of sediments that host gas hydrate and
shallow bedrock in Håkjerringdjupet would have been far in excess of the
“weak” till that was recovered from beneath the Siple Coast ice stream,
West Antarctica (Kamb, 1991) and driving stresses that are typical of
active streams, which have a tendency to not exceed 20 kPa, assuming a
similar relative shear strength increase.
Winsborrow et al. suggested
there would be basal friction that would have been locally enhanced by
stiff sediments and shallow bedrock beneath the Håkjerringdjupet ice
stream which would provide resistance to the flow of the overlying ice.
A strong friction bond would probably have been formed with the
overlying ice by the sediments of high shear strength which would favour
glacitectonic decollement deeper within the substrate. The glacitectonic
hill-hole pair that is visible at present on the seafloor was formed by
thrusting and subsequent deposition of sediments and bedrock containing
hydrate by the ice, which was slow moving.
There are major hydrocarbon reservoirs across the shelf areas that were
previously glaciated by the Eurasian ice sheet complex, and several
palaeoice streams flowed over substrates that were associated with
confirmed hydrocarbon systems. Widespread gas hydrate formation,
particularly at reservoirs that were leaking, that had focused migration
of gas, would have been promoted by the subglacial conditions of high
pressure and low temperature prevailing beneath these ice streams, and
consequent regulation of ice stream basal thermomechanics and flow.
Across the footprint of the palaeoice sheet multiple observations may
now require to be reinterpreted on the basis of this hypothesis. The
large glacitectonic landforms and till that was heavily overconsolidated
associated with the Sklinnadjupet ice stream (Ottesen et al., 2005;
Sættem et al., 1996) flowing over the extensive reservoirs of
hydrocarbon, and the widespread presence of overconsolidated glacial
sediments across the southwestern part of the Barents Sea (Sættem et
al., 1992) are consistent with the regulation of the flow of ice streams
by gas hydrates.
Based on the presence of extensive sedimentary basins and modelling
studies (Wadham et al., 2012; Wallmann et al., 2012) it is proposed that
abundant gas hydrate accumulations are present beneath the ice sheets of
Greenland and Antarctica. Also, gas hydrates have been identified in ice
core samples obtained from above the subglacial Lake Vostok in East
Antarctica (Uchida et al., 1994). The role of potentially widespread gas
hydrate reservoirs in the modification of the thermomechanical regime at
the base of contemporary ice sheets, which makes them critically
sensitive, as well as their impact on ice steam force balance and
dynamics has, so far, not been recognised. This control that was
previously unforeseen, given the current lack of knowledge with regard
to the distribution of gas hydrate, represents a significant unknown in
attempts to model the current and future discharge and evolution of
contemporary ice sheets, as well as their contribution to rising global
sea levels.
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Author: M.H.Monroe Email: admin@austhrutime.com Sources & Further reading |