The Marine Life Information Network

This biotope is characterized by the absence of species resulting from sediment mobility and abrasion (JNCC, 2015), rather than the presence of typical species.  Therefore, changes in temperature will not alter the biotope as it is defined by the abiotic habitat.  Hence, resistance to an increase in temperature is assessed as 'High' and resilience as ‘High’ (by default) and this biotope is assessed as 'Not sensitive'.

This biotope is characterized by the absence of species resulting from sediment mobility and abrasion (JNCC, 2015), rather than the presence of typical species.  Therefore, changes in temperature will not alter the biotope as it is defined by the abiotic habitat.  Hence, resistance to an increase in temperature is assessed as 'High' and resilience as ‘High’ (by default) and this biotope is assessed as 'Not sensitive'.

This biotope is characterized by the absence of species resulting from sediment mobility and abrasion (JNCC, 2015), rather than the presence of typical species.  Therefore, changes in temperature will not alter the biotope as it is defined by the abiotic habitat.  Hence, resistance to an increase in temperature is assessed as 'High' and resilience as ‘High’ (by default) and this biotope is assessed as 'Not sensitive'.

This biotope is characterized by the absence of species resulting from sediment mobility and abrasion (JNCC, 2015), rather than the presence of typical species.  Therefore, changes in temperature will not alter the biotope as it is defined by the abiotic habitat.  Hence, resistance to periodic extremes of temperature due to heatwaves is assessed as 'High' and resilience as ‘High’ (by default) and this biotope is assessed as 'Not sensitive'.

This biotope is characterized by the absence of species resulting from sediment mobility and abrasion (JNCC, 2015), rather than the presence of typical species.  Therefore, changes in temperature will not alter the biotope as it is defined by the abiotic habitat.  Hence, resistance to periodic extremes of temperature due to heatwaves is assessed as 'High' and resilience as ‘High’ (by default) and this biotope is assessed as 'Not sensitive'.

This biotope is characterized by the absence of species resulting from sediment mobility and abrasion (JNCC, 2015), rather than the presence of typical species.  Therefore, changes in acidification and carbonate chemistry as a result of increased pC0₂ will not alter the biotope as it is defined by the abiotic habitat.  Hence, resistance to an increase in pC0₂ is assessed as 'High' and resilience as ‘High’ (by default) and this biotope is assessed as 'Not sensitive'.

This biotope is characterized by the absence of species resulting from sediment mobility and abrasion (JNCC, 2015), rather than the presence of typical species.  Therefore, changes in acidification and carbonate chemistry as a result of increased pC0₂ will not alter the biotope as it is defined by the abiotic habitat.  Hence, resistance to an increase in pC0₂ is assessed as 'High' and resilience as ‘High’ (by default) and this biotope is assessed as 'Not sensitive'.

A rise in sea level increases the water depth at the shore and results in increased wave and tidal energy along the shore, due to the increase in fetch and reduction in wave attenuation (Pethick, 2001; Crooks, 2004; Fujii, 2012).  As a result, coastal landforms (e.g. subtidal bedforms, intertidal flats, saltmarshes, shingle banks, sand dunes, cliffs and coastal lowlands) migrate along and parallel to the shore to maintain their position with the coastal energy gradient (Cooks, 2004; Fujii, 2012).  For example, mudflats migrate landwards to a lower energy position and may be replaced by sand flats that have themselves migrated landwards from exposed conditions (Crooks, 2004).  In effect, ‘coastal roll-over’ results as the shore moves landwards by the erosion of the landward, upper limit of the shore and deposition at its lower limit (Crooks, 2004).  Pethick (2001) suggested that a sea-level rise rate of 6 mm/yr could result in landward movement of estuaries by 10 m/yr, long-shore migration of open coast landforms of 50 m/yr and ebb-tidal deltas to extend laterally by 300 m/yr.  For example in Norfolk, the coarse sediment beaches of Scolt Head Wells were predicted to be replaced by mudflats and saltmarsh, while sand beaches were predicted to replace salt marsh and sand dune area of Thornham, Scolt and Stiffkey (Pethick, 2001).

However, many shores will not be able to move landward, either due to natural barriers (e.g. rock or cliff) or artificial structures (e.g. roadways, sea defences), resulting in ‘coastal squeeze’ and the potential substantial loss of intertidal habitat (Fujii, 2012; Mossman et al., 2015).  Increased water depth and increased wave action may change to the shore from a dissipative to reflective morphology with a steeper slope and coarser sediment but lower biomass (Fujii, 2012).  For example, 61% of 1084 shore profiles in England and Wales had already experienced steepening since the mid-19^th century due to foreshore erosion and flood defences (Taylor et al., 2014; Fujii, 2012).  Fujii & Raffaelli (2008) modelled the likely effects of sea-level rise on the Humber estuary.  They suggested that sea–level rises of 10 cm, 30 cm, and 50 cm would result in loss of 2.2%, 6.7% and 11.2% of the intertidal area (including mud and sand flats), and when beach steepening and sediment shifts were taken into account, loss in macrobenthos of 6.7, 11.6 and 11.9% respectively.  They concluded that a 30 cm increase in sea-level could result in an overall loss in the macrobenthos of 22.8% (Fujii & Raffaelli, 2008).  Galbraith et al. (2002) modelled the effect of sea-level rise at five wetland sites in the USA on tidal flats (mud and sand). They suggested that sea-level rise produced by a 2°C change (predicted as 34-77 cm by 2100) in the USA, could result in a 20-70% loss of current intertidal area at four of the sites examined, although there was variation between sites (Galbraith et al., 2002).

The effects of sea-level rise and increased wave action may be increased further due to storms and storms surges.  IPCC (2019) note that the frequency of extreme sea-level events (e.g. due to storm) was predicted to increase as sea-level rises.  However, there is no consensus on the future storm and wave climate around UK coasts (Mossman et al., 2015; Lowe et al., 2018; Palmer et al., 2018).

Sensitivity assessment. This is a physical habitat dominated by shingle, gravel, cobbles and pebbles (JNCC, 2015).  It is found from the upper to lower shore, depending on wave exposure and subject to a high level of abrasion due to sediment mobility.  The evidence suggests that sea-level rise could result in landward migration of the habitat as the upper reaches of the shore are eroded and the lower reaches submerged.  However, where hard structures (e.g. cliffs, sea defences) prevent landward migration it may be lost and/or submerged and become SS.SCS.ICS.SSh.  It may also migrate along the shore and, with increased wave exposure, the area of this habitat may increase elsewhere, although it may be lost from the site of interest.  Therefore, under the middle emission scenario (ca 50 cm rise) a proportion of the habitat could be lost (based on Fujii & Raffaelli, 2008) and resistance is assessed as ‘Medium’.  Pethick & Crooks (2000) suggested that shingle ridges could return in 1-10 years after an extreme storm event.  However, sea-level rise is an ongoing pressure and no recovery is likely, therefore, resilience is assessed as ‘Very low’ and sensitivity as ‘Medium’.  Similarly, under both the high emission scenario (70 cm) and the extreme scenario (107 cm), resistance is probably ‘Low’ (a 25-75% loss), so that resilience is assessed as ‘Very low’ and sensitivity as ‘High’.  However, there is likely to be considerable variation between sites (e.g. Galbraith et al., 2002; Mossman et al., 2015; Lowe et al., 2018; Palmer et al., 2018) so confidence in the assessments is ‘Low’.

A rise in sea level increases the water depth at the shore and results in increased wave and tidal energy along the shore, due to the increase in fetch and reduction in wave attenuation (Pethick, 2001; Crooks, 2004; Fujii, 2012).  As a result, coastal landforms (e.g. subtidal bedforms, intertidal flats, saltmarshes, shingle banks, sand dunes, cliffs and coastal lowlands) migrate along and parallel to the shore to maintain their position with the coastal energy gradient (Cooks, 2004; Fujii, 2012).  For example, mudflats migrate landwards to a lower energy position and may be replaced by sand flats that have themselves migrated landwards from exposed conditions (Crooks, 2004).  In effect, ‘coastal roll-over’ results as the shore moves landwards by the erosion of the landward, upper limit of the shore and deposition at its lower limit (Crooks, 2004).  Pethick (2001) suggested that a sea-level rise rate of 6 mm/yr could result in landward movement of estuaries by 10 m/yr, long-shore migration of open coast landforms of 50 m/yr and ebb-tidal deltas to extend laterally by 300 m/yr.  For example in Norfolk, the coarse sediment beaches of Scolt Head Wells were predicted to be replaced by mudflats and saltmarsh, while sand beaches were predicted to replace salt marsh and sand dune area of Thornham, Scolt and Stiffkey (Pethick, 2001).

However, many shores will not be able to move landward, either due to natural barriers (e.g. rock or cliff) or artificial structures (e.g. roadways, sea defences), resulting in ‘coastal squeeze’ and the potential substantial loss of intertidal habitat (Fujii, 2012; Mossman et al., 2015).  Increased water depth and increased wave action may change to the shore from a dissipative to reflective morphology with a steeper slope and coarser sediment but lower biomass (Fujii, 2012).  For example, 61% of 1084 shore profiles in England and Wales had already experienced steepening since the mid-19^th century due to foreshore erosion and flood defences (Taylor et al., 2014; Fujii, 2012).  Fujii & Raffaelli (2008) modelled the likely effects of sea-level rise on the Humber estuary.  They suggested that sea–level rises of 10 cm, 30 cm, and 50 cm would result in loss of 2.2%, 6.7% and 11.2% of the intertidal area (including mud and sand flats), and when beach steepening and sediment shifts were taken into account, loss in macrobenthos of 6.7, 11.6 and 11.9% respectively.  They concluded that a 30 cm increase in sea-level could result in an overall loss in the macrobenthos of 22.8% (Fujii & Raffaelli, 2008).  Galbraith et al. (2002) modelled the effect of sea-level rise at five wetland sites in the USA on tidal flats (mud and sand). They suggested that sea-level rise produced by a 2°C change (predicted as 34-77 cm by 2100) in the USA, could result in a 20-70% loss of current intertidal area at four of the sites examined, although there was variation between sites (Galbraith et al., 2002).

The effects of sea-level rise and increased wave action may be increased further due to storms and storms surges.  IPCC (2019) note that the frequency of extreme sea-level events (e.g. due to storm) was predicted to increase as sea-level rises.  However, there is no consensus on the future storm and wave climate around UK coasts (Mossman et al., 2015; Lowe et al., 2018; Palmer et al., 2018).

Sensitivity assessment. This is a physical habitat dominated by shingle, gravel, cobbles and pebbles (JNCC, 2015).  It is found from the upper to lower shore, depending on wave exposure and subject to a high level of abrasion due to sediment mobility.  The evidence suggests that sea-level rise could result in landward migration of the habitat as the upper reaches of the shore are eroded and the lower reaches submerged.  However, where hard structures (e.g. cliffs, sea defences) prevent landward migration it may be lost and/or submerged and become SS.SCS.ICS.SSh.  It may also migrate along the shore and, with increased wave exposure, the area of this habitat may increase elsewhere, although it may be lost from the site of interest.  Therefore, under the middle emission scenario (ca 50 cm rise) a proportion of the habitat could be lost (based on Fujii & Raffaelli, 2008) and resistance is assessed as ‘Medium’.  Pethick & Crooks (2000) suggested that shingle ridges could return in 1-10 years after an extreme storm event.  However, sea-level rise is an ongoing pressure and no recovery is likely, therefore, resilience is assessed as ‘Very low’ and sensitivity as ‘Medium’.  Similarly, under both the high emission scenario (70 cm) and the extreme scenario (107 cm), resistance is probably ‘Low’ (a 25-75% loss), so that resilience is assessed as ‘Very low’ and sensitivity as ‘High’.  However, there is likely to be considerable variation between sites (e.g. Galbraith et al., 2002; Mossman et al., 2015; Lowe et al., 2018; Palmer et al., 2018) so confidence in the assessments is ‘Low’.

A rise in sea level increases the water depth at the shore and results in increased wave and tidal energy along the shore, due to the increase in fetch and reduction in wave attenuation (Pethick, 2001; Crooks, 2004; Fujii, 2012).  As a result, coastal landforms (e.g. subtidal bedforms, intertidal flats, saltmarshes, shingle banks, sand dunes, cliffs and coastal lowlands) migrate along and parallel to the shore to maintain their position with the coastal energy gradient (Cooks, 2004; Fujii, 2012).  For example, mudflats migrate landwards to a lower energy position and may be replaced by sand flats that have themselves migrated landwards from exposed conditions (Crooks, 2004).  In effect, ‘coastal roll-over’ results as the shore moves landwards by the erosion of the landward, upper limit of the shore and deposition at its lower limit (Crooks, 2004).  Pethick (2001) suggested that a sea-level rise rate of 6 mm/yr could result in landward movement of estuaries by 10 m/yr, long-shore migration of open coast landforms of 50 m/yr and ebb-tidal deltas to extend laterally by 300 m/yr.  For example in Norfolk, the coarse sediment beaches of Scolt Head Wells were predicted to be replaced by mudflats and saltmarsh, while sand beaches were predicted to replace salt marsh and sand dune area of Thornham, Scolt and Stiffkey (Pethick, 2001).

However, many shores will not be able to move landward, either due to natural barriers (e.g. rock or cliff) or artificial structures (e.g. roadways, sea defences), resulting in ‘coastal squeeze’ and the potential substantial loss of intertidal habitat (Fujii, 2012; Mossman et al., 2015).  Increased water depth and increased wave action may change to the shore from a dissipative to reflective morphology with a steeper slope and coarser sediment but lower biomass (Fujii, 2012).  For example, 61% of 1084 shore profiles in England and Wales had already experienced steepening since the mid-19^th century due to foreshore erosion and flood defences (Taylor et al., 2014; Fujii, 2012).  Fujii & Raffaelli (2008) modelled the likely effects of sea-level rise on the Humber estuary.  They suggested that sea–level rises of 10 cm, 30 cm, and 50 cm would result in loss of 2.2%, 6.7% and 11.2% of the intertidal area (including mud and sand flats), and when beach steepening and sediment shifts were taken into account, loss in macrobenthos of 6.7, 11.6 and 11.9% respectively.  They concluded that a 30 cm increase in sea-level could result in an overall loss in the macrobenthos of 22.8% (Fujii & Raffaelli, 2008).  Galbraith et al. (2002) modelled the effect of sea-level rise at five wetland sites in the USA on tidal flats (mud and sand). They suggested that sea-level rise produced by a 2°C change (predicted as 34-77 cm by 2100) in the USA, could result in a 20-70% loss of current intertidal area at four of the sites examined, although there was variation between sites (Galbraith et al., 2002).

The effects of sea-level rise and increased wave action may be increased further due to storms and storms surges.  IPCC (2019) note that the frequency of extreme sea-level events (e.g. due to storm) was predicted to increase as sea-level rises.  However, there is no consensus on the future storm and wave climate around UK coasts (Mossman et al., 2015; Lowe et al., 2018; Palmer et al., 2018).

Sensitivity assessment. This is a physical habitat dominated by shingle, gravel, cobbles and pebbles (JNCC, 2015).  It is found from the upper to lower shore, depending on wave exposure and subject to a high level of abrasion due to sediment mobility.  The evidence suggests that sea-level rise could result in landward migration of the habitat as the upper reaches of the shore are eroded and the lower reaches submerged.  However, where hard structures (e.g. cliffs, sea defences) prevent landward migration it may be lost and/or submerged and become SS.SCS.ICS.SSh.  It may also migrate along the shore and, with increased wave exposure, the area of this habitat may increase elsewhere, although it may be lost from the site of interest.  Therefore, under the middle emission scenario (ca 50 cm rise) a proportion of the habitat could be lost (based on Fujii & Raffaelli, 2008) and resistance is assessed as ‘Medium’.  Pethick & Crooks (2000) suggested that shingle ridges could return in 1-10 years after an extreme storm event.  However, sea-level rise is an ongoing pressure and no recovery is likely, therefore, resilience is assessed as ‘Very low’ and sensitivity as ‘Medium’.  Similarly, under both the high emission scenario (70 cm) and the extreme scenario (107 cm), resistance is probably ‘Low’ (a 25-75% loss), so that resilience is assessed as ‘Very low’ and sensitivity as ‘High’.  However, there is likely to be considerable variation between sites (e.g. Galbraith et al., 2002; Mossman et al., 2015; Lowe et al., 2018; Palmer et al., 2018) so confidence in the assessments is ‘Low’.

This biotope is characterized by the absence of species resulting from sediment mobility and abrasion (JNCC, 2015), rather than the presence of typical species.  Therefore, changes in temperature will not alter the biotope as it is defined by the abiotic habitat.  Hence, resistance to an increase in temperature is assessed as 'High' and resilience as ‘High’ (by default) and this biotope is assessed as 'Not sensitive'.

This biotope is characterized by the absence of species resulting from sediment mobility and abrasion (JNCC, 2015), rather than the presence of typical species.  Therefore, changes in temperature will not alter the biotope as it is defined by the abiotic habitat.  Hence, resistance to an increase in temperature is assessed as 'High' and resilience as ‘High’ (by default) and this biotope is assessed as 'Not sensitive'.

This biotope is characterized by the absence of species resulting from sediment mobility and abrasion (JNCC, 2015), rather than the presence of typical species: changes in salinity will therefore not alter the biotope (based on the abiotic habitat). Resistance to an increase in salinity is therefore assessed as 'High' and resilience as ‘High’ (by default) and this biotope is considered to be 'Not sensitive'.

This biotope is characterized by the absence of species resulting from sediment mobility and abrasion (JNCC, 2015), rather than the presence of typical species: changes in salinity will therefore not alter the biotope (based on the abiotic habitat). Resistance to a decrease in salinity is therefore assessed as 'High' and resilience as ‘High’ (by default) and this biotope is considered to be 'Not sensitive'.

Changes in water flow at the pressure benchmark are considered unlikely to lead to alterations in the biotope as wave exposure would still result in sediment mobility, preventing the establishment of a more species rich biotope.  Resistance is therefore assessed as ‘High’ and resilience as ‘High’ (by default) so that the biotope is considered to be ‘Not sensitive’. 

This biotope occurs from the lower to upper shore and sediment mobility, rather than emergence, is a key factor preventing the establishment of a more species rich biotope.  An increase in the emergence period of this biotope would make it even more inhospitable to marine invertebrates. Where the biotope occurs in the supralittoral zone, a reduction in saline spray and splash may favour the colonization of terrestrial plants, which if able fully to establish will have a stabilising effect on the substratum. Consequently, this factor has the potential to alter the biotope. Similarly a decrease in emergence that led to this biotope becoming fully sublittoral would result in reclassification (most likely to the biotope SS.SCS.ICS.SSh). The LS.LCS.Sh.BarSh biotope would not be recognized in either scenario and resistance has therefore been assessed as ‘Low’. On return to prior emergence regime sublittoral species that are intolerant of emergence and plants that may have colonized the substratum and which are intolerant to saline splash and spray will probably decline rapidly. Therefore resilience has been assessed as ‘High’. This biotope is therefore considered to have ‘Low’ sensitivity’ to changes in emergence. 

This biotope is found on shores that are judged to be moderately exposed or exposed (JNCC, 2015). The presence of this biotope across these two categories is considered to indicate (by proxy) that increases or decreases in wave exposure at the pressure benchmark are unlikely to lead to alterations to the biotope.  Resistance is therefore assessed as ‘High’ and resilience as ‘High’ (by default) so that the biotope is considered to be ‘Not sensitive’.

This pressure is Not assessed but evidence is presented where available. As this biotope is characterized by the lack of species, exposure to contaminants will not result in significant impacts.

This pressure is Not assessed but evidence is presented where available. As this biotope is characterized by the lack of species, exposure to contaminants will not result in significant impacts.

Small amounts of oil that can persist for decades in the intertidal zone of coarse-sediment beaches have been documented in a few well-studied cases (Owens et al. 2008). Oil that survives attenuation over the short-term (weeks to months) will persist until there is a change in the environmental conditions, as might occur where there is a seasonal storm-wave climate or as a beach undergoes long-term (erosional) changes. Oil residues can persist on the beach surface as tar mats, asphalt-like pavements, or as veneers on sediment particles or hard surfaces. Subsurface oil residues can persist in similar forms or as fill or partial fill of the pore spaces between coarse-sediment particles. Oil penetrates until it reaches fine-grained sediment, the water table, bedrock, or other penetration-limiting layers. Amounts of persistent oil are very small fractions of the volumes that were originally stranded and these protected residues can continue to biodegrade as they become thinner and more discontinuous.

This pressure is Not assessed but evidence is presented where available. As this biotope is characterized by the lack of species, exposure to contaminants will not result in significant impacts.

Not evidence was found.

This pressure is Not assessed.

As this biotope is characterized by the lack of species, de-oxygenation will not result in significant impacts. De-oxygenation is unlikely as this biotope is intertidal and exposure to air and tidal flushing is likely to recharge oxygen levels. Biotope resistance is therefore assessed as 'High', and resilience as 'High' (by default) and the biotope is considered to be 'Not sensitive'.

As this biotope is characterized by the lack of species present due to sediment mobility, nutrient enrichment will not result in significant impacts. Biotope resistance is therefore assessed as 'High', and resilience as 'High' (by default) and the biotope is considered to be 'Not sensitive'.

As this biotope is characterized by the lack of species, organic enrichment will not result in significant impacts. Organic deposits are likely to be removed rapidly by wave action although in periods of calm an organic deposit may be rapidly colonized by oligochaetes or amphipods. Biotope resistance is assessed as 'High' as enrichment is likely to be very short-lived, and resilience as 'High' (by default), the biotope is considered to be 'Not sensitive'.

All marine habitats and benthic species are considered to have a resistance of ‘None’ to this pressure and to be unable to recover from a permanent loss of habitat (resilience is ‘Very Low’).  Sensitivity within the direct spatial footprint of this pressure is therefore ‘High’.  Although no specific evidence is described confidence in this assessment is ‘High’, due to the incontrovertible nature of this pressure.

This biotope is characterized by coarse sands (JNCC, 2015). A change to a hard or artificial substratum would significantly alter the character of the biotope. The biotope is therefore considered to have 'No' resistance to this pressure (based on a change to a sediment habitat), recovery is assessed as 'Very low', as the change at the pressure benchmark is permanent. Biotope sensitivity is therefore assessed as 'High'.

The benchmark for this pressure refers to a change in one Folk class.  The pressure benchmark originally developed by Tillin et al., (2010) used the modified Folk triangle developed by Long (2006) which simplified sediment types into four categories: mud and sandy mud, sand and muddy sand, mixed sediments and coarse sediments.  The change referred to is therefore a change in sediment classification rather than a change in the finer-scale original Folk categories (Folk, 1954).  The change in one Folk class is considered to relate to a change in classification to adjacent categories in the modified Folk triangle.  For shingle habitats a change in one folk class may refer to a change to gravels, mixed sediments or muddy sands, sandy muds and muds. A change in sediment type would result in reclassification of the biotope (JNCC, 2015) and a change to mixed or fine sediments would likely result in the establishment of a species rich and more diverse community (depending on other habitat factors). Biotope resistance is therefore assessed as ‘None’ and resilience as ‘Very low’ as the change at the pressure benchmark is permanent. Sensitivity is therefore ‘High’.

The process of extraction will remove the abiotic habitat; therefore a resistance of ‘None’ is recorded. As the shingle is mobile where small areas are impacted infilling is likely to be rapid following sediment redistribution by wave action. For instance, at Village Bay on St Kilda, an island group far out into the Atlantic west of Britain, an expanse of sandy beach was removed offshore as a result of winter storms to reveal an underlying rocky shore (Scott, 1960). Yet in the following summer the beach was gradually replaced when wave action was less severe. In view of such observations, that many sandy beaches disappear in winter and reappear in spring, it is likely that recovery would occur in less than a year or six months.  As a result, resilience is assessed as ‘High’, and sensitivity as ‘Medium’.  Recovery where large volumes of shingle are removed over wide areas may lead to slower recovery if sediments are not available and/or water transport is limited. 

This biotope is characterized by the absence of species through sediment mobility (JNCC, 2015), rather than the presence of typical species: abrasion will therefore not alter biotope character. The highly mobile species present occasionally in this biotope may only be found in extremely low abundance and are not specifically dependent on this biotope. Resistance to this pressure is therefore assessed as 'High' and resilience as ‘High’ (by default) and this biotope is considered to be 'Not sensitive'.

This biotope is characterized by the absence of species through sediment mobility (JNCC, 2015), rather than the presence of typical species: abrasion will therefore not alter biotope character. The highly mobile species present occasionally in this biotope may only be found in extremely low abundance and are not specifically dependent on this biotope Resistance to this pressure is therefore assessed as 'High' and resilience as ‘High’ (by default) and this biotope is considered to be 'Not sensitive'.

This biotope occurs in scoured habitats and it is likely, depending on local sediment supply, that the biotope is exposed to chronic or intermittent episodes of high-levels of suspended solids as local sediments are re-mobilised and transported by wave action. This biotope is characterized by the absence of species through sediment mobility (JNCC, 2015), rather than the presence of typical species: changes in suspended solids will therefore not alter the biotope. Resistance to an increase or decrease in suspended solids is therefore assessed as 'High' and resilience as ‘High’ (by default) and this biotope is considered to be 'Not sensitive'.

This biotope is characterized by the absence of species through sediment mobility (JNCC, 2015), rather than the presence of typical species: the addition of a single deposit of fine sediments which will be removed by wave action will therefore not alter the biotope. Resistance to this pressure is therefore assessed as 'High' and resilience as ‘High’ (by default) and this biotope is considered to be 'Not sensitive'.

This biotope is characterized by the absence of species through sediment mobility (JNCC, 2015), rather than the presence of typical species: the addition of a single deposit of fine sediments which will be removed by wave action will therefore not alter the biotope. Resistance to this pressure is therefore assessed as 'High' and resilience as ‘High’ (by default) and this biotope is considered to be 'Not sensitive'.

Not assessed.

Not evidence

Not relevant.

Not relevant.

Not relevant.

Not relevant’ to seabed habitats.  NB. Collision by grounding vessels is addressed under surface abrasion.

Not relevant.

This biotope is not characterized by any typical species, those that are present, such as Bathyporeia spp.  are not translocated and this pressure is therefore considered 'Not relevant'.

The high levels of abrasion resulting from the movement of shingle and the subsequent sediment instability will limit the establishment of all but the most highly scour resistant invasive non-indigenous species (INIS) and no direct evidence was found for effects of INIS on this biotope.  The low levels of water and organic matter retained by this biotope, are considered to additionally inhibit permanent colonization by invasive species. Overall, there is no evidence of this biotope being adversely affected by non-native species. 

As this biotope is characterized by the absence of a biological assemblage apart from occasional and ephemeral presence of amphipods or other species deposited by an ebbing tide (JNCC, 2015), this pressure is considered to be 'Not relevant'.

As this biotope is characterized by the absence of a biological assemblage apart from occasional and ephemeral presence of amphipods or other species deposited by the ebbing tide (JNCC, 2015), this pressure is considered to be 'Not relevant'.

As this biotope is characterized by the absence of a biological assemblage apart from occasional and ephemeral presence of species deposited by an ebbing tide (JNCC, 2015), this pressure is considered to be 'Not relevant'.