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Earth Science Conservation Review
| Belmore, Ballintempo & Tullybrack Uplands; Knockmore - Pollaraftra | Fermanagh |
| Site number: | 1162 | ||
| ESCC: | IC | ||
| Locality Type: | Karst | Status: | ASSI |
| Grid Reference: | H0850 Approximate | ||
| Google maps: | 54.39901,-7.8768 | ||
| County: | Fermanagh | Council area: | Fermanagh & Omagh District Council |
| Period: | Quaternary, Carboniferous | ||
| Stages: | Holocene, Visean | ||
| Lithostrat: | Dartry Limestone Formation, Glencar Limestone Formation, Knockmore Limestone Member, Meenymore Formation | ||
| Site Description | |
|---|---|
| Highlights: | |
The impressive cliffs of Knockmore Hill form a dramatic backdrop to the northern edge of the Tullybrack uplands. The Knockmore area hosts one major cave system, the Pollaraftra stream cave which lies under a classic fault valley. This 2km fault controlled cave has a number of phreatic zones with fossil passage bypasses and there are significant areas of calcite speleothems. There are numerous smaller speleological sites in the area and groups of fine surface karst features. The major sinks and largest resurgence are associated with Pollaraftra although there are other small swallets and risings. Relict caves are well represented and some are intermittent bat roosts, whilst others have good speleothems and one is a scheduled historic monument. The area (~14km2) has some of the finest surface karst topography in Northern Ireland. | |
| Introduction: | |
The Knockmore - Pollaraftra area is comprised of Knockmore Hill, the limestone scarp rising from the Sillees valley to its south and a dissected hilly area to the north and west. Lying at the northern end of the Belmore - Ballintempo region, the area is bounded further north and to the west by the heavily faulted Glenade Sandstones of Lough Navar, Lough Fadd and Little Dog. To the south lies the main part of the Ballintempo uplands. The main lithology in the area is the Knockmore Limestone and the resulting karst topography consists of numerous small hills, cliffs, closed depressions and dry valleys dominated by the major cliff feature of Knockmore. To the south of Knockmore Hill is an E-W valley under which lies the Pollaraftra cave system. Major speleological sites: Pollaraftra (H080 498) and Legland Rising (H096 496) - 2000m long 73m deep. Minor speleological sites: Lettered Cave (scheduled historic monument REF. FERM 191:40) (H088 504), Whitehouse Cave (25m long) (H067 502), Poulnamuck (100m long) (H068 502), Pollnamansh (60m long) (H068 501), Garrison Cave (75m long) (H088 497), Roadside Pot (20m deep) (H087 500), Meander Cave (H094 494), Arches (H086 500), Pollnamadda (H088 491), Crinoid cavern (H085 493), Relict caves (H074 510, H078 510), Relict caves, Doagh Lough Area (H077 518). Surface sites: Good and extensive limestone pavement, Sheet 191 in grid square H49 09 (approximately located in the 100m grid squares 0E 0N, 0E 1N, 0E 2N, 0E 3N, 1E 0N, 2E 0N, 3E 0N, 4E 0N, 1E 1N, 1E 2N). In grid square H07 50 (approximately located in the 100m grid squares 0E 2N, 1E 2N, 0E 3N, 1E 3N, 1E 4N, 2E 4N). In grid square H08 50 (southeast corner) and H08 49 (northwest corner). Approximate catchment area of Pollaraftra: ~3.5km2. Total surveyed cave: ~2300m. Approximate area of exposed karren: ~4000m2. Total area: ~14km2. | |
| Description: | |
I - Hydrology Allogenic water feeds the main sinks of the Pollaraftra cave which forms a relatively simple linear drainage system. The sinks are located on the fault plane in the valley (~230m amsl) and the water resurges close to the Knockmore-Glencar contact at Legland Rising (~140m amsl). With the exception of a few small stream sinks (e.g. Poulnamuck), diffuse recharge feeds the underground drainage to the north of the Pollaraftra fault and there are a number of small risings below the Knockmore cliff and another at Sraniff. The Screenagh River takes surface water east to the Sillees River. All the discrete surface drainage enters the Pollaraftra valley from the south and sinks at the fault and drains eastwards through the system. The largest surface stream splits in the valley floor with half the water sinking immediately on reaching the fault. The remainder flows a further 200m on the surface before sinking next to the cave entrance doline (Martin's Entrance). Another small stream flows from the east to sink into a pothole, the second (old) entrance. II - Underground Karst Pollaraftra The cave is a linear stream cave which follows the fault closely and is developed in the bedded flank facies of the carbonate mudbanks of the Knockmore Limestone Member. In the first 400m of the cave however there are a number of shale beds within the limestones. A number of inlet tributaries, with associated passages, join the main stream in the initial half of the cave. The second half of the cave leading to the resurgence is characterised by a low level active, often phreatic streamway with a well decorated fossil passage above. In the old entrance chamber the fault is clearly visible and slickensides can be seen. The active streamway initially follows a fracture controlled route from the entrance series and fossil phreatic passages above often converge with it. Just downstream of the first active phreatic section (Sump 1) the passages merge in a canyon averaging 1m wide by 4m high. At this point, ~5mm long, translucent, needle-shaped crystals, are occasionally seen on the matrix of a fault breccia which forms the passage walls. Remnants of the fossil route still exist in the roof of the canyon as far as the waterfall and for a short section, in normal water conditions, the stream flows in a lower impenetrable level below the canyon. The passage size steadily increases and there are good examples of a number of speleothem types. Calcite curtains, stalactites, stalagmites, helictites and false floors with sandstone cobbles cemented to the undersides are present. A 30cm long, piece of bone is also cemented into a piece of false floor on the south wall of the passage and other bones washed out of sediment in this area have been identified as the left radius - ulna of a cow (pers. comm. K. James Ulster Museum, 1994) but were not dated. A 1m x 25cm diameter collapsed stalactite lies in the streamway. The 15m wide 2m high Luncheon Shelf chamber shows classic bedding breakdown as does the Boulder Chamber 100m downstream. In this chamber is a major inlet which can be followed some 200m back through a boulder choke into a streamway in bedding breakdown blocks. Past the Chamber another inlet enters from the north and the passage becomes a high rift with 3 major boulder collapses along its 300m length. Where the canyon is open it is floored with sandstone cobbles and the walls are covered with flood sediment. An inlet joins the canyon from the south before a short cascade leads down to Sump 2 and a climb up the Mud Wall leads to the abandoned upper passages. The fossil passage leading from the top of the Mud Wall is initially controlled by the fault and runs above the active stream which follows a slightly different course some 6m below. The lower active level consists of four phreatic sections (Sumps 2-5) with varying lengths of streamway between each. The active conduit is joint controlled with a number of tight bends. Connection between the upper level and lower level can be made between Sump 2 and 3 where the stream runs in a canyon. The fossil passage is very well decorated beyond a section of wet, soft sediments near the Mud Wall. The speleothems in this area include a cascade of gour pools, helictites, multiple curtains and a large calcite column. There are a number of patches of an unusual form of globular eccentric speleothems, numerous single spots of calcite (~1-2mm) which have the appearance of 'sesame seeds' stuck to the walls. At a significant chamber with a large boulder pile a small inlet enters down a calcited aven which corresponds closely with the position of Garrison Cave. Beyond this 300m of static canal in high (6m) joint controlled canyon lead to a sump (Second Canal Sump). At Canal Sump 1, the water is noticeably peaty in colour, in comparison to the clear water of the static canals. In the passage 100m upstream from the Second Canal Sump are a number of grey laminated clay banks. Minor speleological sites: The most northerly sites of karst - speleological interest in this area are the suite of relict caves in the cliffs which lie on the sandstone - limestone contact. Here, five short caves show classic examples of anastomoses, phreatic passage with vadose entrenchment, small natural arches and fine clastic sediment infills. The hill to the west of Doagh Lough is split by a dry valley with a series of small cliffs and relict caves. Just to the north of the Garrison - Derrygonnelly road, at a small hill, is the most westerly part of this Knockmore Limestone exposure and on its summit is Whitehouse Cave. Entered by a vertical rift, this relict cave consists of a single chamber (15 x 4m) with a boulder slope leading down to the calcite blocked continuation of the controlling fissure. The cave has good soft calcite deposits and some small stalactites, stalagmites and flowstones. Poulnamuck and Pollnamansh which both take small streams draining this hill are small active caves with some high level chambers and calcite speleothems. The Pollaraftra fault scarp exposes the mudbank flank facies in cliffs along the north side of the valley in which there are a number of relict caves. The most significant is Garrison Cave, a steeply descending passage of phreatic origin with a vadose trench. This canyon passage has an infill of fine muds which line the floor. Further into the cave they become wet from a number of small inlets. Good soft calcite deposits and some small stalactites, stalagmites and flow stone are present. Further down the valley, where the fault is less distinct, are a number of other relict caves and Meander Cave which takes a small stream. III - Surface karst The cliffs of Knockmore expose the massive carbonate mudbank facies. The many small cliffs to the southwest expose the bedded mudbank flank facies of the Knockmore limestone. These limestones generally dip gently to the south. The limestone pavements on Knockmore and on the bench running southeast towards Noon's Hole are the best developed pavements in Fermanagh with small areas of clint and grikes interspersed with vegetation growing on drift material. The pavement displays many classic 'Karren' features in addition to clints and grikes e.g. solution pans, solution pits and solution runnels. The bench also has a number of solution dolines (oriented on major fissures), potholes (e.g. Pollnamadda and Crinoid Cavern) and a line of small sinks fed from the sandstone uplands to the west. At Legland the water from Pollaraftra rises and over a distance of 5m, sinks and rises again before flowing down a series of waterfalls and cascades. Above the rising, at the line of small cliffs, there are a number of detached limestone blocks with a boulder field below. The fault on which the Pollaraftra valley is formed has a down throw to the south. It divides Knockmore from the limestone benches to the south. The resultant topography is a striking scarp slope with limestone cliffs on the north side of the valley and a less steep slope incised by stream valleys topped by small sandstone crags to the south. In the stream valleys are good exposures of the Dartry Limestone and overlying Formations. Exposures of the Meenymore Formation show bedding planes with well developed ripple marks. | |
| Importance: | |
The Pollaraftra system is the best example of a fault controlled cave in Northern Ireland and within the system are a number of features which are of particular importance. The water which enters the system is generally unpolluted by habitation and present farming practice. There are very good examples of a wide range of forms of calcite deposit in the fossil passage past the Mud Wall and the 'sesame seed' botryoidal calcite is particularly worthy of note. Clastic sediments are not extensive but do show features (mammalian bones and the glacial flour clays) which are of additional interest to the palaeomorphological records generally held in cave sediments. The population of Gammarus duebeni celtictus in static pools above the Mud Wall are one of the few cave dwelling populations known in N. Ireland. There are a number of minor speleological sites which have features of importance. Whitehouse Cave has good soft calcite deposits, the Doagh Lough Caves have excellent examples of 'keyhole' passage cross sections and anastomoses. Both of these sites and Garrison Cave have bat roosts which support small intermittent populations. Knockmore Cliff is one of the best exposures of carbonate mudbank in N. Ireland and with the fault scarp exposure of the mudbank flank in the Pollaraftra valley comprises a good example of these lithologies. Within the Pollaraftra valley, the fault orientated sink line and sink capture are the best example of this feature in N. Ireland. The extensive pavement in this area is typical of karren development in Fermanagh, being heavily dissected and interspersed with drift material. The solution and collapse dolines, dry valleys and limestone pavement are abundant and form part of the unique suite of surface karst feature in the Knockmore - Pollaraftra area. The belt of limestone pavement trending south from Pollaraftra towards Noon's Hole is the most extensive area of limestone pavement in N. Ireland. | |
| Interpretation: | |
I - Hydrology The 3km2 catchment for the cave is almost exclusively south of the fault with two possible exceptions; one inlet just downstream of the Boulder Chamber may feed from the north as may the peaty pool at Canal Sump 1. The water entering at Canal Sump 1 may originate from the Road Side Pot area. In the south it is uncertain where the karst watershed lies between the Pollaraftra drainage and the Noon's drainage. The series of sinks become progressively younger to the west of the cave entrances as a result of sink capture and are probably feeding the recently explored inlet passage. Evidence of flooding and backing up of the stream is provided by the fine sediment deposits on the walls of the canyon passage downstream of the Boulder Chamber. During periods of heavy rain, water backs up at Sump 2 and can flow over the top of the Mud Wall. Water from the active streamway may add water to the static canals, but they are also topped up from the active Canal Sump 1 during flood. The presence of flood debris calcited into stalactites near the 'Dead Chicken' stalactite and in the Sump 1 Bypass passages, also indicate occasional flooding to the roof. II - Underground Karst Pollaraftra appears to have a relatively simple history of development compared to other cave systems in the area. This could be due to the strong fault control. The cave has active phreatic, epiphreatic and fossil phreatic sections interspersed with major breakdown chambers and vadose canyon. The biggest of the breakdown chambers, the Boulder Chamber, is situated at the confluence of the two major streams and its size is probably related to an increase in corrosion and corrasion in this area, in conjunction with subsequent bedding failure. The presence of calcite canopies and remnants of false floors indicate a period of infill and later reworking of clastic sediments in the cave. The size of some calcite speleothems which have collapsed and are lying in the stream suggests a substantial period of calcite deposition in what is now an active vadose passage. The fine needle-shaped crystals which are occasionally present have been tentatively identified as Mirabilite Na2SO4.10H2O, although chemical analysis is required to confirm this. This salt is derived from the breccia matrix and presumably crystallises due to evaporation of matrix water at the rock-air interface. This mineral is very rare in temperate caves and may crystallise at this point as there is a substantial draft where it is found. The 'sesame seed' calcite , common in an area of fossil passage near the static canals, is a form of botryoidal calcite not seen elsewhere in Northern Ireland. The banks of grey laminated clays in the passage near the terminal choke are deposits of glacial flour which may be varved, indicating deposition in an underground lacustrine environment. The survey of Pollaraftra shows that the end of explored section is close to resurgence at Legland and the general cave morphology suggests that a fossil resurgence exists although it may be completely collapsed or infilled. Also from the survey it appears that Garrison cave represents a remnant of the Pollaraftra system which relates to the high level passages above the Mud Wall. The Doagh Lough relict caves lie on the faulted contact between the Knockmore Limestone - Glenade Sandstones and this contact may have controlled the location of the caves. Another possible controlling factor may have been the presence of an ice edge and/or subsequent glacial erosion leaving remnants of pre- interglacial cave systems. III - Surface Karst Faulting and the effects of glaciation have been major influences in shaping the present topography. The Pollaraftra fault and the fault to the north of Whitehouse Cave have clearly controlled the valley form and development. The cliffs of Knockmore are a glacially truncated section through a mud bank. Karst features such as the dry valleys, doline sinks and spring lines have been superimposed on this glacial topography. | |
| Notes: | |
CONCLUSION The Knockmore - Pollaraftra area has been demonstrated to contain surface and underground karst features which are of significant karst geomorphological and geological interest and quality. There are also a number of biological sites associated with the karst which support intermittent bat populations and other faunal populations of importance in a national context. For site specific information see; Key Site 414 - Pollaraftra Key Site 415 - Legland Rising Key Site 416 - Lettered Cave Key Site 417 - Whitehouse Cave Key Site 418 - Poulnamuck Key Site 419 - Pollnamansh Key Site 420 - Garrison Cave Key Site 421 - Roadside Pot Key Site 422 - Meander Cave Key Site 423 - Arches Key Site 424 - Pollnamadda Key Site 425 - Crinoid Cavern Key Site 426 - Lough Doagh relict caves Key Site 427 - Limestone pavement. For information and reference lists on the systems and features of other karst areas within the Belmore, Ballintempo and Tullybrack Uplands see; Key Site 1158 - Belmore Key Site 1159 - Boho Key Site 1160 - Reyfad-Carrickbeg Key Site 1161 - Noon's Hole-Arch Cave. BIOLOGICAL INTEREST There are no records of biospeleological observations or collections undertaken in the Knockmore - Pollaraftra area, and limited observations and records of bat populations, prior to this study. A small faunal collection was made in Pollaraftra as part of this review. Identification was undertaken by Dr. R. Anderson of the Department of Agriculture. Bat observations were limited to looking for droppings and cursory examinations of accessible and potential sites. In Pollaraftra, the stream carries trogloxenes into the cave and brings organic material into the system providing food for faunal populations. A number of the sediment banks are covered in worm casts and fungal growths are sometimes present on this washed-in organic material. The presence of Collembola sp. (spring tails) is common on the surface of static pools throughout the cave and in the minor cave sites. A small population of approximately twenty individual fresh water shrimps (Gammarus duebeni celtictus) were found living in a static pool above the Mud Wall ~1km from the entrance. It is unlikely that this area is inundated by flood water more than once or twice a year and, as this species has a life span of approximately one year (pers. comm. Dr. R. Anderson), this could be a cavernicolous population. A single specimen of the spider (Porrhoma pygmaeum) was collected from just downstream of Sump 1, 100m from the entrance. This spider is not rare on the surface being found in wet areas in undergrowth (pers. comm. Dr. R. Anderson). Though not often found in caves it is considered by some spider specialists to be able to maintain subterranean populations (Chapman, 1993). It does not appear to have been previously recorded from Irish caves. Specimens of an unidentified Hemiptera sp. (water bug) and an unidentified Chironomid were also collected in Pollaraftra. In many of the relict caves there are populations of the common cave spider (Meta menardi), herald moth (Scoliopteryx libatrix) and fox (Vulpes vulpes). Evidence of bat habitation has been recorded from the entrance chambers of Pollaraftra, Garrison Cave (The Leisler Spring 1994), Whitehouse Cave (pers. comm. N.I. Bat group), the Doagh Lough Caves and a number of the relict caves in the valley between Garrison Cave and the Legland rising. | |
| Keywords | |
|---|---|
| Minerals: | Aragonite, Calcite, Mirabilite |
| Rocks: | Limestone, Mudstone, Shale |
| Structures: | bedding, fault, joints, slickensides |
| Relations: | Glacio-fluvial sediment |
| Geomorph: | breakdown, clastic sediments, doline, flowstone, gour pool, helictite, organic sediments, sinkhole, speleothem, stalactite, stalagmite, straw |
| Measurements | |||||
|---|---|---|---|---|---|
| Length: | 2300 m | Width: | Height: | ||
| Depth: | 73 m | Area: | 14 km2 | ||
| Access | |
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| Planning: | HISTORY OF EXPLORATION According to Coleman (1965), Plunket excavated fifteen caves in Knockmore Hill during the 1890's and made a number of archaeological finds. The first cavers to enter Pollaraftra were a mixed group of Yorkshire Ramblers and Craven members in 1949 and by the end of 1951 the cave had been explored to within a few hundred metres of the resurgence. Farr and Solari in the 1970's dived downstream as far as Sump 5 completing the exploration to date with the exception of the 1994 extension of the inlet in the Boulder Chamber 200m upstream towards the second sink. |
| Management: | |
Internal threats: The Pollaraftra streamway is a high energy cave passage with medium energy passage above the regular flood level. Past the Mud Wall there are areas of medium and low energy cave. Some protection for this section of cave from large numbers of cavers is inherent in its remote position, over 1 km from the entrance. The main areas of calcite speleothems at the gour pools and before the canals have, to date, been generally unaffected by cavers. Doagh Lough caves are isolated in the cliff above the lough and are of little interest to the general caving population. As they display a number of fine speleological features they could be regarded as good sites for designation. Both Garrison and Whitehouse caves are vulnerable as they are relatively easily accessible to casual uninformed visitors. External threats: With the exception of the sinkhole next to the cottage at H084 496 and Roadside Pot H087 500 which have been badly polluted with farm and household waste, the important surface karst features and the water quality of the area are in good condition. The landowners have fenced a number of dolines in the area around Meander cave, presumably to prevent stock from straying into them. | |
| Threats: | Accidental damage by cavers or casual visitors; farm, household waste. |
| Uses | |
| Potential: | There are a number of surface and underground sites related to Pollaraftra where further exploration could be undertaken: extending the main inlet upstream; extending the inlet just downstream of the Boulder Chamber; diving at Sump 3 and the Second Canal Sump; entering in the resurgence area and working upstream; following the fossil phreatic passage crossing Boulder Chamber at right angles; surface digging in the area to the north of Pollaraftra. The connection of Garrison cave to Pollaraftra by digging could be seen as an exploration objective. The benefits of this exploration are however, probably outweighed by the importance of maintaining the integrity of Garrison Cave. Study of the clastic and chemical sediments in Pollaraftra and some of the minor sites would be of interest in building up knowledge of the speleogenesis of the area. |
| References (28) | |||
|---|---|---|---|
| Adair, F., 1974. Notes on the distribution and behaviour of the cave spider, Meta menardi (Latr.) in Ireland (Araneae Argiopidae). Irish Naturalists Journal, vol. 18 pt. 2, pp.40-41. | |||
| Barnes, S., 1994. Preliminary Hydrological Investigation of the Area between Carnlough and Waterfoot, County Antrim, Northern Ireland. (Thesis) University of East Anglia. | |||
| Boon, M., 1977. Down to a Sunless Sea. | |||
| Brook, D., 1971. Notes on the Reyfad Area. University of Leeds Speleological Association Review, numb. 8. | |||
| Clark, S., 1975. Hull University Speleological Society Expedition to Northern Ireland 1975. Hull University Speleological Society. | |||
| Coleman, J., 1965. The Caves of Ireland. Anvil Books, Tralee. | |||
| Drew, D.et al., 1977. Caves and Karsts of Ireland. In 7th International Speleological Congress British Cave Research Association. | |||
| Fletcher, T.P., 1977. Lithostratigraphy of the Chalk (Ulster White Limestone Formation) in Northern Ireland. Report of the Institute of Geological Sciences, vol. 77/14. | |||
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| Jameson, H.L., 1896. On the Exploration of the Caves of Enniskillen and Mitchelstown for the R.I.A. Flora and Fauna Committee. Irish Naturalists Journal, vol. 5, pp.93-100, plates 1. | |||
| Jones, G.Ll. & McKeever, M., 1987. Sediments and Palynology in Marble Arch Cave. Cave Science, vol. 14 numb. 1. | |||
| Kelly, J.G., 1989a. The late Chadian to Brigantian Geology of the Carrick-on-Shannon and Lough Allen Basins, North West Ireland. (Thesis) N.U.I. | |||
| Kelly, J.G., 1989b. Geology and Caves of Cuilcagh Mountain, Counties Fermanagh and Cavan. Irish Speleology, vol. 13. | |||
| Kelly, J.G., 1990. Reyfad Pot. Irelands Deepest (and Longest?) Descent 96. | |||
| Kelly, J.G., 1995. The Asbian Geology of Cuilcagh Mountain Area, Co's Fermanagh and Cavan, Ireland. Initiation, growth and decline of a tectonically controlled carbonate ramp. In European Dinantian Environments II. | |||
| Legg, I.C., Johnston, T.P., Mitchell, W.I. & Smith, R.A., 1995. Geology of the country around Derrygonelly and Marble Arch. Memoirs of the Geological Survey Northern Ireland, vol. Sheet 44,56,43. | |||
| Magennis, P., 1874. The Ribbon Informer. A Tale of Lough Erne. Frederick Bell and Co. | |||
| Martel, E.A., 1897. Irelande et Cavernes Anglaises. Libraire ch. Delagrave., Paris. | |||
| McKay, S., 1987. The Chemical Differentiation of Carbonate Aquifers in the Karst of North-West Ireland, with a view to predicting the type and length of cave system under Belmore Mountain. (Thesis) University of Bristol. | |||
| McKay, S., 1989. A study of Carbonate Aquifers in the Karst of North West Ireland. Irish Speleology, vol. 13. | |||
| Mitchell, W.I., 1983. High grade Dolomite deposits in the Belcoo - Boho area of County Fermanagh. (Unpublished Report) Geological Survey of Northern Ireland Open File Reports, vol. 68. | |||
| Nichols, A., 1970. Cambridge University Caving Club Expedition to Ireland, 1970. Cambridge University Caving Club. | |||
| Oswald, D.H., 1955. The Carboniferous Rocks between the Ox Mountains and Donegal Bay. Journal of the Geological Society of London, vol. 111, pp.167-186. | |||
| Sheridan, D.J.R., 1972. Upper Old Red Sandstone and Lower Carboniferous of the Slieve Beagh Syncline and its setting in the northwest Carboniferous basin, Ireland. Special Papers of the Geological Survey of Ireland, vol. 2, pp.1-120. | |||
| Williams, P.W., 1970. Limestone morphology in Ireland. In Irish Geographical Studies, pp.105-124 Queens University of Belfast. | |||
| Map(s): | The following areas are marked and labelled on 1:10,000 sheets 190 and 191 as follows: K1. Doagh Lough. Relict caves and dry valley. K2. Whitehouse Cave and Poulnamuck. K3. Small area of limestone pavement. K4. Pollaraftra Cave and associated surface features. K5. Knockmore Hill, cliff and area of limestone pavement. | ||
| Record type: | ESCR report | ||
| Entered by: | E M Porter | ||
| Last updated: | 23 Dec 2003 | ||
| Enlander, I., Dempster, M. & Doughty, P., 2026. Belmore, Ballintempo & Tullybrack Uplands; Knockmore - Pollaraftra, County Fermanagh, site details. [In] Earth Science Conservation Review. https://www.habitas.org.uk/escr/site.php?item=1162. Accessed on 2026-11-04. |
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