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Earth Science Conservation Review
| Kearney Point – Knockinelder Bay – Lower Palaeozoic | Down |
| Site number: | 1352 | ||
| Locality Type: | Coastal Section, Foreshore | Status: | ASSI |
| Grid Reference: | J648512 | ||
| Google maps: | 54.38319,-5.46333 | ||
| County: | Down | Council area: | Ards & North Down Borough Council |
| Period: | Silurian | ||
| Stages: | Llandovery | ||
| Site Description | |
|---|---|
| Highlights: | |
The outstanding highlights are: 1. Examples of a beautifully exposed orthorhombic system of kink bands which is figured and described in the Encyclopaedia of Earth Sciences (1987) and in several internationally used text books on structural geology (eg Suppe (1985), Ramsay and Huber (1987)) 2. Some very unusual sub-horizontal sheets of Caledonian lamprophyre (the ‘Kearney sills’) 3. Excellent and well-exposed examples of several key elements of the structural fabric of the British and Irish paratectonic Caledonides, including convergent and divergent cleavage fans and clockwise transecting cleavage. All of these rocks and structures are easily and safely accessible at low- or mid-tide from a narrow coastal path on National Trust property. There are small car parks at either end of the section. Thus it is probably as a teaching laboratory for structural geology that the site has its greatest value. Teaching opportunities range from introductory demonstrations of the elements of folding and the geometry of dykes and sills to Honours-level exercises on the three-dimensional geometry of transecting cleavage and/or kink bands. | |
| Introduction: | |
The site (Fig. 1) lies on the outer or Irish Sea coast of the Ards Peninsula and thus within the Central Belt of the Southern Uplands - Down - Longford Terrane. The Terrane is now generally, if not quite unanimously, regarded as a late Ordovician – early Silurian accretionary prism (e.g. Anderson in Mitchell (ed.) 2004). It is largely composed of well-bedded deep marine sediments. Sandy or silty grey turbidites are interlayered with grey shales, the latter now generally converted to slate. The coast from Knockinelder Bay east to Kearney Point and then north to Kearney Village is an almost continuous wave-cut platform in the Kearney Siltstone Formation (Hawick Group) of Upper Llandovery age. According to the accretionary prism model these rocks were deposited on oceanic crust at or near the north-western margin of the Iapetus Ocean. During late Ordovician and Silurian Periods the ocean closed by north-westward subduction of the dense oceanic crust beneath the neighbouring Laurentian continent. The less dense sediments, which had been deposited on that crust, were scraped off and accreted as a sequence of slabs or ‘tracts’ to the leading edge of the continent (see Anderson, in Mitchell (ed.) 2004, Fig.4.2). The oldest, north-western, tract was added first, and was followed south-eastward by incrementally younger tracts. Seventeen tracts have now been recognised in County Down, individual tracts ranging in width from a few hundred metres to over four kilometres. The Kearney site lies entirely within the Portaferry Tract, currently the fifteenth in the sequence, and its sedimentary rocks, part of the Kearney Siltstone Formation, have the lithological characteristics of the Hawick Group. The fine grained turbidites are mainly siltstones but include some fine-grained sandstone. Turbidites and interbedded shale are so rich in carbonate that careous or honeycomb weathering is common. While there are no obvious primary red beds at the Kearney site they do occur elsewhere in the same tract and in the same formation. Hawick Group sediments are rarely fossiliferous and no fossils are known from the Kearney Formation but at Quintin Bay, two kilometres south of Kearney Point, the formation rests conformably on the Tara Sandstone Formation in which thin bands of black shale have yielded a Monograptus crispus Zone graptolite fauna (Anderson and Rickards 2000). This implies that the Kearney Siltstones were deposited very late in the Llandovery Epoch. At Kearney there are multiple repetitions of individual beds by folding so that the total stratigraphic thickness of the strata exposed at the site may be as little as 100 metres. During accretion the sediments were deformed, cleaved, metamorphosed and intruded by igneous rocks. In some tracts it is possible to recognise the imprints of four distinct sequential phases of ductile deformation, of which the first is invariably the most important. This initial accretionary event produced tight (locally isoclinal) upright folds (F1) and a slaty cleavage (S1) which is particularly well developed in the shale interbeds. In general the northern limbs of the anticlines are thicker than the southern so that a majority of beds young or “face” to the north on excellent sedimentary evidence. The tectonic fabric produced during this first accretionary phase is extremely well exposed at Kearney, with text book examples of the upright folds and the associated cleavage (Plates 1, 5, 8, 9, 11 and 13). At some of the fold hinges the cleavage refracts quite beautifully in passing from siltstone to slate, so forming well developed convergent and divergent cleavage fans (Plate 5). Perhaps surprisingly, the slaty cleavage is not exactly axial planar to the contemporary upright folds but in plan view can be seen to strike a few degrees clockwise of the fold traces in a manner which is now known to characterise the initial (D1) deformation in large areas of the paratectonic Caledonides of Britain and Ireland (Anderson 1987). F1 folds and S1 cleavage in County Down were subsequently refolded about two sets of minor (decimetre to metre-scale) folds (F2 and F3) with gently inclined axial surfaces and hinges plunging gently east. The F2 and F3 folds are very similar in appearance. Both tend to have straight limbs and sharply defined hinges. Both tend to be spatially and temporally associated with crenulation cleavages (S2 and S3) parallel to their axial surfaces, again in a manner characteristic of much of the British and Irish paratectonic Caledonides. These crenulation cleavages are seen as an obvious small scale wrinkling of the slaty cleavage (Plate 7). In the few outcrops in Down where F2 and F3 occur together the folds which verge to the south (ie with respect to the long limbs the short limbs of the folds are rotated top to south) are refolded by the folds which verge to the north. On this basis the south-verging folds are regarded as F2 and the north-verging as F3. The few folds of this type at Kearney are north-vergent and so regarded as F3. No clear imprint of the second deformation has been recognised at Kearney. Where the slaty cleavage was intense, it provided the essential, ‘card-deck’, mechanical anisotropy for the development of an orthorhombic system of kink bands (F4 in the deformation sequence). (A kink band is a “thin band or plate transverse to the foliation and bounded by the axial surfaces of a pair of folds of opposite sense” (Anderson 1969)). Excellent examples of vertical kink bands, each a few centimetres wide but some extending for several metres along their length, are beautifully exposed on the surface of the wave-cut platform at the eastern end of Knockinelder Beach (Plates 2 and 3).The geometry of this system, as measured and described by Anderson (1964 and 1969), has been widely quoted in the literature on kink band definition and geometry. If tectonic structures were allotted type localities then Kearney would be a strong candidate for designation as a type kink band locality. Descriptions, data and photographs of the Kearney kink bands appear in the Encyclopaedia of Earth Sciences and in a number of international text books (e.g. Suppe 1985, Ramsay and Huber 1987). Careful mapping of the Kearney outcrops reveals the presence of numerous faults, their traces typically marked by gullies between the rocks rather than by exposure of the fault rock itself. The majority of these faults are steeply dipping strike-slip (or wrench) faults, displacing fold traces and/or dykes laterally. Most of the strike faults effect sinistral displacements of a few metres and strike at about 015 degrees. The conjugate dextral faults are less numerous, tend to effect smaller slips and strike at about 125 degrees (Anderson 1987b). The deformed sediments of the Southern Uplands - Down - Longford Terrane are host to some thousands of minor igneous intrusions of Caledonian age and of lamprophyric composition. The vast majority are thin (less than 2m thick) vertical or sub-vertical sheets, somewhat arbitrarily described as ‘dykes’, because of their steep orientation, even though many are at least locally concordant with the vertical beds they intrude. The Kearney Point outcrops are special in that they not only include typical examples of such dykes but there are also some ten gently inclined lamprophyre sills or sill fragments (Plate 8). While steeply inclined lamprophyre dykes occur throughout the Southern Uplands – Down – Longford Terrane, gently inclined sills appear to be unique to Kearney and to the coastal outcrop immediately to the north HISTORY The first detailed reference to the geology of the site appears to be in the 1871 Memoir of the Geological Survey of Ireland (Traill and Egan 1871). The 19th century geologists had neither the knowledge nor the techniques to achieve an understanding of the stratigraphy and structure of the sediments so in dealing with the solid geology the memoir concentrates almost completely on describing and recording the numerous dykes and sills. One of the small sills at Kearney Point is beautifully and accurately illustrated in a line drawing which forms the frontispiece to the memoir and is reproduced as Figure 2 of this report. Reynolds (1931) published detailed field and petrographic descriptions of the lamprophyre dykes and sills of the Ards Peninsula. Based on her examination of some 260 examples, she found it possible to divide the dykes into an Older or ‘Crushed’ Series and a Younger or ‘Uncrushed’ Series. The Older Series dykes are all less than two metres thick, visibly cleaved and under the microscope appear altered or decomposed to a degree that makes the original mineralogy and hence petrographic classification difficult. However Reynolds concluded that all are lamprophyres – “mainly minettes and rarely vogesites”. In contrast the Younger Series Dykes are typically 1 to 15 metres thick, uncleaved and commonly of a fresh crystalline appearance. Reynolds found it possible to subdivide the Younger Series into some nine petrographically distinct varieties, five of which are characterised by hornblende and four by biotite and pyroxene. The Cloghy Fault, some 4 km north of Kearney, not only forms the northern boundary of the Portaferry Tract but it is also the northern limit of the Older Dykes. Several hundred Older Dykes crop out in the southern Ards and in Lecale, with at least 15 examples at Kearney. Interestingly Reynolds regarded the gently inclined lamprophyre sheets at Kearney as part of the Older Series even though none of the sills show evidence of cleavage or crushing. The majority of the Younger Series dykes crop out north of the Cloghy Fault but about ten, widely spaced, examples of these much fresher and generally more massive rocks occur in the two tracts to the south of the Fault. One example, a biotite minette, crops out on the coast SE of Kearney Village (see later description). Anderson (1962) completed a field-based thesis on the stratigraphy, sedimentology and structure of the Lower Palaeozoic rocks of the Ards Peninsula. In terms of their relevance to the Kearney Key Site his most important subsequent publications are the studies of kink band geometry (Anderson 1964 and 1969). Descriptions of the stratigraphy and structure of the Silurian sediments may be found in Anderson and Cameron (1979), Anderson (1987a, and 2001), and Barnes, Anderson and McCurry (1987) with the most recent summary in Chapter 4 of the Regional Guide to the Geology of Northern Ireland (Anderson in Mitchell (ed.) 2004). | |
| Description: | |
The Kearney Site is important because of the occurrence of dykes, sills and structures which generally range from a few centimetres to a few metres across. To facilitate their location this chapter of the report offers GPS-based 10-figure Irish Grid references. Geologists navigating by conventional map and compass methods should ignore either the fifth and tenth integers or the fourth, fifth, ninth and tenth integers of the Irish Grid refernce depending on the scale of the map available to them. A large-scale plan of the site with the more important localities labelled is provided as Figure 1 of this report. Visitors to the site are advised to use one of the two car parks labelled on Figure 1. Most people will then use the coastal path and the (minor) Kearney Road to complete a circuit of about 2.5km. It is strongly advised that this circuit be made in an anticlockwise direction. This is because the structures are generally easier to find and best viewed looking ENE i.e. along the regional Caledonoid strike of the strata and down the ENE plunge of the many folds. Some of the most intense D1 deformation in County Down occurs in a 30-metre-wide strike parallel (ie trending at 065 degrees) zone, which crosses the coast at each end of Knockinelder Bay and again at Kearney Village. It is quite beautifully exposed on a smooth wave-cut rock platform about 2m above high water mark at the east end of Knockinelder beach (IJ 64239 51365) (Plate 1). Both the 10 to 80cm thick siltstone beds and interleaved slates show intense cleavage and numerous upright, tight or isoclinal, folds. However note that the flat topped outcrop is at acute angle to the easterly plunge of the fold axes (between 20 and 50 degrees toward 065 degrees) and this non-profile section makes the folds appear tighter than they are. The intense composite fabric of subparallel bedding and cleavage imparts a “card-deck” rheology to the rocks, ideal for the subsequent development of kink bands. Several excellent examples of vertical or steeply inclined kink bands (Plates 2 and 3) are exposed in profile section on the surface of the platform, particularly in the vicinity of some rusty fence posts (Point A on Fig. 1, Irish Grid IJ 64249 51351). The kink bands are typically less than 15 cm thick. Note that although some bands show weak fractures or joints along the axial surfaces these are not faults. The offset or displacement of the kink band is effected by folding alone. The kink bands here and throughout the Ards Peninsula are nearly all steeply inclined and developed in a steeply inclined foliation. Thus they displace the foliation to the right (dextrally as in Plate 2) or to the left (sinistrally). At this locality and in the Ards generally, kink bands of dextral displacement outnumber sinistrals in a ratio of about 2 to 1. Conjugate pairs of dextral and sinistral kink bands are not common but several pairs occur at this locality. In some cases (as in the example on Plate 3) one or both of the kink bands fail to continue beyond the line of intersection and the two appear to be exactly contemporary. In other cases one band cuts across and displaces the other and so is at least marginally the younger. Examples of both relationships can be seen in the few square metres around the bases of the metal fence posts at Locality A. In either case note that the kinking effects a horizontal shortening in the plane of the foliation and that the dextral and sinistral pairs are approximately symmetrical about the foliation and thus the direction of shortening. Both dextral and sinistral bands make an angle of about 60 degrees with the foliation (Anderson 1964, 1969) so that, unlike pairs of shear fractures, the bands subtend an obtuse angle about the direction of shortening.. The rotation of the foliation in the band is a product of slip on that foliation. The slip not only produces rotation but it first opens and then closes the foliation in the band. If rotation does not continue to completion (symmetry of cleavage about the axial surface) the foliation (cleavage) appears much more open and obvious within the band than outside it – as in Plate 2). For development of these and other facets of kink band geometry see Anderson (1969). Continue south-eastward for about 150m along the outer, coastal, side of the fence to locality B on Figure 1 (IJ 64346 57206). In this distance the intensity of folding and cleavage diminishes and several Older Series lamprophyre dykes occur. At B, immediately west of a sharp corner in the fence, there is a typical example of an Older Series Dyke, 64 cm thick and cut by quartz-filled tension gashes (Plate 4). While generally bedding-parallel, the dyke offsets from one bedding plane to another at this point. A “bridge” of sediment effectively separates the dyke into two parts, each part wedging out into a sharp point, the decreasing dilation effected by one part of the dyke being gradually replaced by increasing dilation on the other part (see Plate 4). Walk a further 130m south eastward to point C on Figure 1 (IJ 64443 51120). C is a few metres on to the rock immediately south of the southernmost limit of grass on Kearney Point. Look east to view a superb profile section of an upright F1 anticline with associated and well developed S1 slaty cleavage (Plate 5). The cleavage clearly fans so that in the siltstone beds the cleavage surfaces converge downwards in what is known as a convergent fan while in the slate interbeds the cleavage converges upward in a divergent fan. Sharp refraction of the cleavage occurs at each junction between siltstone and slate. Climb onto the crest of the anticline to stand on the well exposed folded bed that forms the present erosion surface. The fold clearly plunges east, at between 8 and 18 degrees toward 063degrees. The S1 cleavage intersects with the bedding plane to form a text-book quality intersection lineation which also plunges eastward, approximately but not exactly parallel to the F1 fold hinge. Careful examination shows that the plunge of the intersection lineation varies from one limb of the fold to the other and in fact varies systematically with its position on the fold. This is a classic indication that the cleavage is not axial planar to the fold but transects it. While the transection is not particularly obvious at this locality, careful observation shows that in plan view the cleavage strikes between 2 and 7 degrees clockwise of the fold trace. (The fold trace trends in direction 063 degrees and the cleavage strikes between 065 and 070 degrees.) This is an example of the clockwise transecting cleavage geometry now recognised in many areas in the southern parts of the Southern Uplands – Down - Longford Terrane, in the English Lake District and in folded lower Palaeozoic rocks in central and southern Ireland. The geometry is consistent with sinistral transpression during closure of Iapetus (see Anderson 1987b for detail and discussion). There are further fold hinges, synclinal and anticlinal, a few metres to the south in which demonstrate the same clockwise transection in plan view Continue 100m north-eastward to locality D (Fig 1) where an isolated and pointed sea-stack protrudes to a height of 4m from the surrounding shingle (IJ 64481 51241). The area immediately around the sea-stack offers the best outcrops of the F3 folds and S3 crenulation cleavage at the Kearney Site. 10m east of the stack and 1m south of a 40cm lamprophyre dyke at IJ 64491 51240 there are several angular (or chevron) F3 folds plunging gently eastward (Plate 6). These refold the already vertical beds and the slaty cleavage. Looking ENE at the folds their short limbs (generally about 20cm long) are rotated with respect to the long vertical limbs in an anticlockwise sense toward the north (Plate 6). The folds thus verge northward and on that basis are attributed to the F3 deformation phase in south Down. The folds are spatially associated with a crenulation cleavage. The crenulations of the earlier slaty cleavage are both typical and obvious on the northern faces of the 4m-high sea stack (Plate 7) and indeed are typically much easier to identify than the S3 cleavage itself. The crenulations form along the lines of intersection between the steep S1 and flat-lying S3. As explained in the introduction, there are several gently inclined sills of lamprophyre at Kearney Point. The most interesting and photogenic example lies some 150m due eastward at Locality E (IJ6463651238). The sheet of grey-pink lamprophyre is some 25cm thick and covers an irregular area of about 30m by 10m. The sill neatly cuts across an F1 anticline and syncline (Plate 8) and inclines at about 6 degrees to the north. It is interesting to compare Plate 8 with the excellent line drawing from Traill and Egan’s Geological Survey Memoir of 1871, reproduced as Figure 2 of this report. There are several other gently inclined lamprophyre sheets immediately to the north-east and to the south, some of them probably eroded outliers of the main sheet (see Fig. 1 for locations). Pink calcite veins are common in the host sediments adjacent to the sills. The sediments consist of laminated and careous siltstone beds up to 0.8m thick interlayered with thin bands of slate (originally shale). With considerable difficulty, experience and a good hand lens it is possible to discern a tectonic grain elongation or “stretching direction” in the slates at Locality E, though this is easily confused with fine S1/S3 crenulations which are also present. The lineation plunges gently ENE, in the plane of S1 and approximately parallel to the F1 fold axis (See Anderson 1987b for discussion). At locality F (IJ6469251268) there is an excellent profile section of a tight, upright, F1 syncline (Plate 9). The profile clearly demonstrates the flattening effected by compression on the fold geometry. Each of the folded beds is markedly thicker at the fold hinge than on the fold limbs. The siltstone beds are as much as twice as thick at the hinge as on the limbs and the interlayered slates demostrate even larger ratios. Careful examination of the fold again shows that the cleavage, though apparently axial planar when viewed in the profile section, is a few degrees clockwise of the axial surface in plan view. Continue east and then north around the point toward Kearney village. On either side of Port Down there are several thin Older Series lamprophyre dykes with interesting examples of intersection and lit-par-lit injection structures. However if you search for these please note that the intertidal outcrop in this area is often dangerously slippery. At Locality G (IJ6506251754), a 1.2m thick Newer Series dyke of grey-black biotite-bearing minette has been intruded, generally concordantly, in north-facing thin siltstones and slates. The dyke may be traced for over 100 metres parallel to the strike of the host sediments as a slightly irregular and branching vertical wall standing up to 1.5m above the shingle (Plate 10). The dyke is thicker than any of the Older Series intrusions at Kearney. The rock of which it is composed is clearly more erosion resistant, fresher and has a more obviously crystalline texture. Fifty metres north of the dyke the sediments are once again intensely cleaved and folded (Plate 11) in what is apparently the along-strike continuation of the zone of intense folding described at Locality A. Tight or isoclinal folds, some with sheared out limbs, well developed S1 cleavage and some honeycomb weathering again characterise the zone. At Locality H (IJ6508251829, or 30m on a bearing of 108 degrees from the SE corner of the most easterly cottage (Number 7) in Kearney village) there is excellent exposure of an anticline with variable plunge and evident clockwise transecting cleavage (Plates 12 and 13). The fold hinge trends at 055 degrees and the plunge varies between about 15 degrees westward through horizontal to 23 degrees eastward so that within 7 metres along the hinge two culminations are separated by a saddle (Plate 12). Other folds in this zone of intense D1 deformation also demonstrate variable plunge due to high and inhomogeneous strain. Looking eastward along the fold hinge (Plate 13) it is readily possible to discern the trace of the local S1 cleavage on top of the folded bed and this is clearly transecting. The cleavage strikes at 076 degrees and dips at 84 degrees northward. Thus in plan view the angle of clockwise transection of fold by cleavage is some 21 degrees. The plunge of the bedding/cleavage intersection lineation once again varies, systematically and dramatically, with position on the fold. In the slates at Locality H it is again possible to discern a weak grain elongation or stretching direction (X1) that plunges between 18 and 30 degrees toward 070 degrees (See Anderson 1967b for discussion and interpretation of the stretching lineation). | |
| Importance: | |
National geology: Interpretation of the tectonic structures at Kearney has been important to the understanding of deformation in the Southern Uplands - Down - Longford Terrane. The gently inclined sheets of lamprophyre at Kearney Point (the “Kearney sills”) appear to be rare or even unique in the paratectonic Caledonides of Britain and Ireland. International geology: The outcrops at the eastern end of Knockinelder Bay, have been historically important in establishing the elements and interpretation of the geometry of kink bands. Geometrical data, photographs and diagrams obtained at Knockinelder appear in the Encyclopaedia of Earth Sciences and in a number of international text books (e.g. Ramsay and Huber 1987, Suppe 1985). | |
| Interpretation: | |
The Kearney outcrops afford the opportunity to conduct a masterclass on the recognition and interpretation of the structural features characteristic of the low-grade metamorphic rocks of the Southern Uplands – Down - Longford Terrane. Many of these features have widespread occurrence in the paratectonic Caledonides of Britain and Ireland. | |
| Conclusions: | |
A well developed system of conjugate kink bands demonstrating an overall orthorhombic symmetry is extremely well displayed in the outcrop at the eastern end of Knockinelder Bay | |
| Notes: | |
The full range of ESCR site relating to the Lower Palaeozoic are as follows: Outer Ards Stratigraphic, Palaeontological and Structural sites Coalpit Bay – Lower Palaeozoic (record no. 1350) Helen’s Bay – Grey Point – Lower Palaeozoic (record no. 1351) Kearney Point – Knockinelder Bay – Lower Palaeozoic (record no. 1352) Orlock Bridge – Lower Palaeozoic (record no. 1353) Tieveshilly – Carrstown – Lower Palaeozoic (record no. 1354) Orlock Bridge - Structural (record no. 652) Whiskin Rocks - Structural (record no. 653) White House Port, Cloghy - Structural (record no. 654) Knockinelder Bay and Kearney Point - Structural (record no. 655) Millin Bay - Structural (record no. 656) Pomeroy area Craigbardahessiagh and Bardahessiagh River – Palaeontology (record no. 29) Lime Hill Farm – Palaeontology (record no. 33) Little River and Slate Quarry Bridge – Palaeontology (record no. 31) | |
| Keywords | |
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| Rocks: | Turbidite, Greywacke, Shale, Lamprophyre |
| Access | |
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| Approach: | Public access along National Trust coastal path from Kearney Village |
| Restrictions: | Public access |
| Management: | |
The inland part of the Key Site area around Kearney Village, Kearney Point and Knockinelder is used mainly as pasture for cattle. Kearney Village is a small hamlet of cottages owned by the National Trust. Geological interest is confined to a narrow coastal strip at and below High Water Mark. There are no buildings on or even close to this strip, save for three coastal cottages at Kearney Village. | |
| Threats: | As explained above, the outcrops of interest are entirely confined to a very narrow strip at High Water Mark. The strip extends along some 1.5 kilometres of low-lying rocky coast. This coastal strip is, I believe, entirely owned by the National Trust and so not threatened by any private development. Indeed I can imagine only one possible threat. There is a pleasant coastal path extending from the eastern end of the beach at Knockinelder Bay around Kearney Point to Kearney Village. For about 150 metres eastward from the end of the Bay the raised beach on which the path once rested has been eroded back to the fence which bounds the neighbouring fields. This erosion of the path has occurred during the last 40 years. It might reasonably be argued that this section of the path needs repair. Any repair should be conducted so as to avoid damage to the neighbouring rock outcrop. For example a concrete promenade would be both out of character and potentially damaging to the geological interest of the site. A sympathetic and careful repair presents no threat. Visiting geologists should ideally be warned about excessive use of geological hammers. There is little interest for geological collectors in any case (No fossils and no unusual minerals are known at the site). All the geology of interest can be sampled and collected using compass-clinometer, hand lens, camera and notebook. The one possible exception is that a petrologist with access to thin section and microscope might wish to sample the lamprophyre of the Kearney Sills. It is possible to collect a sample from any of the several sills exposed without doing any significant damage but the photogenic, and indeed historic, outcrop at Locality E should be avoided. |
| Record type: | ESCR report | ||
| Entered by: | I J Enlander | ||
| Last updated: | 1 April 2019 | ||
| Enlander, I., Dempster, M. & Doughty, P., 2026. Kearney Point – Knockinelder Bay – Lower Palaeozoic, County Down, site details. [In] Earth Science Conservation Review. https://www.habitas.org.uk/escr/site.php?item=1352. Accessed on 2026-11-06. |
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