2.a. Plate tectonic context

Prior to the late Ludlow, the Silurian palaeogeography of Wales and the Welsh Borderland was dominated by the Welsh Basin, an area of subsidence that was flanked to the south and east by the more stable Midland Platform and to the north by the Irish Sea Platform (or Monian Terrane). All were structural elements of a tectonic plate traditionally known as ‘Avalonia’, but which recent studies have shown to be more complex in its crustal composition and early history (e.g. Waldron et al. Reference Waldron, Schofield, Dufrane, Floyd, Crowley, Simonetti, Dokken and Pothier2014). By the close of the Ordovician, this assemblage of crustal fragments – part of the Anglo-Acadian Belt of Cocks & Fortey (Reference Cocks and Fortey1982), or Avalonian Terrane Assemblage of Verniers et al. (Reference Verniers, Pharaoh, Andre, Debacker, De Vos, Everaerts, Herbosch, Samuelsson, Sintubin, Vecoli, Winchester, Pharoah and Verniers2002) – had fused with the more easterly plate of Baltica to form a single, mid southern latitude, tectonic and faunal province.

The early Silurian closure of the Iapetus Ocean and the consequent collision between parts of Avalonia-Baltica and the northern supercontinent of Laurentia initiated the Scandian Orogeny in northern Europe. This event, viewed as a late stage of the protracted Caledonian orogenic cycle, strongly influenced Silurian deposition within the Welsh Basin and along its margins (e.g. Woodcock et al. Reference Woodcock, Butler, Davies, Waters, Hesselbo and Parkinson1996; Davies et al. Reference Davies, Waters, Molyneux, Williams, Zalasiewicz and Vandenbroucke2016). The Middle Devonian deformation of the basin’s marine Silurian fill, and of the Pridoli to Early Devonian red beds that succeeded it, has long been viewed as consequential to the terminal collision of Avalonia-Baltica with Laurentia and as the manifestation in the UK of the North American Acadian Orogeny (e.g. Soper et al. Reference Soper, Webb and Woodcock1987; Woodcock et al. Reference Woodcock, Awan, Johnson, Mackie and Smith1988). However, this Middle Devonian deformation is now believed to significantly postdate the closure of the Iapetus Ocean and thought more likely to mark events taking place within an evolving Variscan orogenic province to the south (e.g. Woodcock & Soper, Reference Woodcock, Soper, Brenchley and Rawson2006; Woodcock et al. Reference Woodcock, Soper and Strachan2007). Use of the term ‘Acadian Orogeny’ as a label for this event is also questioned (Woodcock, Reference Woodcock, Woodcock and Strachan2012a).

2.b. Pre-late Ludlow palaeogeography

The Welsh Basin provides a record of continuous deposition of predominantly deep marine facies from Early Ordovician until at least early Ludlow times (Figures 1 and 3a; e.g. Davies et al. Reference Davies, Fletcher, Waters, Wilson, Woodhall and Zalasiewicz1997; Cave & Hains, Reference Cave and Hains2001). In contrast, sediment accumulation on the Midland Platform during this interval was discontinuous both temporally and spatially (Bassett et al. Reference Bassett, Bluck, Cave, Holland, Lawson, Cope, Ingham and Rawson1992; Cramer, Reference Cramer1964; Woodcock et al. Reference Woodcock, Butler, Davies, Waters, Hesselbo and Parkinson1996). Palaeocurrent and provenance studies for early to mid-Silurian rocks in Wales confirm that different sectors of the platform were the dominant sources of sediment supplied to the basin during this period. The basin and platform were separated by the active, NE-striking, Welsh Borderland Fault System (WBFS; Woodcock & Gibbons, Reference Woodcock and Gibbons1988; Cherns et al. Reference Cherns, Cocks, Davies, Hillier, Waters, Williams, Brenchley and Rawson2006). Movements on intra-basinal faults were significant at various times during the basin’s evolution. The Midland Platform was also host to important fracture belts, including the Neath Disturbance and Malvern Lineament that influenced the deposition and preservation of Silurian sediments (e.g. Bassett et al. Reference Bassett, Bluck, Cave, Holland, Lawson, Cope, Ingham and Rawson1992; Butler et al. Reference Butler, Woodcock and Stewart1997).

Figure 3.

Palaeogeographic reconstructions of the study area. (a) Pre-late Ludlow. (b) Late Ludlow and earliest Pridoli. GGA, Golden Grove Axis; GA, Gorsley Axis; AF, Abercyfor Formation. (c) Early Pridoli hiatus and forced regression. CMSF-RF, Clifford’s Mesne Sandstone Formation – Rushall Formation; PMF, Pwll-Mawr Formation. (d) Mid-Pridoli incision and incised valley fill.

Late diagenetic illite crystallinity data for late Llandovery deep water facies in west Wales (Merriman, Reference Merriman2006; Woodcock, Reference Woodcock, Woodcock and Strachan2012a) implies that the western part of the Welsh Basin was subject to less overburden than areas further east adjacent to the WBFS. This region of the basin may have experienced limited inversion as early as the latest Llandovery, the focus of deep water facies deposition then shifting eastwards as the basin and its attendant fractures responded to the plate convergence (e.g. Davies et al. Reference Davies, Fletcher, Waters, Wilson, Woodhall and Zalasiewicz1997; Cave & Hains, Reference Cave and Hains2001; Smith, Reference Smith, Lomas and Joseph2004). Accompanying these physiographical changes, the dominant supply of detritus shifted from the east to that shed from tectonically uplifted Avalonian tracts that lay to the south and south-west, linked to the Midland Platform (e.g. Morton et al. Reference Morton, Davies and Waters1992; Ball et al. Reference Ball, Davies, Waters and Zalasiewicz1992). By the mid Wenlock, as plate collision abolished the Iapetus Ocean, links to the southern Rheic Ocean had likely already been established and the latter was the dominant marine influence during the Ludlow and Pridoli.

By early Ludlow (Gorstian) time, active deep-water deposition was confined to a narrow belt of subsidence previously labelled the Montgomery Trough, or as preferred here, the Clun Forest Sub-Basin (Figures 1 and 3a; Holland & Lawson, Reference Holland and Lawson1963). At this point, much of the former Welsh Basin had likely evolved into a region of shallow marine deposition or was emergent (Hillier et al. Reference Hillier, Marriott, Higgs and Howells2019). The facies that accumulated in and adjacent to the Clun Forest Sub-Basin across its eastern and southern margins and the contiguous Midland Platform describe the northward and westward progradation of shallower over deeper facies in a pattern that confirms that the supply of sediment during this period remained predominantly from the south and east (e.g. Siveter, Reference Siveter2000; Barclay et al. Reference Barclay, Davies, Humpage, Waters, Wilby, Williams and Wilson2005; Schofield et al. Reference Schofield, Davies, Waters, Wilby, Williams and Wilson2004, Reference Schofield, Davies, Jones, Leslie, Waters, Williams, Wilson, Venus and Hillier2009). However, Hillier et al. (Reference Hillier, Waters, Marriott and Davies2011) link the late Gorstian input of tectonically generated alluvial fans shed off local fault scarps to the earliest onset of terrestrial red bed conditions in SW Wales (e.g. Hillier & Williams, Reference Hillier and Williams2004; Barclay et al. Reference Barclay, Davies, Hillier and Waters2015). The first appearance within these red bed tracts of detritus sourced from the Caledonian Orogen (e.g. Sherlock et al. Reference Sherlock, Jones and Kelley2002; see Sections 2.c and 2.d below) shows that a fundamental reconfiguration of sediment supply routes and depocentres was ongoing during late Gorstian times. Wales, it appears, then lay within reach of the alluvium being shed from uplifting regions to the north. Hillier et al. (Reference Hillier, Marriott, Higgs and Howells2019) recognize Late Gorstian tectonism as a factor in the semi-regional inversion of the area to the north and west of the WBFS. This, they contended, promoted the formation of an extensive, low-gradient pediment plain cut by migrating, southwards flowing streams emerging from Caledonian uplands.

2.c. Late Ludlow (Ludfordian) and Pridoli palaeogeography

By the close of the Gorstian, the range of active marine deposition had contracted to an area occupied by the WBFS and adjacent parts of the Midland Platform, centred on a vestigial Clun Forest depocentre. The latter continued to receive sediment from a southerly sector, and it was within its confines that the thickest Ludfordian successions, including facies of deepest aspect, accumulated (Figure 3b). An early Ludfordian deepening event led to an expansion of marine conditions and the establishment of an extensive shallow-water, storm-influenced setting here recognized as the Cae’r mynach Seaway. In South Wales, the Golden Grove Axis acted as a structural hinge that separated this expanded region of marine deposition from the still extant pediment surface to west, and it seems likely that similar structural features perhaps linked to the Central Wales and Tywi lineaments also influenced the early location of this interface.

A focus of this study is the sedimentology of the separate delta progrades that subsequently advanced into the remnant marine tract from northerly and easterly quadrants as the input of sediment from the south declined and the supply of Caledonian detritus came to dominate. In SW Wales, thin deposits of locally derived debritic colluvium (Abercyfor Formation, AF) that overstep strata deformed during earlier Ashgill, Telychian and Late Gorstian structural events were the first to accumulate on the pediment surface (Hillier et al. Reference Hillier, Marriott, Higgs and Howells2019). The onset and expansion of ORS deposition records the spread of alluvial conditions that characterized the Pridoli and Lower Devonian succession of South Wales and the Welsh Borderland (Allen, Reference Allen1985; Bassett et al. Reference Bassett, Lawson and White1982; Bassett et al. Reference Bassett, Bluck, Cave, Holland, Lawson, Cope, Ingham and Rawson1992; Woodcock, Reference Woodcock, Woodcock and Strachan2012b). The thick, northerly derived red bed succession (e.g. Allen, Reference Allen and Owen1974a) records accommodation within the developing Anglo-Welsh Basin, which expanded to subsume the regions of the former pediment and marine seaway alike (Figures 1 and 3c; Hillier et al. Reference Hillier, Marriott, Higgs and Howells2019). This basin has been viewed as a Caledonian foreland basin formed in response to the collision between Avalonia and Laurentia and which migrated southwards to affect Wales during the Pridoli and Lower Devonian (e.g. King, Reference King1994). However, Woodcock et al. (Reference Woodcock, Soper and Strachan2007) suggest that the tectonic legacy of this collision was minimal in southern Britain. They link the accommodation and preservation of the Caledonian marine and non-marine succession in Wales to ongoing strike-slip displacement along the site of Iapetus suture zone and the development to the south of post-collision, transtensional basins. However, early Variscan tectonism, known to have been influential in Wales from as early as the Llandovery, continued to play a role by influencing links to the Rheic Ocean (see Section 6h) (Woodcock, Reference Woodcock, Woodcock and Strachan2012c).

This study builds on the findings of Hillier et al. (Reference Hillier, Marriott, Higgs and Howells2019) in recognizing separate episodes of basin-wide denudation and local incision of the ORS alluvial plain during the early and mid-Pridoli (Figures 3c–d). Regions of maximum erosion and incision were likely structurally controlled, with local faulting influential. In SW Wales, the valley fills preserve the deposits of streamflow conglomerates, alluvial fan and estuarine heterolithics of the Freshwater East Formation (FEF). This study provides details of the contemporaneous Pont ar Llechau Formation (PALF) valley fill succession, but also of a putative earlier Pridoli hiatus (Figures 1 and 3c–d).

2.d. Sediment composition and source

Ludfordian and early Pridoli delta progradation resulted in widespread micaceous sandstone deposition. This is recorded in the north and south-east of the study area as the Downton Castle Sandstone Formation (DCSF) and its local correlatives, and in the west as the Tilestones Formation (TilF). In studying the DCSF, Hobson (J.S.C. Hobson, unpub. PhD thesis, University of Birmingham, Hobson, Reference Hobson1960) recognized the influence of two discrete delta systems: a ‘Welsh Delta’ that Allen (Reference Allen1974b) confirmed advanced into the Ludlow and Clun areas from the north-east; and a ‘Woolhope Delta’ that supplied the coeval sandstones of the Woolhope, Malvern and May Hill inliers from the east. Our study supports these earlier findings for the DCSF of its type area, but by uncovering greater complexity including sandstone facies of differing age and setting suggests that the concept of a Woolhope Delta is misleading. Our data also fail to endorse previous suggestions that the sediment source for the TilF lay either to the west (Allen, Reference Allen1985) or south (e.g. Potter & Price, Reference Potter and Price1965; Owen, Reference Owen1967; Cope & Bassett, Reference Cope and Bassett1987; J. Almond, unpub. PhD thesis, University of Bristol, Almond, Reference Almond1983; Bassett et al. Reference Bassett, Bluck, Cave, Holland, Lawson, Cope, Ingham and Rawson1992). Behind these deltas, terrestrial ORS sediment accumulated, with coastal plain deposits of the Temeside Mudstone Formation (TemF) passing into terrestrial dryland deposits of the Moor Cliffs Formation (MCF; Hillier et al. Reference Hillier, Marriott, Higgs and Howells2019).

The abundance of large white mica flakes in Ludfordian and Pridoli sandstones in Wales and the Welsh Borderland testifies to the extensive unroofing of high-grade metamorphic rocks – probably mica schists – within sediment source areas. Outcrop location and size, and their detailed petrography, show that neither the Dutch Gin Schists of Pembrokeshire nor the Rushton Schists in Shropshire could have served as the principal source for this material (e.g. Baker et al. Reference Baker, Lemon, Gayer and Marshman1968; McIlroy & Horak, Reference McIlroy, Horak, Brenchley and Rawson2006), which must have lain further to the north. The schists and gneisses of the Mona Complex, forming part of a putative Irish Sea landmass, have been considered as a source for ‘Downtonian’ sandstones in the Welsh Borderlands that, in addition to quartz, mica and other heavy minerals, include abundant garnet (e.g. Heard & Davies, Reference Heard and Davies1924; Wallis, Reference Wallis1928; Walder, Reference Walder1941). Allen (Reference Allen1974b) rejected this possibility and anticipated Sherlock et al. (Reference Sherlock, Jones and Kelley2002) in suggesting that unroofed metamorphic tracts within the Caledonian Orogen were the more likely source for these mica- and garnet-rich mineral assemblages.

Hillier & Williams (Reference Hillier and Williams2004) suggest that the initial route via which this detritus was delivered to SW Wales, during the Gorstian, was a circuitous one that had to negotiate a still extant Welsh Basin to the north. However, the flood of mica supplied to Ludfordian–Pridoli sandbodies and the evidence provided by palaeocurrent vectors (Figure 3b) shows that the former basin had then ceased to exist as an intervening trap for sediment. This former site of deep marine sediment accumulation appears by this time to have formed part of a cryptic, but likely extensive Ludfordian land area (Hillier et al. Reference Hillier, Marriott, Higgs and Howells2019). Rivers that drained northerly source terrains were able to traverse this landscape as they delivered their mica-rich load to southerly facing Ludfordian shorelines in mid and south Wales. The long-distance terrestrial sediment transport models previously invoked for the ORS (e.g. Allen, Reference Allen1974b; Simon & Bluck, Reference Simon and Bluck1982; Allen & Crowley, Reference Allen and Crowley1983), it appears, were already well established by late Ludlow times.

However, local mineral and clast assemblages reported from the Ludfordian–Pridoli rocks of the region point to a more complex regional palaeogeography. J.S.C. Hobson, unpub. PhD thesis, University of Birmingham (Hobson, Reference Hobson1960) matched clasts in the DCSF of the Kington area to nearby Precambrian tracts. In the Silurian inliers in the south-east of the study area, the Precambrian rocks of the Midland Platform as seen in the Malvern Hills have been viewed as the likely source of local mineral assemblages rich in detrital biotite, zircon and rutile (Walmsley, Reference Walmsley1959; Tucker, Reference Tucker1960; J.S.C. Hobson, unpub, PhD thesis, University of Birmingham, Hobson, Reference Hobson1960; Phipps & Reeve, Reference Phipps and Reeve1967). Palaeocurrent data in this study support Hobson’s (J.S.C. Hobson, unpub. PhD thesis, University of Birmingham Hobson, Reference Hobson1960) assertion that some sediment in this region was supplied from the east. In the west, clast assemblages in the TilF and its contiguous facies, include plutonic igneous rocks, chlorite/muscovite schists and phyllitic and low-grade metamorphic lithologies (J. Almond, unpub. PhD thesis, University of Bristol, Almond, Reference Almond1983), which are consistent with the unroofing and reworking of conglomerate bodies present within the older basinal succession to the north (e.g. Davies et al. Reference Davies, Fletcher, Waters, Wilson, Woodhall and Zalasiewicz1997; Evans, Reference Evans1992; Schofield et al. Reference Schofield, Davies, Waters, Wilby, Williams and Wilson2004, Reference Schofield, Davies, Jones, Leslie, Waters, Williams, Wilson, Venus and Hillier2009; Wilby et al. Reference Wilby, Schofield, Wilson, Aspden, Burt, Davies, Hall, Jones and Venus2007). The abundance of angular acid volcanic clasts in other units implies that exposed volcanic units present within a now eroded early-mid Ordovician succession were also a source of debris (Hillier et al. Reference Hillier, Waters, Marriott and Davies2011). A picture emerges of locally active sources of sediment along the flanks of a Ludfordian–Pridoli depositional tract, possibly inselbergs that stood proud to the basal ORS pediment and its successor delta coastal plain, but with the latter principally in receipt of sediment delivered from distant orogenic uplands to the north.

3.a. Introduction

The regional and global forcing factors outlined above, linked to new and existing biostratigraphical findings, offer context for the sedimentological and palaeogeographical analysis presented herein. Figure 1 and Tables 1 and 2 summarize these findings and provide the architectural framework for the following account. Several key events emerge as influential in the development of the region’s Ludfordian to early Pridoli successions and serve to inform revisions to regional lithostratigraphical nomenclature. Figure 4 shows how many of the older terms relate to the new scheme. Much of the new nomenclature follows that applied by the British Geological Survey (BGS) during its mapping of parts of central and southern Wales (e.g. Schofield et al. Reference Schofield, Davies, Waters, Wilby, Williams and Wilson2004, Reference Schofield, Davies, Jones, Leslie, Waters, Williams, Wilson, Venus and Hillier2009; Barclay et al. Reference Barclay, Davies, Humpage, Waters, Wilby, Williams and Wilson2005) and also the recommendations of Barclay et al. (Reference Barclay, Davies, Hillier and Waters2015) in their review of ORS terminology. Some further comment is required. Changes to the established terminology for the type Ludlow succession permit unfettered use of chronostratigraphical nomenclature first used Cherns & Bassett (Reference Cherns, Bassett, Boucot and Lawson1999), but which has previously failed to gain widespread acceptance (Figure 5). In their seminal study of the Ludlow Series type area, Holland et al. (Reference Holland, Lawson and Walmsley1963) proposed four new chronostratigraphical stages, the Eltonian, Bringewoodian, Leintwardinian and Whitcliffian. The Subcommission on Silurian Stratigraphy (Holland, Reference Holland1980) concluded subsequently that the Ludlow should be divided into two internationally recognizable units and, in response, Holland et al. (Reference Holland, Lawson, Walmsley and White1980) proposed the stage terms that are in current use, the Gorstian and Ludfordian. However, Waters & Lawrence (Reference Waters and Lawrence1987) and Cherns & Bassett (Reference Cherns, Bassett, Boucot and Lawson1999) have since recognized that the four-fold divisions of Holland et al. (Reference Holland, Lawson and Walmsley1963) can be employed as regional sub-stages, or chronozones of the Gorstian and Ludfordian stages. Such usage is followed here. The definitions of each chronozone including their type sections are as detailed in Holland et al. (Reference Holland, Lawson and Walmsley1963). Lawson & White (Reference Lawson, White, Holland and Bassett1989) further document their benthic fossil content including critical faunal incomings and outgoings. The findings of subsequent studies, including work on miospores and acritarchs, are alluded to in the text. Figure 5 shows how these regional Ludlow chronozones relate to selected international and regional biozonal schemes. We follow Higgs (Reference Higgs2022) in his usage of informal chronostratigraphic subdivisions of the Pridoli.

Table 1.

Alphabetical key to lithostratigraphical symbols used in Figure 1, including primary sources of nomenclature, significant synonyms and comments on specific usage in this text. Symbols with numbered suffixes refer to parts a division that display different geographical and/or stratigraphical ranges (e.g. TemF1, TemF2). Other abbreviations: Lr, Lower; Up, Upper; Mudst, Mudstone

Table 2.

Explanation of numbered architectural elements and other notes in Figure 1

Figure 4.

Former stratigraphical nomenclature for the Ludlow and early Pridoli successions of the North-Eastern and South-Eastern provinces (inc. Long Mountain, Clun Forest and Ludlow areas and the eastern Silurian inliers) after the named authors, focusing on those units recognized herein as Cae’r mynach Formation (CarF). 1, Long Mountain Siltstone Formation of Palmer (Reference Palmer1970); 2, Causemountain Formation of Palmer (Reference Palmer1970); 3, Basal Lower, Lower and Upper Leintwardine beds of Whitaker (Reference Whitaker1962) and Lawson (Reference Lawson1973); 4, Leintwardinian facies included by the named authors in underlying, predominantly Bringewoodian divisions; 5, sense of Worssam et al. (Reference Worssam, Ellison and Moorlock1989); 6, units previously believed to correlate with the Downton Castle Sandstone Formation of the Ludlow area, but here interpreted as elements of a younger succession (see Figure 1); 7 units now recognized as Moor Cliffs Formation (Barclay et al. Reference Barclay, Davies, Hillier and Waters2015). Abbreviations: Bring., Bringewoodian; Gorst., Gorstian; EAM, Eastern Avenue Member; for other abbreviations, see Table 1.

Figure 5.

Chronostratigraphical subdivisions of the Ludlow and Pridoli highlighting late Silurian–Early Devonian Graptolite and spore zones of Wales and the Welsh Borderland with the ranges of key early Pridoli ostracod taxa. The spore zonation of NW Spain is shown to demonstrate the proposed correlation of the PALF with that of the Anglo-Welsh Basin. There are currently no formal subdivisions for the Pridoli Series, the usage here follows that of Higgs, Reference Higgs2022.

Note that the southerly sourced Ludlow facies of the Clun Forest Sub-Basin are not a focus of this study and are alluded to only briefly below. A more detailed lithostratigraphical summary of this succession is in preparation. Reference below to ‘BGS digital maps’ relates to maps that are publicly available via the BGS Map Portal and BGS Map Viewer.

The derivation and distribution of prograde sandstones allows three depositional provinces to be distinguished: a Western (or TilF) Province, a North-Eastern (or DCSF) Province and a South-Eastern Province, which includes the region of the Clifford’s Mesne Sandstone Formation (CMSF) deposition (Figure 1). In the latter province, local sandstone facies commonly contain biotite, but it was also a region of widespread erosion and sedimentary omission.

Shelly macrofossils, principally brachiopod and bivalves, have been studied extensively in the past and remain significant for dating of Ludfordian marine strata. Key Ludfordian and Pridoli ostracod species have also proved that significant and vertebrate remains are important in the terrestrial strata. However, spore assemblages have increasingly been relied upon and considerable palynological research has been undertaken in Wales and the Borderland (Anglo-Welsh Basin) to establish a spore zonation for the late Ludfordian to Pridoli interval (e.g. Richardson & Lister, Reference Richardson and Lister1969; Richardson & Edwards, Reference Richardson, Edwards, Holland and Bassett1989; Burgess & Richardson, Reference Burgess and Richardson1995; Edwards & Richardson, Reference Edwards and Richardson2004) (Figure 5). In addition, Higgs (Reference Higgs2022) has recently identified new Pridoli spore assemblages from Pembrokeshire that do not match the established zonation and reviewed the reasons for this. The only new biostratigraphical work undertaken as part of this study has been palynological, focusing on spores (Figure 6; Supplementary Figure 1), and to a lesser extent acritarchs and chitinozoans (Figure 7). Samples were studied from the Cae’r mynach Formation (CarF), TilF and PALF in the Western Province, and the Rushall Formation (RF) in the South-Eastern Province.

Figure 6.

Selected trilete spore taxa from the Tilestones Formation (a–j) and Pont ar Llechau Formation (k–y) identified in this study. (a). Retusotriletes cf. warringtoni Richardson & Lister, Reference Richardson and Lister1969. MPA 55422, slide 2A, F15/3, MPK 14781; (b). Retusotriletes charulatus McGregor & Narbonne, Reference McGregor and Narbonne1978. KH/CH4, G26; (c). Ambitisporites dilutus (Hoffmeister) Richardson & Lister, Reference Richardson and Lister1969. KH/CH2, S24; (d). Archaeozonotriletes chulus var. chulus Richardson & Lister, Reference Richardson and Lister1969. KH/CH3, T25; (e). Apiculiretusispora sp. C Richardson & Lister, Reference Richardson and Lister1969. KH/CH2, O19; (f). Scylaspora scripta Burgess & Richardson, Reference Burgess and Richardson1995. KH/CH4, K28; (g). Stellatispora inframurinata var. inframurinata Burgess & Richardson, Reference Burgess and Richardson1995. KH/CH2, P16; (h). Stellatispora inframurinata var. inframurinata Burgess & Richardson, Reference Burgess and Richardson1995. KH/CH2, U16; (i). Insolisporites sp. MPA 55422, slide 1A, J18/4, MPK 14782; (j). Chelinospora obscura Burgess & Richardson, Reference Burgess and Richardson1995. KH/CH2, O15. (k). Retusotriletes sp. A Burgess & Richardson, Reference Burgess and Richardson1995. MPA 55404, slide 2B, R11/0, MPK 14783; (l). Ambitisporites avitus Hoffmeister, Reference Hoffmeister1959. MPA 55406, slide 1A, G35/4, MPK 14784; (m). Archaeozonotriletes chulus var. chulus Richardson & Lister, Reference Richardson and Lister1969. MPA 55406, slide 1A, Q11/0, MPK 14785; (n). Apiculiretusispora spicula Richardson & Lister, Reference Richardson and Lister1969. MPA 55403, slide 1B, N21/2, MPK 14786; (o). Apiculiretusispora sp. C. Richardson & Lister, Reference Richardson and Lister1969. MPA 55406, slide 1A, M33/3, MPK 14787; (p). Apiculiretusispora synorea Richardson & Lister, Reference Richardson and Lister1969. MPA 55406, slide 1A, J20/2, MPK 14788; (q). Concentricosiporites sagittarius (Rodriguez) Rodriguez, 1983. MPA 55404, slide 2B, P19/3, MPK 14789; (r). Synorisporites verrucatus Richardson & Lister, Reference Richardson and Lister1969. MPA 55404, slide 2B, E12/0, MPK 14790; (s). Synorisporites verrucatus Richardson & Lister, Reference Richardson and Lister1969. MPA 55404, slide 2B, N14/2, MPK 14791; (t). Stellatispora inframurinata var. inframurinata Burgess & Richardson, Reference Burgess and Richardson1995. MPA 55404, slide 1B, X21/0, MPK 14792; (u). Chelinospora cf. hemiesferica (Cramer & Diez) Richardson, Rodriguez & Sutherland, Reference Richardson, Rodriguez and Sutherland2001. PAL3C, R13; (v). Chelinospora cf. lavidensis Richardson, Rodriguez & Sutherland, Reference Richardson, Rodriguez and Sutherland2001. PAL3C, F30; (w). Chelinospora cantabrica Richardson, Rodriguez & Sutherland, Reference Richardson, Rodriguez and Sutherland2001. PAL3C, V24; (x). Scylaspora cf. elegans Richardson et al. Reference Richardson, Rodriguez and Sutherland2001. MPA 55403, slide 2A, R10/0, MPK 14793; (y). Breconisporites sp. MPA 55403, slide 2A, X8/1, MPK 14794.

Figure 7.

Late Silurian acritarchs (a–d, h, j–m), prasinophytes (e–g, i) and chitinozoans (n–p) identified during this study. Scale bar in (f) = 10 µm for (a–m); scale bar in (o) = 25 µm for (n, o); scale bar in (p) = 10 µm. (a) Comasphaeridium brevispinosum (Lister, Reference Lister1970) Mullins, 2001, Cae’r mynach Fm. (CarF1), Sawdde Gorge, MPA 55414, slide 1, M4/2, MPK 14795; (b) Comasphaeridium brevispinosum, Cae’r mynach Fm. (CarF1), Sawdde Gorge, MPA 55414, slide 1, P3/0, MPK 14796; (c) Comasphaeridium brevispinosum, Cae’r mynach Fm. (CarF1), Sawdde Gorge, MPA 55414, slide 1, U30/1-2, MPK 14797; (d) Sol radians Cramer, 1964, Cae’r mynach Fm. (CarF1), Cennen Road, MPA 55415, slide 1, P21/2, MPK 14798; (e) Cymatiosphaera sp. A? of Richards & Mullins, Reference Richards and Mullins2003, Cae’r mynach Fm. (CarF1), Cennen Road, MPA 55415, slide2, M8/1, MPK 14799; (f) Cymatiosphaera sp. A?, Cae’r mynach Fm. (CarF1), Sawdde Gorge, MPA 55411, slide 2, F18/4, MPK 14800; (g) Cymatiosphaera sp. A?, Cae’r mynach Fm. (CarF1), Sawdde Gorge, MPA 55411, slide 2, M24/4, MPK 14801; (h) Percultisphaera stiphrospinata Lister, Reference Lister1970, Cae’r mynach Fm. (CarF1), Sawdde Gorge, MPA 55412, slide 1, F8/3-4, MPK 14802; (i) Pterospermella foveolata Lister ex Dorning, Reference Dorning1981, Cae’r mynach Fm. (CarF1), Cennen Road, MPA 55415, slide 1, U6/0-2, MPK 14803; (j) Rhacobrachion mala (Cramer, 1964) Dorning, Reference Dorning1981, Cae’r mynach Fm. (CarF1), Sawdde Gorge, MPA 55411, slide 1, X30/3, MPK 14804; (k) Rhacobrachion mala, Tilestones Fm. (TilF3), Capel Horeb Quarry, MPA 55422, slide 2A, Q18/2, MPK 14805; (l) Leoniella carminae Cramer, 1964, Cae’r mynach Fm. (CarF1), Sawdde Gorge, MPA 55414, slide 1, L12/0-3, MPK 14806; (m) Leoniella vilis Kiryanov, Reference Kiryanov1978, Cae’r mynach Fm. (CarF1), Sawdde Gorge, MPA 55412, slide 2, R10/3, MPK 14807; (n) Angochitina elongata? Eisenack, Reference Eisenack1931, Tilestones Fm. (TilF3), Capel Horeb Quarry, MPA 55422, slide 2A, D17/3, MPK 14808; (o) Eisenackitina lagenomorpha? (Eisenack, 1931), Tilestones Fm. (TilF3), Capel Horeb Quarry, MPA 55422, slide 2B, M24/0-1, MPK 14809; (p) Eisenackitina lagenomorpha?, Cae’r mynach Fm. (CarF1), Sawdde Gorge, MPA 55412, slide 1, F16/4, MPK 14810.

Since the erection of the Pridoli Series, the LBB and its correlatives (see Section 3.c below) have been taken to mark the base of the series in Wales and the Welsh Borderland (White & Lawson, Reference White, Lawson, Holland and Bassett1989). Many of the microfloral taxa present in the ‘bone bed’ and in the succeeding strata have not been recovered from the underlying succession and are recognized as Pridoli markers. However, Loydell and Frýda (Reference Loydell and Frýda2011) interpret the isotope excursion they discovered spanning the LBB and extending into the overlying stratigraphy (see Figure 1), as the global Lau Event. This, if confirmed, would demonstrate a late Ludfordian age for these strata and, by default, their fossil assemblages. Turner et al. (Reference Turner, Burrow, Williams and Tarrant2017) have sought robustly to defend the status quo. It is not the place for this study to arbitrate and the assumption of an early Pridoli age continues, with caution, to be applied herein.

3.b. Early Leintwardinian flooding event

The dating and impact of this flooding episode are well established throughout the study area. East of the WBFS, both in the type Ludlow succession and more widely, the onset of calcareous siltstone deposition above limestone-rich facies typical of the Bringewoodian is widely acknowledged to record a transgressive deepening (Cherns et al. Reference Cherns, Cocks, Davies, Hillier, Waters, Williams, Brenchley and Rawson2006; Cherns, Reference Cherns and Ray2011). These transgressive facies commonly yield leintwardinensis Biozone graptolites, but such faunas are known locally to appear first in facies that form part of preceding, principally Bringewoodian, lithostratigraphical divisions. Aymestry Limestone facies of Leintwardinan age occur at the Ludfordian stratotype in Sunnyhill Quarry (Cherns, Reference Cherns1988; Lawson & White, Reference Lawson, White, Holland and Bassett1989) and in the Malverns (Phipps & Reeve, Reference Phipps and Reeve1967; Barclay et al. Reference Barclay, Ambrose, Chadwick and Pharaoh1997). Waters & Lawrence (Reference Waters and Lawrence1987) recognized the earliest Leintwardinian faunas in the otherwise Bringewoodian Eastern Avenue Member in the Rumney inlier. Where developed, these earliest Leintwardinian levels underlie gradational contacts with the succeeding transgressive strata. However, in the Church Stretton area and in the successions of the southern Malverns and the Woolhope and May Hill inliers, where the contact between Bringewoodian and Leintwardinian facies is sharp, there is evidence of widespread omission and erosion. Beds of conglomerate that comprise bored clasts of limestone are abundant in the basal few metres of the Leintwardinian succession. Bringewoodian limestones were the source of the clasts in some of these units, but others may testify to the destruction of contemporary hardgrounds and show that there were sites of condensed deposition during the earliest phase of Leintwardinian deepening (Cherns, Reference Cherns1988; Watkins, Reference Watkins1979). Siliciclastic pebbles overlie the erosive base of the Usk Inlier Ludfordian succession. The non-sequence in the Gorsley Inlier, where Ludfordian rocks overlie a contact with Wenlock limestones that displays evidence of karstic dissolution, emphasizes the active role played by the Gorsley Axis.

West of Ludlow, in the Leintwardine and Wigmore areas, graptolite-bearing, early Ludfordian rocks are associated with features linked to the cut and fill of contemporary submarine canyons and associated slump scars formed along the margin of the Clun Forest Sub-Basin (Whitaker, Reference Whitaker1962, Reference Whitaker1994; BGS, 2000). In the deeper water sub-basinal successions to the west, evidence of Leintwardinian deepening is recorded by the graptolitic Cwm-yr-hob Member (Cave & Hains, Reference Cave and Hains2001). In the Western Province, in the Cwm Craig-Ddu area, the lowest levels to yield Saetograptus leintwardinensis leintwardinensis evidence a more muted lithological response (Williams, Reference Williams2003). Further south, the mud-prone Fibua Formation (Schofield et al. Reference Schofield, Davies, Waters, Wilby, Williams and Wilson2004) marks the onset of an abrupt deepening. The age of its basal graptolite fauna at Fibua Quarry (SN 8913 3932), consisting solely of subspecies of Bohemograptus bohemicus, has been reassessed. It is no longer seen as indicative of the Bohemograptus proliferation interval, as suggested by Schofield et al. (Reference Schofield, Davies, Waters, Wilby, Williams and Wilson2004), but to demonstrate a pre-leintwardinensis Biozone age (James Wilkinson pers.comm., 2019). It follows that the current BGS mapping of the Mynydd Epynt region (see Schofield et al. Reference Schofield, Davies, Waters, Wilby, Williams and Wilson2004; Barclay et al. Reference Barclay, Davies, Humpage, Waters, Wilby, Williams and Wilson2005; BGS, 2005a,b) is in error. These findings, in concurring with the report by Whitaker (Reference Whitaker1962) of B. bohemicus from the basal ‘Lower Leintwardine Beds’ in the Downton Gorge, imply that, though principally a Leintwardinian episode, the transgression had its origins late in the Gorstian incipiens graptolite Biozone.

In the Sawdde area, it is the erosive contact between Trichrug Formation red beds and the conglomerates at the base of the marine CarF that records the Leintwardinian transgression (e.g. Siveter et al. Reference Siveter, Owens and Thomas1989; Schofield et al. Reference Schofield, Davies, Jones, Leslie, Waters, Williams, Wilson, Venus and Hillier2009). This is supported by acritarchs, chitinozoans and macrofauna from the overlying succession (see Section 3.e.2). Faunas recovered from the Cennen Road section confirm that marine conditions had also extended on to the eastern flank of the Golden Grove Axis during the Leintwardinian (see Section 3.e.2). In more westerly sections, between Llandeilo and Carmarthen, the period of piedmont erosion that preceded this marine advance is recorded as an unconformity, increasing in magnitude westwards. However, this is a compound feature. It intervenes between Ludfordian terrestrial deposits and rocks that range from Wenlock to Neoproterozoic in age but conflates the impacts of multiple erosional episodes.

3.c. Ludlow Bone Bed flooding event

The abrupt changes in macro- and microfossil assemblages that take place across the LBB explain why it has gained such stratigraphical importance. Yet opinions have varied about the nature of the event it marks. In its type area, the LBB sensu stricto (Antia, Reference Antia1980; Bassett et al. Reference Bassett, Lawson and White1982) is the lowest of several bone-bearing levels present within an up to 0.3 m thick interval recognized by Bassett et al. (Reference Bassett, Lawson and White1982) as the Ludlow Bone Bed Member (LBBM). Gastropods, bivalves, ostracods, eurypterids, fish and plant remains are the dominant fossil components in and above this unit (e.g. Murchison, Reference Murchison1839; Elles & Slater, Reference Elles and Slater1906; Bassett et al. Reference Bassett, Lawson and White1982; Siveter et al. Reference Siveter, Owens and Thomas1989; White & Lawson, Reference White, Lawson, Holland and Bassett1989; Miller, Reference Miller1995; Lane, Reference Lane, Aldridge, Siveter, Siveter, Lane, Palmer and Woodcock2000).

Early models saw this assemblage as offering evidence of an abrupt shoaling and associated changes in salinity. Richardson & Rasul (Reference Richardson and Rasul1990) sought to explain the pronounced changes to palynological assemblages that occur at the base of the LBBM as evidence for such an event. However, the select assemblage of articulated brachiopods hosted by the LBBM (e.g. Bassett et al. Reference Bassett, Lawson and White1982) supports a majority of studies that recognize the bone beds as reworked lags formed in a storm-stirred setting that, if not fully marine, faced the open sea (see Section 6.c) and, further, that see the LBB itself as marking the onset of a period of rising sea level and reduced sediment supply (e.g. Allen & Tarlo, Reference Allen and Tarlo1963; Antia, Reference Antia1979, Reference Antia1980; Allen, Reference Allen1985; Smith & Ainsworth, Reference Smith and Ainsworth1989; Ainsworth, Reference Ainsworth1991; Veevers & Thomas, Reference Veevers, Thomas and Ray2011). Recently, Hauser & Gold (Reference Hauser and Gold2023) have sought to emphasize the role played by autogenic sedimentary processes during the accumulation of the LBBM and the succeeding early Pridoli succession. Such processes are acknowledged likely to have been influential during Ludfordian episodes of delta advance, but the current study confirms that marine base-level changes of regional, if not global reach were significant during the early Pridoli.

Bone-bearing levels that have been correlated with the LBBM have been taken to testify to the impact of this deepening episode in many areas of the North-Eastern and South-Eastern provinces (Allen, Reference Allen1974b; Bassett et al. Reference Bassett, Lawson and White1982). The findings reported herein call some of these correlations into question. The relevant phosphate and bone-bearing levels seen in the Woolhope, Gorsley and May Hill inliers, and that underlie the RF and CMSF, are believed to be significantly younger (see Sections 3.d, i and j). The current study allows for transgressive bone beds preserved in the Malverns, Usk and Rumney successions (e.g. Phipps & Reeve, Reference Phipps and Reeve1967; Squirrell & Downing, Reference Squirrell and Downing1969; Waters & Lawrence, Reference Waters and Lawrence1987) still to be viewed as correlatives of the LBB. Objective proof for this and of the early Pridoli age of the overlying restricted marine succession is lacking. Bone beds seen in the Tites Point and Brookend Borehole sucessions (Cave & White, Reference Cave and White1971) on the south side of the Bristol Channel have also been cited as equivalent to the LBB, but, being located to the south of the Severn Estuary Fault Zone (Wilson et al. Reference Wilson, Davies, Smith and Waters1988), are considered palinspastically displaced.

Where the LBBM is absent, it is faunal or lithological changes believed to mark the onset of the associated deepening episode that have been widely adopted as the proxy base of the Pridoli Series (Cocks et al. Reference Cocks, Holland and Rickards1992). In the Clun Forest area, the series boundary is taken at the base of the ‘Platyschisma Beds’ of Earp (Reference Earp1938; see Cave & Hains, Reference Cave and Hains2001) and in the Western Province at the base of the TilF (Schofield et al. Reference Schofield, Davies, Jones, Leslie, Waters, Williams, Wilson, Venus and Hillier2009). However, in the absence of graptolites from late Ludlow and Pridoli rocks in the UK (Zalasiewicz et al. Reference Zalasiewicz, Taylor, Rushton, Loydell, Rickards and Williams2009), such correlations have relied on fossil evidence that the current study finds deficient.

3.d. Early Pridoli Hiatus

A significant finding of the current study is a widespread intra-early Pridoli erosional event believed to record the impact of a forced regression (Figures 1 and 3c). Sites that display the evidence for this event, including channelling and calcretization affecting the top of the TilF and DCSF, are listed in Section 6. In the South Eastern Province, it is manifested by an erosion surface overlain by bone beds in the Woolhope, Gorsley and May Hill inliers. Accordingly, these levels are no longer correlated with the LBBM (see Sections 3i and j). The erosion surface at the base of the ORS in the Rumney Borehole (Waters & Lawrence, Reference Waters and Lawrence1987) is also interpreted as the early Pridoli Hiatus. However, the bone bed that lies 7 cm below the hiatus is still considered to be a correlative of the LBBM. Only the Usk Inlier succession fails to preserve obvious impacts of the early Pridoli Hiatus. The recognition of the Hiatus is reflected in the stratigraphical labelling used for units that pre- and postdate its impacts, the rocks that overlie it here considered to be mid-early Pridoli in age.

3.e. Cae’r mynach Formation (CarF)

3.f. Tilestones Formation (TilF)

3.g. Downton Castle Sandstone Formation (DCSF)

The term Downton Castle Sandstone was first proposed by Elles & Slater (Reference Elles and Slater1906) for the prominent sandstone unit well exposed in the Downton Gorge. Its recognition as the basal division of the former Downtonian (e.g. Allen, Reference Allen and Owen1974a) underpinned the useage proposed by Bassett et al. (Reference Bassett, Lawson and White1982) and its subsequent assignment to the Pridoli Series (e.g. White & Lawson, Reference White, Lawson, Holland and Bassett1989). As noted above, divisions previously included as members in the DCSF by Bassett et al. (Reference Bassett, Lawson and White1982) are here excluded from it (Figure 4). The base is now defined as the appearance of sandstone bed amalgamation in the sandstone prone sequence. Though the high-energy sandstones of the DCSF are largely unsuited for the preservation of spores and ostracods, F. groenvalliana has been found in the basal 0.75 m (David Siveter pers. comm.) and the formation is believed to fall entirely within the range of this taxon (Siveter, Reference Siveter, Holland and Bassett1989).

The labelling of strata as DCSF on BGS digital maps of the Woolhope, Mayhill and Usk areas is incorrect. Some of these units are not sandstone-dominated and their stratigraphical relationships do not compare. Herein, the DCSF is recognized as an early Pridoli deltaic sand body that, with the arguable exception of the Malverns area, is preserved princiapally to the north of the Neath Disturbance.

Deltaic sandstones present in the Knighton, Clun Forest and Long Mountain areas are recorded in the literature as ‘Yellow Downtonian’ (Holland, Reference Holland1959; Palmer, Reference Palmer1970). Cave & Hains (Reference Cave and Hains2001) included these strata in their early Pridoli Clun Forest Formation but did not recognize or map a major sandstone unit. Investigations as part of the current study have confirmed that the DCSF is present (e.g. Stonehouse Dingle) but in many localities is cut out by faulting. The sandstone units display sedimentological differences from those in the Ludlow area (see below), but the current study confirms that they were deposited by the same north-easterly sourced delta system (Figures 1 and 3b). The LBB is not recognized in these westerly successions, but the interval underlying the sandstones that contains the same brackish water fossil assemblage as the Platyschisma Shales Member has been taken as evidence for an early Pridoli age (e.g. Cave & Hains, Reference Cave and Hains2001).

Strata worked for tiles in the Long Mountain area and mapped by BGS as TilF (BGS, 2008b; Cave, Reference Cave2008) are also better viewed as a local representative of the DCSF. A local equivalent of the LBBM has been recognized in the underlying succession (Palmer, Reference Palmer1970). From overlying levels seen as equivalent to the ‘Platyschisma Shales’, Miller (Reference Miller1995) recovered what he considered to be early Pridoli microfossil assemblages.

In the Malverns area, heterolithic facies included in the CarF, for example at Brockhill Quarry (S.J. Veevers, unpub. PhD thesis, University of Birmingham, Veevers, Reference Veevers2006), Woodbury Quarry and Woodfield Farm (White et al. Reference White, Ellison and Moorlock1984), intervene between a local bone bed and a sandstone unit for which the label DCSF may continue to be appropriate. Penn (Reference Penn1987) suggests that the DCSF was encountered in the Maesteg No. 1 Borehole (SS 8528 9245), but gamma ray and acoustic log responses across the interval are similar to those for calcareous sandstones in the overlying MCF.

3.h. Temeside Mudstone Formation (TemF) and Moor Cliffs Formation (MCF)

3.i. Clifford’s Mesne Sandstone Formation (CMSF), Rushall Formation (RF) and Pwll-Mawr Formation (PMF)

The CMSF (Lawson, Reference Lawson1954; Reference Lawson1955) is present in the Gorsley and May Hill inliers. At Gorsley and around Clifford’s Mesne, the formation comprises up to 24 m of thick-bedded, pale orange, fine- to medium-grained sandstones, quite unlike the DCSF of the Ludlow area. In the May Hill Inlier south of the NW-SE trending Glasshouse Fault, it comprises a finer-grained succession of massive siltstones and silty sandstones (Lawson, Reference Lawson1955, see also Gardiner, Reference Gardiner1920; Lawson, Reference Lawson, Lawson, Curtis, Squirrell, Tucker and Walmsley1982). As described above, the CMSF overlies a succession of silty shales with a restricted marine fauna, referred here to CarF 3. These shales, seen at Linton Quarry in the north and Longhope Quarry in the south, contain faunas and spores that confirm an intra-Pridoli age for the CMSF.

Secondary reddening offers a plausible alternative explanation for red mudstones interbedded within the upper parts of the CMSF in the M50 road cutting that might otherwise be taken to suggest a gradational passage into the succeeding MCF (Allen & Dineley, Reference Allen and Dineley1976).

The RF was first recognized by Squirrell & Tucker (Reference Squirrell and Tucker1960) in the Woolhope Inlier and extends to the north in a faulted inlier at Shucknall Hill (Figure 1). It comprises up to 27 m of coarse- to fine-grained sandstones and olive grey and green mudstones and siltstones. The coarser and finer lithologies are present in roughly equal measure and exhibit rapid lateral and vertical changes in facies (Brandon, Reference Brandon1989). Articulated brachiopods, likely reworked, are confined to the basal few centimetres of the formation. The presence of inarticulated brachiopods and abundant eurypterid and fish remains supports sedimentological evidence for deposition in a shallow and restricted, brackish water setting; locally preserved green beds with calcrete nodules testify to periods of emergence (see Section 4.b.8).

The prominent erosion surface at the base of the RF marks the early Pridoli Hiatus. It is widely overlain by a 2.5 to 30 cm thick bone-bearing unit. The latter comprises a dark grey, locally conglomeratic, carbonaceous sandstone bed with fish bones, scales and phosphate pebbles and locally contains boulders eroded from the underlying CarF (Stamp, Reference Stamp1923; Gardiner, Reference Gardiner1927). This bone bed’s sparse fauna is dominated by comminuted eurypterid remains, together with plant fragments and carbonized algae. Inarticulate brachiopods and stratigraphically important ostracods have also been recovered. CarF facies that underlie the erosion surface exhibit no evidence of pedogenic alteration.

Squirrell & Tucker (Reference Squirrell and Tucker1960) correlated the bone-bearing level with the ULPB of the Gorsley and May Hill successions and followed Lawson (Reference Lawson1955) in interpreting them as LBB correlatives. They found the RF difficult to match with either the DCSF or TemF of the Ludlow area due to its heterolithic character. They correlated it with CMSF of the Gorsley and May Hill areas, but mistakenly considered it also to be the latteral equivalent of the Speckled Grit of the Usk area and the DCSF of the Malverns. These are all areas where the TemF is absent.

Confirmation of an early Pridoli age for the RF is provided by the presence of ostracods, including F. groenvalliana, from exposures of the basal beds in Perton Lane (Brandon, Reference Brandon1989; Miller, Reference Miller1995). Spores from the same locality are of the TS Assemblage Biozone (Fanning et al. Reference Fanning, Richardson, Edwards, Blackmore and Barnes1991; Edwards & Richardson, Reference Edwards and Richardson2004), and this is confirmed by a sample (Pert 1) taken from 0.55 m above the base of the formation at this locality. This sample yielded the following spore taxa, Synorisporites tripapillatus, S. verrucatus, Cymbosporites echinatus, Archaeozonotrilletes chulus var. chulus, Apiculiretusispora spicula and A. synorea. In the Rumney Borehole, the basal 13 m of strata previously included in the Raglan Mudstone Formation (Waters & Lawrence, Reference Waters and Lawrence1987) are here recognized as the newly named PMF. Its basal erosion surface marks the early Pridoli event. The formation is dominated by a heterolith of dark purple and reddish-purple mudstones with laminae and thin beds of siltstone and fine sandstone. Bioturbation is locally present as are lingulids, some preserved in life position. A single calcrete profile is associated with a unit of massive red mudstone. Spore assemblages recovered by Burgess & Richardson (Reference Burgess and Richardson1995) from a 0.8 m thick unit of grey-green laminated mudstone with plant debris, present just below the top of the formation in the Rumney Borehole, are of the TS Assemblage Biozone.

In the Usk Inlier, a thin interval of mottled red and green mudstones intervenes between the local CarF succession and fully terrestrial MCF facies. These mark an extension of the PMF into the Usk region, but there they form part of a succession lacking evidence for the early Pridoli Hiatus (see Section 6.d.3).

3.j. A new model for the correlation of early Pridoli rocks in the Welsh Borderland

Underpinning established early Pridoli correlations has been the assumption that the basal bone-bearing beds that underlie both the RF and CMSF equate with the LBB and, consequently, that both formations correlate with the overlying Ludlow area succession (e.g. Lawson, Reference Lawson1954, Reference Lawson1955; Squirrell & Tucker, Reference Squirrell and Tucker1960; Brandon, Reference Brandon1989; Bassett et al. Reference Bassett, Bluck, Cave, Holland, Lawson, Cope, Ingham and Rawson1992). The Speckled Grit (Walmsley, Reference Walmsley1959) of the Usk area has also been seen as a correlative of the DCSF and is shown as such on BGS paper and digital maps. However, there are sedimentological and palaeogeographical reasons to question these long-held assertions and a rigorous reassessment of the biostratigraphical evidence permit alternative correlations of early Pridoli rock units.

The first option is to accept the long-standing correlation with the Ludlow area succession. In this scenario, the bone and locally boulder strewn erosion surface at the base of the RF and CMSF relates to the shoaling episode marked by TilF 3 and the Aston Munslow Member and was cut prior to the main early Pridoli phase of delta progradation. The RF might then be regarded as having formed in a back-barrier, estuarine or lagoonal setting landward of the contemporary delta. However, the basal erosion surface evidently testifies to a significant base-level event. Carbonate-rich facies are known to undergo rapid lithification. Nevertheless, boulder-grade clasts derived from the underlying succession imply a level of induration consistent with a period of burial and their excavation testimony to significant incision. Evidence that the earlier shoaling episode culminated in comparable levels of erosion elsewhere along the margins of the Cae’r mynach Seaway is lacking. It then becomes difficult to envisage how this level of incision could have been generated in a setting located alongside a passively prograding deltaic shoreline. Nor is it obvious where this shoreline was located. The subsequent DCSF delta advance was from the north-east, yet the crop of the brackish RF lies well to the south of the Ludlow area of progradation and to the west of the DCSF of the Malverns. The RF occupies a region that palaeogeographical reconstructions might reasonably envisage to be on the seaward side of these deltaic coastlines.

The southwards failure of the TemF is also difficult to account for. A lateral passage from green, seawards facing coastal plain facies into a region of MCF red bed accumulation located to the south again lacks palaeogeographical credibity. Unconformity has been invoked to explain this anomaly, yet where seen, the contact between the TemF and MCF is gradational.

Seeking to resolve these palaeogeographical difficulties obliges us to question the long-held assumption that faunas recovered from and above the Woolhope, Gorsley and May Hill bone beds offer unambiguous evidence of a correlation with the LBB. They do not. The ranges of the key miospore and ostracod taxa clearly permit a second option. The lowest levels of the RF, CarF 3 and likely the whole of the PMF in the Rumney Borehole are all of TS Assemblage Biozone age. The unknown position of the base of Biozone A in the Ludlow area allows for the lower parts of TemF 2 and the CMSF to be of TS Assemblage Biozone age as well. All these levels fall within the range of F. groenvalliana, and it is feasible to view them all as lateral correlatives (Figure 1).

Such a model accounts for the significant differences in composition and sedimentary context between the Woolhope, Gorsley and May Hill bone beds and the LBB. In this model, the early Pridoli Hiatus is viewed as testimony to a widely felt forced regression that resulted in the emergence, incision and pedogenesis of regions north of the Neath Disturbance, during the TS Assemblage Biozone. In contrast, the response to this event further south was marine ravinement. This promoted the widespread removal of earlier deposits, including levels equivalent to the LBB and then the accumulation of winnowed bone-rich lags on the erosion surface. The correlations implied by this interpretation, as depicted in Figure 1, allow TemF 2, RF and CMSF to be viewed as a palinspastically sensible succession of coastal plain, back-barrier and barrier deposits, and as evidence for a post-hiatus, mid-early Pridoli episode of delta progradation. A fuller explanation of this model, which envisages CarF 3 and PMF as the coeval deposits of a remnant southerly seaway and its westerly coastline, is given in Sections 6.d.2 and 6.d.3.

Finally, it is interesting to note that Allen & Dineley (Reference Allen and Dineley1976) also suggested that the CMSF and RF are younger than the DCSF and overlie a substantial break. Their evidence was based on the absence of an overlying TemF and the presence of the mid-Pridoli ostracod Kloedenia wilckensiana in the basal CMSF and RF (Lawson, 1956; Squirrell & Tucker, Reference Squirrell and Tucker1960). Their suggestion never gained traction, however, probably as K. wilckensiana in the RF was later shown to be misidentified and to be the earlier F. groenvalliana (Brandon, Reference Brandon1989). The CMSF records are almost certainly similar misidentifications (David Siveter personal communication).

3.k. Mid-Pridoli Hiatus and Pont ar Llechau Formation (PALF)

The PALF (Almond et al. Reference Almond, Williams, Woodcock, Woodcock and Bassett1993; Barclay et al. Reference Barclay, Davies, Hillier and Waters2015) is limited to the Western Province and confined to a narrow tract between just east of the Cennen Valley and just east of Rhyblid (Figures 1, 2 and 3d). Its usage here differs from the Pont ar Llechau Member of Almond et al. (Reference Almond, Williams, Woodcock, Woodcock and Bassett1993). The formation mainly comprises up to 43 m of red brown, bioturbated, gritty argillaceous sandstones with scattered units of sandstones and green mudstones heterolith. A restricted marine fauna is present throughout the bulk of the formation, but units of interbedded sandstones with subordinate green mudstones contain a more diverse fauna.

Based solely on its stratigraphical position, the formation was interpreted by Almond et al. (Reference Almond, Williams, Woodcock, Woodcock and Bassett1993) to be exclusively Pridoli in age. BGS (2008a; see also Barclay et al. Reference Barclay, Davies, Hillier and Waters2015) viewed it as ranging from late Ludfordian into the early Pridoli. Five palynology samples (Figure 6) from three units of grey-green heterolith in the Sawdde Gorge have yielded spores that underpin a radical reappraisal of the formation’s age and setting. The assemblages contain many of the spore taxa recorded in the TilF at Capel Horeb but include additional stratigraphically important taxa. These include Apiculiretusispora spicula, A. synorea, A. sp. C, Chelinospora cantabrica, Chelinospra cf. hemiesferica, Chelinospora cf. cassicula, Chelinospora cf. lavidensis and Scylaspora cf. elegans.

In terms of Richardson & Edwards’ (Reference Richardson, Edwards, Holland and Bassett1989) Anglo-Welsh spore biozonaton, these assemblages would be placed within the TS Assemblage Biozone. However, the presence of several Chelinospora taxa (particulary Chelinospora cf. lavidensis) and Scylaspora cf. elegans is regarded as stratigraphically significant. The Chelinospora lavidensis assemblage has recently been described from the FEF in south Pembrokeshire (Hillier et al. Reference Hillier, Marriott, Higgs and Howells2019; Higgs, Reference Higgs2022), where it was assigned an early mid-Pridoli age based on a palynological correlation with the San Pedro Formation in north-west Spain. In that region, Richardson et al. (Reference Richardson, Rodriguez and Sutherland2001) established a Ludfordian–Pridoli spore biozonation for the Spanish succession in which Chelinospora lavidensis characterized the upper part of the Chelinospora hemiesferica H Biozone of early mid-Pridoli age. However, the rare occurrence of Scylaspora cf. elegans in the base of the PALF (sample MPA 55403) may imply a slightly younger Pridoli age for the formation in the Sawdde section. In Spain, S. elegans is a biozonal index species for the mid- to late Pridoli Scylaspora elegans – Iberospora cantabrica EC Biozone. Additional samples need to be studied to determine whether the PALF should be assigned to this younger biozone.

These findings underpin the belief that the both the PALF and FEF lie above a regional, mid-Pridoli Hiatus and are associated with the development of separate, but largely coeval incised valley systems (Hillier et al. Reference Hillier, Marriott, Higgs and Howells2019). The incision surface also serves to distinguish a younger division (MCF 3) from early levels of the MCF (Figure 1). Though evidently a significant feature in the west, this hiatus level remains unrecognized in eastern red bed successions (see Section 6h).

4.a. Methodology

Our research has focused primarily on the analysis of sedimentary lithofacies within the circa 120-km-long crop of the late Ludfordian to mid-Pridoli rocks that extends from south Pembrokeshire, in south-west Wales, to the Type Ludlow area of the Welsh Borderland (Figure 1) and which includes the CarF, TilF, DCSF, AF, CMSF, RF, PMF, TemF and PALF. Sections in the Clun Forest area to the NW and in the eastern Silurian inliers at Woolhope, Malverns, May Hill, Gorsley and Usk have also been assessed. Facies analysis of the Rumney Borehole near Cardiff has also been undertaken. Numerous small exposures cited by previous workers have also been examined and are referenced individually in the succeeding text. In addition to Kirk’s (Reference Kirk1951) published work, additional data for the poorly exposed tract between Presteigne and Brecon that sits astride the WBFS has been obtained from her unpublished field maps and manuscripts archived by the National Museum and Galleries of Wales (Kirk, Reference Kirkunpublished manuscript) and her unpublished PhD thesis, University of Cambridge, Kirk, Reference Kirk1947. In total, 33 sections were logged in detail, and these field observations were supplemented by the examination of selected petrographic thin sections. The principal sections comprise mainly former ‘tilestone’, building stone and aggregate quarries, road cuts and stream sections. Many former exposures of the LBB and its equivalents have suffered as a result of over-collecting, but fresh sections were examined at Downton Weir Quarry near Ludlow and at a previously unrecognized locations at Gwernilla and on Bradnor Green Golf Course in the Clun Forest area. At the time of writing, permission had not been granted to access the type section of the TemF along the River Teme at Ludlow.

Samples from selected sections and intervals have been processed for palynological analysis. Information for each specimen referred to in the text includes sample number (prefixed MPA for BGS samples), slide number, England Finder slide co-ordinate (e.g. M4/2) and specimen number. Specimens with the prefix ‘MPK’ are stored in the collection of Type and Figured micropalaeontological specimens of the BGS, Keyworth, Nottingham, UK. Specimens with the prefix KH and PAL are stored in the School of Biological, Earth and Environmental Sciences, University College Cork.

4.b. Lithofacies

4.b.3. Lithofacies 1: Distal river- and wave-influenced delta front

This lithofacies characterizes the uppermost part of the CarF (in many sections, including the LBBM and the PSM, CarF 2) as well as similar, but more sandstone prone facies in the Usk and May Hill inliers (CarF 3). It is characterized by low bioturbation indices, having a restricted shelly fauna and exhibiting synaeresis cracks and wrinkle structures. The lithofacies comprises a heterolith of non-amalgamated, very fine- to medium-grade sandstones and silty mudstones (Figures 8a-c). Sandstones are buff to grey, commonly cm- to dm-bedded and sharp-based. Bed bases may be erosive and strewn with mudstone intraclasts and/or skeletal debris. Some beds infill erosive gutters. Internally, beds are predominantly parallel-laminated or contain hummocky cross-stratification, current or wave ripple cross-lamination (Figures 8a and b). A minority of beds exhibit convolute lamination, and some are massive. Bed tops commonly preserve plane bed parting lineation and wave or current ripples (Figure 8d). Some bed tops preserve wrinkle structures. Common are erosively based, guttered sandstone beds that contain hummocky cross-stratification (Figure 8e). Sandstone beds grade upward into cm- to dm-thick grey or olive green mudstones and siltstones which are commonly graded. These are generally parallel- or cross-laminated and contain mm-thick very fine- to fine-grained graded sandstone laminae or cm-thick, lenticular or wavy-bedded sandstones. Common are sandstone-filled synaeresis cracks (Figure 8d). Some mudstone bedding surfaces preserve wrinkle structures (Figure 8f). In Clun Forest, bedsets in this lithofacies comprise m-thick, disorganized units of interbedded sandstone and mudstone deformed beds above soft sediment shear zones. Internal deformation is dominated by asymmetric or isoclinal folds with low-angle duplex thrust faults. Overall, sandstone beds thicken- and coarsen-upward within units of this lithofacies.

Figure 8.

Distal river- and wave-influenced facies association. (a–b) Heterolithic bedset with hummocky cross-statification, Bradnor Green Golf Course, scale bar 0.5 m (0 to 2 m Figure 10c). Dashed lines 1 to 5 represent position of denticle-rich vertebrate bone beds of the Ludlow Bone Bed Member, with bed 1 being the local equivalent of the Ludlow Bone Bed. Grey intervals in (b) represent laterally continuous mudstone interbeds. Note similar style of stratification above and below basal bone bed. (c) Interbedded, cross- and parallel-laminated sandstone beds and muddy siltstones, Sawdde Gorge (Cae’r mynach Formation). Note typical sheeted and lenticular geometries and isolated current-rippled sandstone lenticle (r); scale bar 5 cm. (d) Bed top view of rippled fine-grained sandstone, veneered with mudstone with well-developed sandstone-filled synaeresis cracks (sy). Note paired Arenicolites burrow entrances (Ar), and preservation of the gastropod Turbocheilus (T); loose block, Capel Horeb Quarry. (e) Guttered sandstone bed (with small-scale fault offset) with well-developed wing; internally, bed contains hummocky cross-stratification; Sawdde Gorge, scale bar 0.25 m (3 m on Figure 19). (f) Siltstone bed with well-preserved wrinkle structures, Werngwilym (0.25 m, Figure 22d). Note variable wavelengths of wrinkle structures and flat-topped morphology.

Bioturbation is generally low to moderate (Ichnofabric Index (II) Droser & Bottjer, Reference Droser and Bottjer1986, of 1 to 3), being dominated by Arenicolites, Planolites, Palaeophycus, Chondrites and Skolithos (Figure 8d). Preserved macrofaunas are dominated by bivalves and gastropods, the latter including Turbocheilus helicites (the Platyschisma helicites of earlier reports); a restricted assemblage of articulated brachiopods forms a subordinate component and is absent from some sections. Many sandstone and mudstone beds contain carbonized plant debris.

Common in sections in the north and east of the study area are mm- to cm-thick phosphatic bone-rich sandstone laminae or beds that, on weathering, take on the characteristic gingerbread colour and texture (Bassett et al. Reference Bassett, Lawson and White1982; Figures 8b, 9a-c and 10a-c) of the LBBM, but bone, fish scale and phosphatized mudstone pellet and pebble-bearing levels are present at lower levels of the CarF successions of the eastern inliers (e.g. Lawson, Reference Lawson1955). These bone-bearing levels occur either as discrete beds traceable over the scale of the exposure, or more commonly as discontinuous lags in erosive gutters or at bases of sandstone beds. They may be parallel-laminated or worked into wave or current ripples. The bone beds comprise thelodont and acanthodian fragments, inarticulate brachiopods, phosphate nodules and quartz granules (Antia, Reference Antia1979; Bassett et al. Reference Bassett, Lawson and White1982; Dineley, Reference Dineley, Dineley and Metcalf1999).

Figure 9.

(a) Rippled Ludlow Bone Bed Member at Downton Weir Quarry (North), 2.95 m Figure 10a. (b) Thin-section photomicrograph of the Ludlow Bone Bed Member shown in Figure 9a. Note dominance of vertebrate bone fragments and spines; plane-polarized light, scale bar 1 mm. (c) Thin-section photomicrograph of two vertebrate bone-rich laminae in Ludlow Bone Bed Member from Bradnor Green Quarry (0.95 m of Figure 10c). Laminae directly overlie underlying fine-grained sandstone hummocky bedform and laterally amalgamate and thicken into adjacent topographic lows. Plane-polarized light, scale bar 1 mm.

Figure 10.

Graphic logs through upward coarsening and thickening parasequences. (a) Downton Weir Quarry (north side of River Teme). (b) Downton Weir Quarry (south side of River Teme). (c) Bradnor Green Golf Course (note change in scale). Key to logs in Fig. 13. EPH, early Pridoli Hiatus surface.

The lithofacies is interpreted as forming on the distal reaches of river- and wave-influenced delta fronts, below fair-weather, but above storm-wave base, in settings that its limited assemblage of articulated brachiopods confirms was open to the sea. Sandstone beds and laminae were primarily emplaced by fluvially derived gravity flows or from suspension; hummocky cross-stratification and wave ripples provide evidence of storm-wave reworking (e.g. Dafoe et al. Reference Dafoe, Gingras and Pemberton2010; Olariu et al. Reference Olariu, Steel and Petter2010; Bailey & Bailey, Reference Bailey and Bailey2019). Interbedded mudstones and siltstones were deposited as fair-weather suspension fallout deposits, or as hyperpycnal fluid mud (Bhattacharya & MacEachern, Reference Bhattacharya and MacEachern2009). The common synaeresis cracks are interpreted as being formed by salinity variations associated with freshwater plumes or freshets (MacEachern et al. Reference MacEachern, Bann, Bhattacharya, Howell, Giosan and Bhattacharya2005, Reference MacEachern, Pemberton, Bann, Gingras, MacEachern, Bann, Gingras and Pemberton2007). Guttered bedsets, commonly containing hummocky cross-stratification, are interpreted as the deposits of erosive events created either by fluvial-derived downflows or storm-generated, downwelling coastal jets. The layer-parallel faulted intervals with convolute lamination are interpreted as slide-bound slumps generated by slope instability and/or of offering evidence of seismic events.

Trace fossils comprise an impoverished mixed Cruziana–Skolithos ichnofacies. The generally suppressed nature of bioturbation supports the interpretation of a stressed environment of deposition (Bann & Fielding, Reference Bann, Fielding and McIlroy2004; Fielding et al. Reference Fielding, Bann, Trueman, MacEachern, Bann, Gingras and Pemberton2007; Gani et al. Reference Gani, Bhattacharya, MacEachern, MacEachern, Bann, Gingras and Pemberton2007; MacEachern et al. Reference MacEachern, Pemberton, Bann, Gingras, MacEachern, Bann, Gingras and Pemberton2007). The wrinkle structures are interpreted as matgrounds that developed primarily atop sandstone event beds (Bailey & Bailey, Reference Bailey and Bailey2019) but also on fair-weather fine-grained interbeds. Their occurrence in this environment is well documented from Phanerozoic and Palaeozoic examples (Mata & Bottjer, Reference Mata and Bottjer2009), a prerequisite for formation appearing to be low levels of bioturbation due to environmental stress (Hagadorn & Bottjer, Reference Hagadorn and Bottjer1997, Reference Hagadorn and Bottjer1999; Pflűger, Reference Pflűger1999). A similar lithofacies is observed in the Wenlock age Gray Sandstone Formation, where salinity variations associated with freshwater plumes are interpreted as leading to impoverished infaunas and subsequent matground colonization of the sea bed (Hillier & Morrissey, Reference Hillier and Morrissey2010). Nicholls (Reference Nicholls2019) also identifies such features in deep water deposits of western mid Wales formed during the period of environmental flux associated with the Late Ordovician glacioeustatic lowstand. Salinity-induced environmental stress has been interpreted as the causative mechanism for changes in macrofauna across the basin during Late Ludlow times (Allen & Tarlo, Reference Allen and Tarlo1963; Holland & Williams, Reference Holland and Williams1985). The matgrounds would have formed a prolific food source for the grazing gastropod faunas (Palmer, Reference Palmer, Aldridge, Siveter, Siveter, Lane, Palmer and Woodcock2000), although Peel (Reference Peel1984) proposed that the abundant Turbocheilus helicites may have had a sedentary, ciliary-feeding habit.

Analysis of delta deposits in the rock record has recognized the similarity of shoreface and wave-dominated delta-front deposits (e.g. Dafoe et al. Reference Dafoe, Gingras and Pemberton2010). Trace fossil assemblages have been a useful tool in discriminating between deltaic environments containing ‘stressed’ ichnological assemblages with reduced ichnodiversity and bioturbation intensity and non-deltaic shoreface deposits (e.g. Bann & Fielding, Reference Bann, Fielding and McIlroy2004; Dafoe et al. Reference Dafoe, Gingras and Pemberton2010). In addition, the abundance of traces attributed to suspension feeding organisms and the general poorly developed Skolithos ichnofacies has been inferred as a discriminator between river- and wave-dominated deltas, with river-dominated deltas having a prevalence of the Cruziana ichnofacies (MacEachern et al. Reference MacEachern, Bann, Bhattacharya, Howell, Giosan and Bhattacharya2005; Dafoe et al. Reference Dafoe, Gingras and Pemberton2010). In this study, such distinction has not been possible, and we interpret this lithofacies as a mixed process one (river- and wave-influenced).

4.b.4. Lithofacies 2: Proximal wave-influenced delta front

This lithofacies mainly occurs in the DCSF and CMSF. It comprises a lithofacies dominated by micaceous, very fine- through to medium-grade, buff to grey/green well-sorted sandstones. Individual beds have erosive bases, often strewn with mudstone rip-up clasts or skeletal debris (Figures 10a-c). Bed bases are planar, or more commonly erosive and convex-up. Internally, beds are dominated by hummocky and swaley cross-stratification, and planar-lamination (Figures 11a and b). Occasionally, convolute lamination is observed (Figure 11c). Beds often fine-upward into micaceous finer-grained sandstone, or less commonly, micaceous siltstone. The latter contain common synaeresis cracks. Beds are generally of dm-scale thickness, and they commonly amalgamate. Bedding surfaces preserve both wave and current ripples. Bedsets within this lithofacies reflect upward-thickening and -coarsening above deposits of the distal river- and wave-influenced delta-front lithofacies described above (Figures 10a-c). The Ichnofabric Index is low (1 to 2), comprising Arenicolites, Planolites and Skolithos. Beds locally preserve abundant plant debris.

Figure 11.

Proximal wave-influenced delta-front facies association. (a) Amalgamated bedset comprising predominantly low angle and swaley cross-stratification, Downton Weir Quarry (south), 0.5 to 3 m Fig. 10b. (b) Closeup of bedset with swaley cross-stratification beneath 5 cm scale bar, and hummocky cross-stratification above it, Downton Weir Quarry (North). (c) Convolute lamination displaying symmetrical deformation, Pentre Jack; hammer is 0.3 m long.

The lithofacies was deposited on the proximal front of a wave-dominated delta above fair-weather wave base (e.g. Coates & MacEachern, Reference Coates, MacEachern, MacEachern, Bann, Gingras and Pemberton2007; Dafoe & Pemberton, Reference Dafoe, Pemberton, MacEachern, Bann, Gingras and Pemberton2007). Vertical amalgamation of bedsets and the preservation of swaley cross-stratification towards the top of some cycles reflect high-energy progressive sorting associated with wave and current reworking. Convolute lamination is likely to be the product of wave loading and/or rapid sedimentation. Salinity variations induced by freshwater plumes led to the development of synaeresis cracks. Trace fossils comprise an impoverished Skolithos ichnofacies.

4.b.5. Lithofacies 3: Proximal river-influenced delta front

This lithofacies mainly occurs in the TilF but is locally present in the DCSF. It is dominated by dm- to m-thick, fine- to coarse-grained sandstone beds that are locally pebbly (Figures 12a-c). Parallel-lamination (with associated parting lineation) is common, with subordinate massive sandstone beds. In the latter, floating outsized mudstone and vein quartz granule clasts may be present. Bed bases preserve bounce marks and are locally erosive. Occasionally, thick principally massive beds, but with subordinate convolute lamination are locally developed attaining a maximum observed thickness of 2.8 m (Figure 12a-c). Bedding is predominantly planar and erosional over the scale of the exposure. A few bedset boundaries are erosional and convex-up, with overlying dm-thick sandstone beds containing hummocky and swaley cross-stratification (Figure 13). Decimetre-thick planar-laminated and hummocky beds often have a fining-upward signature. Small-scale current ripple development is occasionally preserved. Rarely developed are thin, micaceous mudstone interbeds, some of which contain sandstone injections (up to 10 cm long) from underlying beds. Bioturbation is uncommon and extremely impoverished (Ichnofabric Index of 1 or 2), being dominated by Skolithos linearis. Skeletal concentrations of gastropods, crinoid ossicles, bivalves and less common brachiopods are observed as lags at bed bases, or in discrete erosional hollows. Plant debris is locally common.

Figure 12.

Proximal river-dominated delta-front facies association at Stonehouse Dingle. (a) Graphic log of the exposed succession in Stonehouse Dingle, exposing an upward-coarsening and -thickening interval of distal river- and wave-influenced facies association overlain by the proximal river-dominated delta-front facies association. Key to logs given in Fig. 13. (b–c) Quarry face (14.5 to 21.5 m Fig. 12a) containing a lower massive, and upper deformed bed separated by massive to parallel-laminated clinoform bedsets which dip to 240^o. (d) Quarry face orthogonal to clinoform dip direction comprising the upper deformed bed with convolute lamination (con; top and base indicated). Deformed bed overlies massive to parallel-laminated clinoform bedsets (cl).

This lithofacies is interpreted as being dominated by deposits of proximal delta-front river-fed hyperpycnal flows based on the dominance of parallel-laminated sandstone beds (e.g. Olariu et al. Reference Olariu, Bhattacharya, Xu, Aiken, McMechan, Giosan and Bhattacharya2005; Plink-Björklund & Steel, Reference Plink-Björklund, Steel, Giosan and Bhattacharya2005; Enge et al. Reference Enge, Howell and Buckley2010; Olariu et al. Reference Olariu, Steel and Petter2010). Massive beds offer evidence of deposition from high-energy, high-concentration gravity flows, with some thicker beds that display convolute lamination, formed by the over-steepening and subsequent collapse of mouth bars (e.g. Olariu et al. Reference Olariu, Steel and Petter2010). Wave and storm influence is limited to the preservation of swaley and hummocky cross-stratification. Sandstone injection phenomena were presumably created by rapid sedimentation and associated elevated pore pressure. The impoverished ichnofauna reflects the environmental stresses associated with riverine discharge, salinity variation and high sedimentation rates (e.g. Dafoe & Pemberton, Reference Dafoe, Pemberton, MacEachern, Bann, Gingras and Pemberton2007; Coates & MacEachern, Reference Coates, MacEachern, MacEachern, Bann, Gingras and Pemberton2007).

At Stonehouse Dingle, bedsets arranged in a low angle, inclined architecture preserve the form of a delta-front clinothem (Figures 12b and c) consistent with outbuilding from the NE into an offshore region of moderate water depth. The low diversity, poorly developed archetypal Skolithos Ichnofacies attests to the highly dynamic, high-energy depositional environment.

4.b.6. Lithofacies 4: Distributary Mouth Bars

The lithofacies locally sits at the top of upward coarsening and thickening cycles in the TilF and DCSF. It comprises planar-laminated, massive or subordinate trough or tabular cross-stratified, dm- to m-thick, fine- to coarse-grained sandstones (Figures 10a, b and 14a-c). Some cross-bedded units contain bipolar palaeocurrents and have mudstone-draped foresets. Beds are tabular or infill broad scours. Bases are generally planar to mildly erosive, commonly with guttered bases. Erosion surfaces may be strewn with mudstone rip-up clasts. Beds display amalgamation and internal scour surfaces. Current ripples are subordinate to larger-scale bedforms and often are arranged in climbing ripple trains. Parting lineation is common. Bedsets sometimes contain convolute lamination, with deformed cross-lamination often comprising small-scale asymmetric folds. Mudstone interbeds are uncommon and comprise micaceous, well-laminated, mm- to cm-thick discontinuous lenses and beds, some with preserved plant debris. Bioturbation is generally absent, although Skolithos is locally observed. Sandstones often contain common plant debris. Some sandstone beds contain ovoid or tubular carbonate nodules (e.g. Figure 10a, 14c and 15a), the latter often bifurcate downwards. Although not corroborated in this study, it is likely this lithofacies at Bradnor Hill has yielded fish faunas, including heterostracans, thelodonts, osteostracans and acanthodians (Figure 8c and d; Banks, Reference Banks1856; Dineley, Reference Dineley, Dineley and Metcalf1999).

Figure 13.

Graphic log through section at Capel Horeb Quarry.

Figure 14.

(a) Planar and current ripple (cr) cross-laminated sandstone of the distributary mouth bar facies association, Downton Weir Quarry (south); 3.75 m Fig. 10b. (b) Planar-laminated distributary mouth bar facies association with guttered bedset base (g), Downton Weir Quarry (south); 3.4 m Fig. 10b. (c–d) Graphic log (c), and image (d) through distributary mouth bar and terminal distributary channel facies associations at Bradnor Green Quarry, scale bar 0.5 m (for key see Fig. 13). (e) Deformed, over-steepened cross-sets with convolute lamination, Rhyblid. Scale bar 0.25 m. (f) Bedform foreset of terminal distributary channel facies association with thin micaceous mudstone drapes; scale bar 5 cm. Bradnor Green Quarry, 1.0 m Fig. 14c.

Figure 15.

(a) Bedding plane view of topmost Downton Castle Sandstone Formation with well-developed ovoid calcrete nodules (n), Llanstephan (3.6 m Fig. 22c). (b) Massive mudstones of the coastal plain facies association with well-developed wedge-shaped peds (highlighted) and vertic calcrete tubules, Cwmffrwd. Hammer 0.3 m long. (c) Tabular-bedded multistorey fluvial channel encased in coastal plain lithofacies mudstones, Green Castle; scale bar 1 m. (d) Tabular fluvial sheet sandstone bed with solitary cross-bed set, Golwg y Byd; hammer 0.3 m long.

The lithofacies is interpreted as the deposits of delta distributary mouth bars (e.g. Olariu & Bhattacharya, Reference Olariu and Bhattacharya2006; Olariu et al. Reference Olariu, Steel and Petter2010; Li et al. Reference Li, Bhattacharya, Zhu, Garza and Blankenship2011) and contains both subaqueous and subaerial elements. Unidirectional traction deposits dominate the preserved architecture and represent energetic, high sedimentation events as fluvial delta distributaries discharged into the coastal zone as hyperpycnal underflows. Bipolar palaeocurrents and mudstone drapes are attributed to tidal influence. The massive sandstone beds represent high-energy, high-concentration gravity flows (Olariu et al. Reference Olariu, Bhattacharya, Xu, Aiken, McMechan, Giosan and Bhattacharya2005; Plink-Björklund & Steel, Reference Plink-Björklund, Steel, Giosan and Bhattacharya2005). Interbedded parallel-lamination, massive and ripple cross-lamination may represent waxing and waning of underflows (Olariu et al. Reference Olariu, Steel and Petter2010). Convolute lamination was developed through possible over-steepening of the mouthbar, accentuated by high sedimentation rates. The ovoid carbonate nodules represent poorly developed calcrete palaeosol horizons (Stage 1 per Machette, Reference Machette and Weide1985), with tubules representing calcified root traces (Klappa, Reference Klappa1980) or burrow fills. The calcretes developed following prolonged subaerial emergence of delta lithosomes associated with the early Pridoli Hiatus and as such are not viewed as linked to mouth bar sedimentation (see Section 6.d below).

4.b.8. Lithofacies 6: Coastal plain

In the TemF and RF, this lithofacies is dominated by olive green to grey mudstones and siltstones and subsidiary green to brown dm-thick micaceous sandstones in cm- to dm-thick besdets. Locally (e.g. at Green Castle), red/maroon colour mottling is observed around desiccation cracks and ped surfaces. Mudstones and siltstones appear massive or are parallel- or cross-laminated. Occasionally, m-thick inclined heterolithic bedsets are observed. Isolated ovoid and tubular carbonate nodules are common as are subhorizontal slickensided fracture surfaces arranged in conjugate sets which rotate previously horizontally bedded carbonate concretions (Figures 15b and 16). Desiccation cracks are commonly observed. Rarely observed are m-thick muddy siltstone beds with low-angle inclined master bedding surfaces (e.g. 60 to 61 m, Figure 16). Skolithos is common. Locally developed in the TemF in the north and east of the study area are dm-thick fine- to medium-grade buff or green sandstone sheets that contain current ripple cross-lamination or parallel-lamination. Scattered through some of these sandstones are vertebrate bone and eurypterid fragments, bivalves, gastropods, lingulids and quartz granules (Elles & Slater, Reference Elles and Slater1906; Allen & Tarlo, Reference Allen and Tarlo1963; Antia, Reference Antia1981). In addition, Antia (Reference Antia1981) recorded wavy and oncolitic stromatolites at Onibury.

Figure 16.

Graphic log of terrestrial facies associations, Cwmffrwd; for key refer to Fig. 13.

This lithofacies is interpreted as the deposits of a mud-prone low-gradient coastal plain environment (Hillier et al. Reference Hillier, Marriott, Higgs and Howells2019). The mudstones and siltstones represent both traction and suspended-load fallout deposits. Massive mudstones possibly represent soil mud-pellet aggregates deposited as a sheet-flood/ephemeral channel fills, or on in-channel muddy braid bars (Marriott & Wright, Reference Marriott and Wright2004). Subsequent compaction of the mud pellets led to a loss of sedimentary structures. The aggregates are thought to be produced during the shrinking and swelling of Vertisols, subsequently reworked and deposited by wind and alluvial processes (Marriott & Wright, Reference Marriott and Wright2004; Hillier et al. Reference Hillier, Marriott, Wright and Williams2007). The horizontal conjugate fracture sets represent wedge-shaped peds created by the shrinking and swelling of the Vertisols generated by seasonal wet–dry cycles (Marriott & Wright, Reference Marriott and Wright2004). The carbonate nodules are calcretes formed at the depth of seasonal wetting within the Vertisol profile (Stages 1 and 2 per Machette, Reference Machette and Weide1985). The low-angle inclined master bedding surfaces constitute inclined heterolithic stratification produced at accretionary benches or channel margins. In the east of the study area, the thin sandstone beds that contain vertebrate and invertebrate remains demonstrate a marine, most probably brackish water tidal influence (Allen & Tarlo, Reference Allen and Tarlo1963; Antia, Reference Antia1981). The predominance of green lithologies in the TemF and RF reflects primary colouration caused by reducing redox conditions associated with a predominantly high, but fluctuating water table. Colour mottling is interpreted as a redoximorphic indicator of this fluctuation.

4.b.11. Lithofacies 9: Inclined heterolithic tidal channels

This lithofacies occurs locally in the PALF, RF and PMF where it comprises inclined heterolithic bedsets of metre-scale thickness (Figures 17 and 18). Inclined bedset bases are marked by planar or gently undulatory erosion surfaces, which may be defined by discontinuous dm-thick, clast supported extraformational and/or intraformational mudstone clast and calcrete nodule lag conglomerate. Bedsets are dominated by low-angle (typically 15–20 degree) interbeds of fine- to medium-grained sandstone (locally pebbly) and laminated mudstone. Flaser, lenticular or wavy bedding is common. Medium-grained sandstones are sometimes trough-cross-stratified, with some bedsets containing bipolar palaeocurrent indicators and mudstone-draped foresets. Synaeresis cracks are observed. Bioturbation is generally low to moderate (II of 1 to 2), but locally more abundant, comprising Palaeophycus, Planolites, Skolithos sp. and Skolithos linearis, with less common Teichichnus, Schaubcylindrichnus, Thallasinoides, Arenicolites and Asterosoma. The PALF contains modiolopsid bivalves and Lingula. In the RF, Pachytheca, plant, fish and eurypterid fragments are common, as are spheroidal phosphate nodules. A solitary bedset of lingulid and plant-bearing deposits occurs in the PMF Rumney Borehole.

Figure 17.

Bedsets in the Temeside Mudstone Formation of the inclined heterolithic tide-influenced fluvial channel facies association overlain by coastal plain mudstones (contact indicated by dashed line) at the Cae’r mynach stream section. Photograph corresponds to 10.7 to 13.5 m in Fig. 22a.

Figure 18.

Tidal sandflat facies association overlying inclined heterolithic tidal channel deposits of the Pont ar Llechau Formation, Sawdde Gorge (24 to 30 m Fig. 19, way up to right).

The master bedding surfaces represent inclined heterolithic stratification (IHS; Thomas et al. Reference Thomas, Smith, Wood, Visser, Calverley-Range and Koster1987) of tidal/fluvial point bars. The basal erosion surface and overlying intraformational conglomerate records lateral migration of the channel thalweg and its lag deposit. Simple sets of trough cross-stratification record the migration of 3D megaripples, and bipolar palaeocurrents and mudstone drapes reflect tidal influence. This lithofacies is similar to described point bars in estuarine bay head deltas (e.g. Allen & Posamentier, Reference Allen, Posamentier, Dalrymple, Boyd and Zaitlin1994; Hillier et al. Reference Hillier, Marriott, Higgs and Howells2019) or in tide-influenced delta plain, distributary channel point bars (e.g. Baker et al. Reference Baker, Harris, Keene, Short, Flemming and Bartholoma1995; Choi et al. Reference Choi, Dalrymple, Chun and Kim2004; Willis, Reference Willis, Giosan and Bhattacharya2005). Bioturbation indicates an impoverished brackish-water Skolithos–Cruziana ichnofacies dominated by infaunal traces.

4.b.12. Lithofacies 10: Tidal sandflat

The lithofacies dominates the PALF and overlies inclined heterolithic tidal channel deposits (Figure 18). It comprises red to purple, locally green, ill-sorted argillaceous, gritty and pervasively bioturbated sandstones with common high- and low-chroma colour mottling. Bedding is tabular and locally wavy, with discontinuous siltstone laminae and mudstone drapes. Common in beds at the top of the lithofacies are ovoid calcrete nodules. Rarely observed are oncoid-like cm-diameter iron oxide ferricretes (Figure 19, 48.8 m). Subordinate red muddy siltstones with sandstone pinstripe laminae contain desiccation cracks, Skolithos, Planolites, and rare Beaconites antarcticus burrows. At Rhyblid, this lithofacies is grey in colour and comprises wavy, flaser and linsen-bedded laminasets with common current ripple and less common wave ripple cross-lamination. Macrofaunas include Lingula, modiolopsid bivalves, gastropods and rare rhynchonellid brachiopods (e.g. Figure 19). A thin lingulid-bearing development of this lithofacies occurs in the PMF in the Rumney Borehole above likely Lithofacies 9 deposits (Figure 20).

Figure 19.

Graphic log, Sawdde Gorge. For key, see Fig. 13. Palynology samples (MPA 55411-14) from the Cae’r mynach Formation discussed in the text (Section 3.e.2) were collected from lower in the section.

Figure 20.

Graphic log of Rumney Borehole. For key, see Fig. 13. LBBM, Ludlow Bone Bed Member.

The lithofacies is interpreted as the deposits of a tidal sandflat that developed marginal to tidal channels. The flats were subject to frequent wetting and drying in response to a fluctuating water table, preserving calcrete palaeosols during episodes of prolonged subaerial exposure (Stage 1 per Machette, Reference Machette and Weide1985). Mottling and ferricretes are interpreted as redoximorphic in nature (Veneman et al. Reference Veneman, Spokas, Lindbo, Rabenhorst, Belloli and J McDaniel1998; Jacobs et al. Reference Jacobs, West and Shaw2002); similar features are observed in interpreted tidal mixed-flat deposits of the FEF (Hillier et al. Reference Hillier, Marriott, Higgs and Howells2019).

5.a. River-influenced delta association

Riverine influences dominated the progradation of a north-westerly sourced TilF delta system into the Western Province. Mapping and dating criteria outlined in Section 3 underpin the recognition of four separate TilF river-influenced delta parasequences (TilF 1 to TilF 4, Figure 1), each comprising upward-coarsening and -thickening bedsets 10 to 15 m thick (e.g. Figures 12, 13, 19, 21 and 22). The transition from the distal into proximal river-influenced delta-front deposits is characterized by a gradual amalgamation of sandstone beds and progressive reduction in silt and mudstone interbeds reflecting depth-dependent fluid power and reworking of fine-grained sediments. Across this transition, there is in general a marked reduction in ichnofaunas and macrofossil assemblages. The upward transition into distributary mouth bars and/or terminal distributary channels is linked to a grain-size jump (e.g. Figures 19 and 21) and a reduction in the estimated mica content of sandstone beds. The transition into overlying coastal plain or inclined heterolithic tide-influenced fluvial channel lithofacies associations is sharp in all observed instances and commonly defined by erosion surfaces and/or winnowed conglomerate lags (see below).

Figure 21.

Graphic log, Cennen Valley roadcut. For key, see Fig. 13.

Figure 22.

Graphic logs illustrating proximal to distal parasequence variations. (a) Cae’r mynach stream section. (b) Bedw-Hir, Gwenddwr stream section. (c) Llanstephan, River Wye (beneath road bridge). (d) Werngwilym waterfall section. (e) Gwernilla log. (f) Erosive base of Temeside Mudstone Formation at Werngwilym (7.8 m Fig 22d); scale bar 0.5 m. For key to logs, see Fig. 13. LBBM, Ludlow Bone Bed Member; EPH, early Pridoli Hiatus surface.

5.b. Wave-influenced delta association

Wave-related processes exercised a strong influence on the early Pridoli DCSF delta system, Hobson’s (J.S.C.Hobson, unpub. PhD thesis, University of Birmingham, Hobson, Reference Hobson1960) ‘Welsh Delta’, which advanced from the north-east. In its type area, the latter appears to comprise a single parasequence of upward-coarsening and -thickening bedsets up to 10 m thick, but in more westerly and distal settings, at Gwernilla, two separate progradational parasequences are recognizable (Figure 22e). The transition from the distal into proximal wave-influenced delta-front deposits is gradual in nature. Where present, the upward transitions into distributary mouth bar and/or terminal distributary channel lithofacies are abrupt. Such lithofacies, together with the palaeoseaward-dipping delta-front clinoforms observed at Stonehouse Dingle, serve to locate points of fluvial supply to otherwise wave-influenced deltaic coastlines. An earlier prograde of wave-influenced delta association is locally recognized in the Aston Munslow Member.

5.c. Wave-influenced, forced regression delta association

This association is restricted to the successions in the Woolhope, Gorsley and May Hill inliers where it comprises facies of both the RF and CMSF (the Woolhope Delta of Hobson, unpub. PhD, thesis, University of Birmingham, Hobson, Reference Hobson1960). The latter formation comprises a single deltaic parasequence of upward-coarsening and -thickening bedsets similar to that of the DCSF with back-barrier deposits of the RF (Figure 24a). However, it differs from the DCSF in its provenance and regional geometry. It represents a narrow NW/SE-orientated deltaic barrier sand bar supplied from the east and sited south-west (seaward) of an extensive back-barrier RF tract (Figures 3c and 24a). The latter was the site of heterolithic tidal channel lithofacies with thin developments of coastal plain lithofacies.

Figure 23.

(a) South-west to north-east correlation illustrating lithofacies variations between measured sections. (b) North-west to southeast correlation illustrating proximal to distal variations in lithofacies associations.

Figure 24.

(a) Graphic logs from north-west to south east sections through the Woolhope to May Hill inliers, extending to Brook House in the Usk Inlier detailing lithofacies of the early Pridoli forced regression. (b) Thin-section photomicrograph of Upper Linton Pebble-Bed (ULPB) at Linton Quarry illustrating well-rounded phosphate intraclasts in plane-polarized light (scale bar 100 microns). (c) ULPB at Station Quarry, Longhope. Top image shows cross-sectional view of ULPB with erosional base into underlying Cae’r mynach Formation mudstone; lower image showing ULPB top, scale bar 2cm. EPH, early Pridoli Hiatus surface; CarF, Cae’r mynach Formation; LBBM, Ludlow Bone Bed Member.

Both formations sit above thin deposits containing granule and pebble-grade phosphate nodules and that locally yield vertebrate and brachiopod debris, exemplified by the ULPB of the Gorsley and May Hill inliers (Figure 24b-c). We interpret these basal beds as regressive lags comprising cannibalized detritus from underlying formations. An assessment of current dating information (see Section 3) allied to local and regional lithofacies analysis (sections 4 and 6) allows both these basal features and the succeeding facies association to be viewed as the products of a widely felt forced regression.

5.d. Incised valley fill association

The tract between the Cilmaenllwyd Quarry and Rhyblid is unusual in its absence of the TemF (Figure 1). Here, the PALF infills a major incision feature and comprises a suite of estuarine units of predominantly tidal sandflat and inclined heterolithic tidal channel lithofacies (Figure 23a). Up to 29 m of such facies are present in the Sawdde Gorge and an estimated 32.5 m at Rhyblid (Supplementary Figure S2), where facies formed in an open-bay setting are also present. The process and location of valley incision accounts for the local absence of the TemF.

5.e. Old Red Sandstone continental association

The predominantly green lithofacies that make up the AF and early TemF existed initially alongside the sandy Ludfordian deltaic systems and, in this context, could be viewed as forming a contiguous, pediment colluvium and delta-top association. However, the subsequent more widespread accumulation of the TemF and MCF justifies their inclusion in what became an exclusive and long-lived ORS continental association. Moreover, in the majority of sections where continental overlie deltaic lithofacies, the contact is sharp and the topmost delta deposits display evidence of palaeopedogenesis including calcrete nodules and calcretized root traces. In contrast, transitions between the green coastal plain and red alluvial lithofacies are conformable and gradational.

In the TemF, calcrete-bearing mudstones host single and multistorey fluvial channel sandstones and units of sheet fluvial heterolithic lithofacies. The sandstone units, commonly richly micaceous, overlie sharp erosive surfaces and fine upwards, but their distribution appears random and parasequences are not readily apparent. Palaeocurrent vectors in the south-west that are more variable than in contiguous deltaic associations may reflect deposition within meandering channels and/or the influence of local topography. Hillier et al. (Reference Hillier, Marriott, Higgs and Howells2019) speculate that this system comprises an embryonic range-front alluvial network, with fluvial sandbodies possibly representing stream capture events. That fluvial sandbodies are less common in the late Ludfordian TemF implies either a reduction in fluvial supply or the establishment of a more mature coastal plain that was host to well established and more stable fluvial pathways.

The green lithofacies reflect the prevalence of a reducing diagenetic regime and of an elevated water table typical of a coastal plain environment. Restricted marine faunas confirm that deposition must have taken place close to sea level and that tenuous links to the open sea were maintained. The rapid, but gradual colour change from predominantly green to red lithologies that marks the base of the MCF records the transition into a better drained alluvial plain that was host to a deeper, fluctuating water table and promoted the oxidation of soil profiles.

6.a. Earliest Leintwardinian

The new architectural model presented for rocks of Ludfordian to early Pridoli age in Wales and the Welsh Borderland (Figures 1 and 23), together with their facies diagnosis, permit a level of parasequence-scale analysis and palaeogeographic reconstruction hitherto unachievable for this time interval. In the Western Province, the AF colluvium is overlain by TemF coastal plain mudstones. Rising base levels accommodated the deposits of this broad coastal plain with well-developed calcrete Vertisols, multi-storey and sheet fluvial lithofacies. The latter are observed at Green Castle and also Cwmffrwd, where some poorly to moderately well-sorted sandstones contain granule- to pebble-grade exotic clasts at their bases (J. Almond, unpub. PhD, thesis, University of Bristol, Almond, Reference Almond1983; Figure 16, 0–61 m) and others contain abundant detrital white mica of Caledonian provenance (e.g. Figure 15, 61–65.5 m). Palaeocurrents from individual micaceous sandstones at Green Castle, Cwmffrwd and Golwg y Byd indicate palaeoflow from the north-west, south-west and west, respectively (Figure 25). Such variation illustrates the likely persistent influence of local topography in a setting where Ludfordian strata overstep much older rocks and terrestrial conditions were largely maintained.

Figure 25.

Summary of palaeocurrent data from measured sections in study. Number at side of data plot corresponds to number of data readings except where more than one data type (e.g. gutter, wave ripple crest orientation) is shown graphically in each plot. In this scenario, numbers of data readings are given after each data type (e.g. gutter, 2; wave ripple 3)

These rivers negotiated a locally complex, fault-influenced topography to supply the Leintwardinian TilF delta of the Cennen region (TilF 1) (cf. Straw, Reference Straw1929). Here, the Golden Grove Axis served as a topographical hinge that separated emergent tracts to the west from the subsidence prone Cae’r Mynach Seaway to the east and provided a seeding point for the TilF delta system. The axis had links to transfer faults that connected the Carreg Cennen Disturbance, part of the Church Stretton Fault Zone, to fractures of the Pontesford Lineament. An uplifted footwall region generated by Ludfordian inversion of the Meusydd Fault (BGS, 1977) appears to have been most influential.

This early river-influenced delta faced a storm-stirred seabed (early Cae’r mynach Seaway) that extended across the former faulted basin margin and adjacent parts of the Midland Platform to cover the whole of south-east Wales and its Borderlands. It attained its greatest depths in the Clun Forest Sub-Basin, where Leintwardinian facies excluded from the CarF, of deeper aspect and southerly provenance, continued to accumulate. Cross-cutting relationships in the vicinity of the Church Stretton Fault Zone near Leintwardine may record local incision by early Ludfordian submarine canyons and/or slump scars which served to route sediment westwards to these deeper settings (e.g. Whitaker, Reference Whitaker1962, Reference Whitaker1994; Siveter et al. Reference Siveter, Owens and Thomas1989; Cave & Hains, Reference Cave and Hains2001; BGS, 2000).

6.b. Early Leintwardinian-Whitcliffian

The supply of Caledonian detritus from the north-west to the deltaic TilF coastline continued throughout the early Ludfordian. The Cennen area remained an initial focus for deposition, but TilF delta parasequences reveal a pattern of progressive progradation and expansion that saw Whitcliffian river-influenced deltaic lithofacies extended as far north as Capel Horeb.

Distal delta-front lithofacies of the CarF (0–4.8 m Figure 21) are seen in the Cennen Valley where they underlie two complete river-influenced TilF deltaic parasequence (TilF 1 and TilF 2, Figure 21, 4.8–20.85 m and 20.85–45.7, respectively). Palaeocurrents from terminal distributary channels and mouthbars in the Cennen Valley and Onen-fawr indicate palaeocurrent flow principally from a NW quadrant, with subordinate NW-directed vectors likely the result of tidal reworking (Figure 25). Primary current lineation supports the interpretation of sediment transport from the NNW, and wave ripple crests indicate a shoreline-oriented approximately WSW-ENE. The calcrete that caps the proximal river-influenced delta-front facies (Figure 21, 20.85–37.4 m) of TilF 2 record its initial emergence and the effects of ongoing Vertisol palaeopedogenesis. Five calcrete profiles are also observed in the succeeding succession of distributary channel fills, implying prolonged subaerial exposure (Figure 21, 38.05–41.6 m). The laminated green mudstone present (37.4–38.05) may record an abandoned channel fill and proximity to coastal plain lithofacies which dominate the overlying TemF1 deposits above.

Both TilF 1 and TilF 2 parasequences are exposed in ‘tilestone’workings at Cilmaenllwyd Quarry (SN 6676 2084 to 6614 2048; the ‘long quarry’ of earlier workers) where parallel-laminated sandstones with well-preserved unidirectional bounce and prod marks typical of proximal river-influenced delta-front deposits were exploited. Intervening ridges of unworked, medium-grained, locally pebbly sandstones displaying convolute lamination and large wave ripples as well as fine-grained sandstones with low-angle lamination are consistent with the distributary mouth bar lithofacies. Purple sandstones previously recorded by Strahan et al. (Reference Strahan, Cantrill, Dixon and Thomas1907) above the ‘Tilestones’ are here attributed to the PALF tidal sandflat lithofacies and overlie the mid-Pridoli incision surface (see Section 6f).

The Sawdde Gorge was beyond the reach of the initial TilF delta advance (Figure 23a). There, the cross-bedded, terminal distributary channel deposits that cap brachiopod-bearing, river-influenced delta lithofacies were emplaced exclusively by the second (TilF 2) progradation (Figure 19, 5.65–21.7 m). Rhyblid lay within reach of both the second and third TilF progrades (Figure 23a; TilF 2, 0–1.5; and TilF 3, 1.5–20.1 m Supplementary Figure S2). The TilF successions in the Sawdde and at Rhyblid both underlie the PALF incision surface. In contrast, Capel Horeb Quarry to the NE lay outside the region of greatest mid-Pridoli incision (Figure 23a), and here a TilF succession that also includes both Leintwardinian and Whitcliffian progrades (Figure 13, TilF 2, 2.6–8.95m; TilF 3, 8.95–39.8m) is abruptly overlain by TemF coastal plain facies.

Sedimentological evidence for shoaling episodes coeval with TilF 1, TilF 2 and TilF 3 in the CarF succession of the South-Eastern Province is ambiguous and may indicate that these episodes of progradation were influenced principally by local changes in accommodation space and sediment supply rather than external base-level events. Nevertheless, the migration into eastern CarF successions, late in the Leintwardinian, of the brachiopod Shaleria ornatella, which culminated in the local development of near monospecific shell banks (Phipps & Reeves, Reference Phipps and Reeve1967), has been seen to offer evidence, if not of shoaling, of an abrupt, regional change in seaway circulation patterns (Watkins, Reference Watkins1979). It is reasonable to speculate that this palaeoecological event was linked to westerly delta advance. Coincidental evidence of renewed scour and omission affecting the Gorsley Axis area offers an indication that tectonic forcing also remained important locally.

The Clun Forest Sub-Basin remained an extant feature for much of the early period of TilF advance. Its gradual demise as a site of deeper southerly sourced facies accumulation and the complementary spread across this region of shallower Cae’r mynach Seaway facies mirrors the pattern of the north-westerly supplied delta spread (Figure 1). However, the sub-basin, though it remained influential as a local depocentre, was abolished as a site of deeper water deposition in mid Whitcliffian times. This marked the period when the storm-influenced, delta facing facies of the Cae’r Mynach Seaway achieved their maximum lateral extent. Evidence that the subsequent shoaling was felt in other parts of the Cae’r mynach Seaway has been alluded to above (Section 3). The newly recognized Aston Munslow Member shows that the earliest wave-influenced deltaic deposits of the North-Eastern Province prograded south-westwards, reaching to the north of Ludlow in late Whitcliffian times. Facies that record coeval shoaling are seen further west (Stonehouse Dingle), and locally in the South-Eastern Province (Roath Park Lake Member), but CarF deposition remained extensive during this interval even at the point of greatest pre-Pridoli deltaic incursion.

6.c. Earliest Pridoli (post-Ludlow Bone Bed transgression)

The LBB transgression, where its impacts are preserved, resulted in a renewed deepening and re-expansion of the Cae’r mynach Seaway. Here, the early Pridoli deposits of this seaway (CarF 2) are envisaged once to have been present throughout much of the South-Eastern Province. Excision during the subsequent hiatus event led to their widespread removal (see below), leaving the lower levels of former ‘Speckled Grit’ succession of the Usk area and a thin development of CarF (CarF 2) above the LBB in the Rumney Borehole as its principal surviving representatives (Figure 19). The limited fauna present during this early Pridoli period of CarF deposition testify to restricted marine conditions. Locally, notably in the North-Eastern Province, trace fossil assemblages and the preservation of mat grounds (e.g. LBBM, PSM) imply that fluvial run-off remained influential and that deltaic coastlines were situated nearby. Certainly, multiple delta systems soon began to prograde into the newly created accommodation space influenced in part by ongoing regional subsidence.

At Downton Gorge and at Ludford Lane, the LBBM and PSM record distal wave-influenced deltaic deposition prior to the entry of the more proximal deltaic lithofacies that comprise the DCSF. Distributary mouth bar lithofacies locally cap this type succession which appears to offer evidence for a single uninterrupted delta advance. Wave ripple crests and gutter casts suggest sediment was supplied to an E-W-orientated coastline from the NE. Cross-stratification in the DCSF at Turner’s Hill, Dudley, observed by Ball (Reference Ball1951), also indicates sediment transport from the NE.

Proximal wave-influenced delta-front lithofacies dominate sections in the DCSF in the vicinity of the Church Stretton Fault Zone (Figure 23b). The sandstone succession in these more distal reaches of the delta system thins south-westwards. Two discrete parasequences are recognized at Gwernilla, but only one of these extends into the much thinner and more distal succession seen at Llanstephan (Figure 22c). It is likely that the two parasequences reflect local autocyclic processes as they are not observed elsewhere. Palaeocurrent vectors suggest that the terminal distributary channel and distributary mouth bar lithofacies seen at Bradnor Green were supplied from the NE (Figure 25).

West of the Church Stretton Fault Zone, in the Clun Forest area, sections at Croachan Dingle and at Stonehouse Dingle are significant in displaying river-influenced DCSF facies (Figure 23b). Proximal river-influenced delta-front lithofacies overlie heterolithic, distal river- and wave-influenced delta-front deposits. The latter contain common convolute-laminated beds and slump units that indicate the importance of mass flow processes in this area. Stonehouse Dingle is notable as the only section where steep delta clinoforms have been observed, and these confirm that the direction of delta progradation in this region, in common with the DCSF-type area, was from the NE. Deltaic deposition at the Croachan and Stonehouse sections occurred astride the axis of the former Clun Forest Sub-Basin, to the west of the Clun Forest Disturbance. It likely remained the region of greatest seaway water depths but also of ongoing seismic instability. East of the Clun Forest Disturbance, at Meeting House Lane, 16 m of proximal wave-influenced delta-front deposits are poorly exposed above distal river- and wave-influenced delta-front deposits. Here and in the Norton Inlier, rock fragments containing denticle-rich laminae, together with the gastropod Turbocheilus at the latter, demonstrate the presence, hitherto unrecorded (e.g. Holland, Reference Holland1959), of the LBBM.

River-influenced deltaic deposition continued in the Western Province where, though the Ludfordian succession as whole thickens to the NE, the TilF thins and is represented, at Fibua, Cae’r mynach and Bedw-Hir, by a single parasequence of the proximal river-influenced delta lithofacies (TilF 4) (Figures 22a, b and 23a). This final prograde marked the conclusion of the series of TilF delta advances into the Western Province that had been ongoing since the early Leintwardinian (Figure 1). However, the pattern of advance depicted by Figure 23a is misleading, the linear TilF crop being largely orthogonal to the dominant south-eastward direction of progradation. The distribution of TilF progrades appears more likely to offer a record of progressive side lap and/or the lateral expansion of the TilF delta system. In truth, the sub-crop extent of each progradation remains unknown, but the active delta front at the point of its early Pridoli culmination may have been extensive and be located in buried stratigraphy well to the east.

The case to view TilF 4 and the DCSF as representing coeval but separately sourced progradations into the Cae’r Mynach Seaway is made in Section 3. At their greatest extent, these separate delta systems likely merged to form a continuous deltaic coastline. River-linked process remained influential on south-east facing TilF shores. Delta-front clinoforms (Stonehouse Dingle), mouth bar and terminal distributary channel deposits (e.g. Downton Gorge, Bradnor Green) show where rivers also traversed south-west to westerly facing shores that were otherwise more strongly influenced by wave activity.

Evidence of any coeval early Pridoli delta advance into the South-Eastern Province was widely obliterated by the subsequent episode of erosion (see Section 6d below). Nevertheless, distal river- and wave-influenced delta-front CarF facies that underlie the local DCSF equivalent suggest that it was an active process in the Malverns area (S.J.Veevers, unpub. PhD thesis, University of Birmingham, Veevers, Reference Veevers2006; White et al. Reference White, Ellison and Moorlock1984).

Throughout the Western Province, to the west and landward of the TilF deltaic shoreline, green, early Pridoli coastal plain facies of the TemF (TemF 1) continued to accumulate in front of coeval MCF red beds. Evidence of intercalation with delta-top TilF facies is seen in the Cennen area TilF 2 parasequence, where thin deposits of green/grey-laminated mudstones interbed with calcrete hosting sandstones and conglomerates of the terminal distributary channel lithofacies (Figure 23). Channellized micaceous sandbodies recognized within both the TemF and MCF locate the sites of south-easterly flowing streams that supplied the delta shoreline (see Sections 3 and 5 above) and offer further evidence of synchronicity.

6.d. Mid-early Pridoli (post-early Pridoli Hiatus)

6.d.2. South-Eastern Province: Woolhope, Gorsley and May Hill inliers

That the late Ludfordian to early Pridoli successions of the South-Eastern Province differ significantly from those of the more northerly and western regions has been alluded to above. The principal differences relate to the nature of the basal erosion surface, the distribution of the RF and CMSF, and the absence of the TemF. Dating constraints, as outlined in Section 3, permit alternative correlations. Here, we explore a radical reinterpretation of the successions that developed south of the Vale of Neath Disturbance and west of the Malverns Axis, one informed by sequence stratigraphical models for forced regressions (e.g. Plint & Nummedal, Reference Plint, Nummedal, Hunt and Gawthorpe2000; Catuneanu, Reference Catuneanu2006).

The South-Eastern Province, prior to the Pridoli, had been a region of relative attenuation and local omission. Structural inversion is invoked as explanation for northern regions being uplifted during the early Pridoli to become an emergent, calcrete forming tract. In contrast, across regions south of the Neath Disturbance, it is the erosion surface overlain by bone-bearing levels, previously seen as equivalent to the LBB, that provide the evidence for coeval erosion. Evidence for channelling and calcretization is absent, and the juxtaposition of facies favours marine ravinement as the denuding mechanism (Figures 3 and 24a).

As to the north, the resumption of deposition was in response to a new episode of delta advance accompanied by a change, as least locally, in the provenance of sand-grade sediment (see Section 2). Initially, there was little space to accommodate the deposits of this putative easterly sourced system and, in response to regressive forcing, the nearshore high-energy zone shoreline would have moved rapidly westwards. The regions south of the Neath Disturbance and astride an initially still active Gorsley Axis were sites of greatest exhumation (Figure 3c). Whether earlier facies of the DCSF delta system ever accumulated in this region is a moot point, but the deep scour that accompanied the marine ravinenment event extended to depths below levels equivalent to the LBB and into the earlier Ludfordian CarF succession. It was on this regressive surface of marine erosion that the distinctive phosphatic pebble and bone-rich lags of the Woolhope, Gorsley and May Hill successions accumulated and the province’s wave-influenced forced regression facies association began to aggrade (Figure 24).

In its proximal reaches, a marked basinward shift in sedimentation is observed at the base of this developing association. RF successions that display inclined heterolithic tidal channels with thin local developments of coastal plain lithofacies (e.g. Shucknall Hill, Perton Lane, Priors Frome Quarry and Rushall in the Woolhope Inlier (Figures 3, 24a and 26), directly overlie exhumed Ludfordian CarF facies of offshore and distal deltaic aspect. In this scenario, these RF deposits accumulated in a setting seaward of the TemF 2 coastal plain, but behind a NW/SE-orientated barrier bar (CMSF) formed by the marine reworking of the putative delta front. The thickest development of these barrier facies between Gorsley and Clifford’s Mesne suggests that the Gorsley Axis, a structural feature closely linked to the trace of the Glasshouse Fault, remained active. It served first as a seeding point for barrier aggregation and subsequently to anchor the sand body in place throughout the mid-early Pridoli. These relationships recall the role played by the Golden Grove Axis in the Western Province at the Leintwardinian onset of TilF deltaic deposition (Figure 3). Wave reworking, well seen at Linton Quarry, was influential during much of the barrier’s development. Wave ripple crests at Clifford’s Mesne suggest that local shoals trended approximately NNW-SSE (Figure 25). Foresets associated with terminal distributary channel deposits seen in the upper part of the formation at Linton Quarry serve to locate the position of a point of fluvial sediment input from the ENE. The finer-grained CMSF succession seen to the south of the Glasshouse Fault, in the Longhope area, represents the seaward-facing facies of the barrier. These in turn passed southwards into the restricted marine facies of the remnant Cae’r mynach Seaway (CarF 3).

Figure 26.

Block diagrams illustrating the early Pridoli Hiatus and forced regression in the Southeastern Province. (a) Downton Castle Sandstone Formation delta coastline of the Malverns area faced the open marine Cae’r mynach Seaway to the south and west. (b) Early Pridoli Hiatus and forced regression with marine ravinement into underlying tracts and subsequent deposition of the Upper Linton Pebble Bed beneath deposits of the Rushall and Clifford’s Mesne Sandstone Formations. Note localized erosion of the Ludlow Bone Bed Member. CarF, Cae’r mynach Formation; DCSF, Downton Castle Sandstone Formation; EPH, early Pridoli Hiatus surface.

6.e. Late early Pridoli

Following the episode of forced regression and basinward shift in sedimentation, the onset of regional subsidence initiated renewed accumulation of ORS continental facies. The younger succession of TemF (TemF 2) began to accumulate across the whole of the North-Eastern Province on an expanding coastal plain with elevated water tables. Elsewhere, in areas where more mature drainage systems were established and water tables depressed, red bed diagenesis was a dominant factor. The subsequent spread of such conditions saw MCF facies established throughout the study area.

Mica and garnet-rich Caledonian detritus now supplied an ORS alluvial plain that, having advanced from the north, covered much of southern Britain. Lingulid and ostracoderm fragments recovered from MCF sandstones at the base of the ORS in the South-Eastern Province (Allen & Dineley, Reference Allen and Dineley1976) suggest proximity to a contemporary shoreline. Prior to the continental-scale late Variscan displacements achieved by the Bristol Channel–Bray Fault Line, this ORS coastal realm likely lay to the south of the present-day Bristol Channel and had close links to the Rheic Ocean.

6.f. Mid-Pridoli incision and valley infill

In the mid-Pridoli, widespread ORS alluvial deposition was punctuated by an episode of incision and valley formation within the Western Province (Figures 3d and 23a). Here, incision removed the TemF (Tem1) and ‘lower’ MCF deposits in the tract between Cilmaenllwyd Quarry and Rhyblid. Here, it is preserved as an estuarine incised valley fill comprising the PALF. The palynological evidence for the mid-Pridoli age of these facies is presented in Section 3. In the Sawdde section, above a basal conglomerate is an alternation of inclined heterolithic tidal channels and tidal sandflat lithofacies (Figure 19, 21.7-50.8 m) describing three parasequences. In contrast, at Rhyblid (6 km along strike) open-bay lithofacies dominate the lower part of the 32.5 m thick succession below an 8.5 m thick capping of tidal sandflat lihofacies (Supplimentary Figure S1).

A circa 60 m thick mid-Pridoli estuarine valley fill sequence is documented by the FEF in Pembrokeshire (Hillier et al. Reference Hillier, Marriott, Higgs and Howells2019). Here, valleys were cut into early ORS alluvium with a NW-SE orientation, and there is evidence of some structural control to their location (Figure 3d). The estuarine valley fills are preserved above lowstand coarse-grained alluvium. However, there is no clear evidence of structural control to the location of the PALF Incised Valley System. The possible superposition of mid-Pridoli and early Pridoli hiatuses in this western region has been alluded to (Figure 1). Any impact of the younger event remains unrecognized in easterly wholly red bed MCF successions. There, elevated rates of subsidence were perhaps a factor in minimising its impacts, with one of the abundant calcretized levels present in this succession marking its local manifestation.

6.g. Role of regional tectonism

The tectonism that had been so influential in achieving the Gorstian reconfiguration of the Welsh Basin remained a factor during the Ludfordian as many of the region’s deep-seated fracture lines responded to continuing transtension. The WBFS, and the Church Stretton Fault Zone in particular, exercised a significant control on the thickness and distribution of lithofacies. The thinner, more carbonate-rich Ludfordian successions present to the east of this fault belt contrast with the much thicker successions that drape it to the west and that host lithofacies, deeper in aspect, which had closer affinities to those of the Clun Forest Sub-Basin (Figure 3a). The Midland Platform evidently remained a structurally positive setting and a region of low accommodation space, at least during the early Ludfordian, that was remote from coarse fraction, siliciclastic input. This contrasted with the pattern of Ludfordian deposition to the west of the Church Stretton Fault Zone. There, following an initial seeding on an active Golden Grove Axis, the subsequent pattern of TilF deposition suggests that an actively subsiding marine trough – the terminal phase of the Clun Forest Sub-Basin – was effective in creating space to accommodate separate episodes of north-westerly sourced delta expansion.

During the Pridoli, though the Clun Forest Sub-Basin was by then no longer a site of deeper facies accumulation, ongoing subsidence may have influenced the position of river channels supplying the south-westward prograding DCSF delta. In so doing, it favoured the development in the Clun Forest area of steep delta-front clinoforms and of gradients necessary to generate mass flow and hyperpycnal deposits (e.g. Olariu et al. Reference Olariu, Steel and Petter2010).

Anomalous features associated with the Church Stretton Fault Zone emphasize the active nature of this fracture belt. The canyon/slump features of the Leintwardine region, though located to the east of the fault belt, likely migrated eastwards from the vicinity of the fault belt in response to headward erosion and/or retrograde, perhaps seismically triggered slumping. Either mechanism implies the presence in early Ludfordian times of a west-facing slope located seaward of an active fault footwall (see Whitaker, Reference Whitaker1962, Reference Whitaker1994; Cave & Hains, Reference Cave and Hains2001). Thickness variations associated with the Gorsley Axis (e.g. Holland & Lawson, Reference Holland and Lawson1963) indicate that Ludfordian tectonism was also locally influential on the Midland Platform. The subsequent impacts of early Pridoli structural inversion and the active roles played by the Church Stretton Fault Zone, the Neath Disturbance and the Malvern Axis have been outlined above.

In the south-eastern region, movements on the NW-SE trending Gorsley Axis resulted in thinning and non-deposition in the Ludlow but thickening in the Pridoli. This can be explained by viewing the footwall region of the Glasshouse Fault first as a seeding point and then as a site that anchored the CMSF barrier and promoted its in situ aggradation. The footwall region to the NE of the fault trace suffered differential uplift with the amount of accommodation space varying through time from Ludlow to Pridoli as recognized by Lawson (Reference Lawson1955). Butler et al. (Reference Butler, Woodcock and Stewart1997) recognize the NW-SE trending Woolhope Fault as an important and influential fracture which experienced reversals of movement at different stages in its history. It may serve to view the Glasshouse and Woolhope faults as individual components of a NW-SE trending Woolhope Fault Belt that acted as transfer structures between the Neath Disturbance and Malvern Line/Severn Estuary Fault Zone with the Gorsley Axis its stratigraphical expression. The role of the latter clearly compared with that of the Golden Grove Axis early in the Leintwardinian.

6.h. Variscan versus Caledonian affinities

The Middle Devonian deformation that affected the older fill of the Welsh Basin as well as its successor deposits – commonly ascribed to the ‘Acadian Orogeny’ – has long been viewed as a late Caledonian event (see Section 2). Woodcock et al. (Reference Woodcock, Soper and Strachan2007; also Woodcock & Soper, Reference Woodcock, Soper, Brenchley and Rawson2006; Woodcock, Reference Woodcock, Woodcock and Strachan2012a) reject this assertion. They argue compellingly that this deformation was the consequence of flat-slab subduction that took place along the northern margin of the Rheic Ocean and was by inference a proto-Variscan event. But at which point did plate processes associated with the Rheic Ocean overtake those of Iapetan affinity as the dominant tectonic influence on Wales and the adjoining regions of England? The complex interplay of tectono-sedimentary events associated with the closure of the Iapetus Ocean and the convergence of its contiguous continental masses are reviewed by Woodcock (Reference Woodcock, Woodcock and Strachan2012c).

Early Silurian volcanic centres at Skomer and Tortworth were likely a by-product of Rheic subduction, whereas syn-orogenic feldspar and lithic-rich sand supplied to the Welsh Basin during the late Llandovery and early Wenlock was from tracts uplifted within Avalonia during the period of Iapetus closure (Woodcock et al. Reference Woodcock, Butler, Davies, Waters, Hesselbo and Parkinson1996; Davies et al. Reference Davies, Fletcher, Waters, Wilson, Woodhall and Zalasiewicz1997). Evidently, there was an extended period when emerging Variscan and late Caledonian influences operated side by side. Sediment was being shed southwards from uplifting tracts linked to the Iapetus collision zone by mid Wenlock times. Woodcock (Reference Woodcock, Woodcock and Strachan2012c) suggests that the foreland basins that accommodated this sediment were responding to regional transtension. He envisages strike-slip within the Caledonian Orogen as the mechanism driving the development of such basins. The basins in northern England and North Wales, he suggests, evolved separately from a remnant Ludlow marine basin in Wales that continued to receive sediment from an emergent region to the south. In contrast, Hillier et al. (Reference Hillier, Marriott, Higgs and Howells2019) invoke partial uplift and the development on an extensive Gorstian pediment plain covering much of north and west Wales, as key factor in the evolution of the region. The findings of the current study show clearly that subsequent Ludfordian marine, deltaic, coastal plain and alluvial facies belts formed part of a southward advancing sedimentary system and that emergent tracts to the south had by then subsided and been submerged.

The age of the youngest shallow marine Ludlow facies preserved in North Wales, the uncleaved Dinas Brȃn Formation of the Llangollen area, is poorly constrained, and at youngest early Whitcliffian in age (see Warren et al. Reference Warren, Price, Nutt and Smith1984; Cocks et al. Reference Cocks, Holland and Rickards1992; Siveter, Reference Siveter2000). These strata do not preclude the possibility that, throughout much of west and North Wales, red bed ORS facies of late Ludfordian age formed part of the sedimentary overburden that facilitated the development of the Acadian cleavage in underlying Early Palaeozoic mudrocks (Soper & Woodcock, Reference Soper and Woodcock2003; Woodcock & Soper, Reference Woodcock, Soper, Brenchley and Rawson2006). The isolated ORS succession on Anglesey is normally listed as Pridoli to Early Devonian in age, but its deformation implies that it formed part of a once much thicker ORS succession (Treagus et al. Reference Treagus, Treagus and Woodcock2011). Perhaps, in common with the unconformable succession in south-west Wales, it too includes a Ludfordian component. The sediment supplied to both areas was derived from both local and distant Caledonian sources. However, in place of a pediment surface, the Anglesey succession records the burial of an incised local topography developed astride the site of the former Irish Sea Platform (or Monian Terrane) (Allen, Reference Allen1965). The marine facies and faunas developed southwards of this expanding ORS system were contiguous with those of the Rheic Ocean.

Such a model is at odds with the successions in northern England. There, marine conditions prevailed into the late Ludfordian and possibly early Pridoli during which time the terrestrial–marine interface lay to the north (Woodcock, Reference Woodcock, Woodcock and Strachan2012c). Such relationships speak to the complexity and diachroneity of Caledonian alluvial advance. They may also imply that the northern England and Welsh depocentres were widely separated at the time of sedimentation and that their current relative positions were imposed by sinistral displacements affecting the margin of the Monian Terrane during the late Early to Middle Devonian Acadian deformation.

In their re-assessment of the ‘Acadian Orogeny’, Woodcock et al. (Reference Woodcock, Soper and Strachan2007); Woodcock (Reference Woodcock, Woodcock and Strachan2012a) envisage a volcanic arc, later displaced along the Bristol Channel–Bray Fault Line, once to have existed in advance of the Rheic subduction zone. Back-arc extension affecting the ‘Avalonian’ crust to the north offers an alternative mechanism to generate the transtension needed in Wales to accommodate its Ludfordian to Early Devonian succession. There is no requirement for Caledonian effects to have fully ceased at this time, but the fundamental changes in provenance and subsidence patterns first evident during the late Gorstian can be seen to mark the point at which Rheic plate tectonics became dominant and Wales was more fully incorporated into an evolving Variscan orogenic province. The deposition and tectonic accommodation of late Gorstian–Early Devonian succession in Wales and the Welsh Borderland, as well as its subsequent deformation, uplift and erosion, were components, arguably, of the same proto-Variscan tectono-sedimentary cycle.

Finally, the juxtaposition of NW-sourced river-influenced with NE-sourced wave-influenced deltaic lithofacies associations across the Church Stretton Fault Zone in the region between Cae’r mynach and Llanstephan requires comment. Their current relationship appears difficult to explain by any passive sedimentological model and the suspicion is that it has been brought about by faulting. The WBFS has long been recognized as long-lived fracture belt that, at depth, may correspond to a significant terrane boundary in basement rocks (Woodcock & Gibbons, Reference Woodcock and Gibbons1988). Woodcock (Reference Woodcock1984) has provided evidence of post-depositional, dextral, strike-slip displacements affecting Ordovician rocks within the WBFS, and Hillier & Williams (Reference Hillier and Williams2004) speculated that Silurian intra-shelf basins were linked to dextral displacements along NE–SW trending faults. The distribution of early Pridoli lithofacies suggests that similar, post-depositional, right-lateral movements also account for the current proximity of deltaic facies produced by different processes along parts of the Church Stretton Fault Zone. For a plausible distribution of facies belts to be achieved, restoration of a displacement in excess of 10 km appears required.

The styles of deformation imposed on the rocks of Wales during the ‘Acadian Orogeny’ are widely acknowledged to reflect the impacts of sinistral transpression (e.g. Woodcock, Reference Woodcock, Woodcock and Strachan2012a; Woodcock et al. Reference Woodcock, Awan, Johnson, Mackie and Smith1988). Therefore, any dextral offset of Ludfordian facies belts along the Church Stretton Fault Zone must have been achieved before and/or after this deformation. Woodcock (Reference Woodcock, Woodcock and Strachan2012a) suggests that the driving influence on the tectonic development of the southern UK during the Early Devonian was a sinistral Caledonian strike-slip regime. In offering an alternative explanation, Rheic back-arc extension also provides a plausible mechanism to generate dextral displacements on the fundamental NE-SW fracture belts that traverse Wales. However, such early displacements would need to survive a predicted ‘Acadian’ reversal. Wilson et al. (Reference Wilson, Davies, Smith and Waters1988) recognize a comparable dextral displacement affecting Early Carboniferous rocks in South Wales along the similarly orientated Severn Estuary Fault Zone. They suggest that intra-Carboniferous movements on NE-SW-orientated faults may have occurred widely throughout Wales. Again, such dextral offsets may have been negated by the sinistral activity that accompanied the Late Carboniferous climax of the Variscan Orogeny (Corfield et al. Reference Corfield, Gawthorpe, Gege, Fraser and Besly1996; Davies et al. Reference Davies, Riley and Wilson2014). It is clear that the juxtaposition of Ludfordian lithofacies seen along the Church Stretton Fault Zone, if indeed the consequence of faulting, is the residual effect of several phases of movement, but the principal of which can all be viewed as Variscan in affinity.