Dubh Lochan, UK Dubh Lochan (56 9'N, 4 36'W, 75m above sea level) is a small lake (7.06 ha) on the eastern shore of Loch Lomond, Scotland (Stewart et al., 1984). The lochan is fed by a small intermittant stream during much of the spring and summer. There is an outflow to Loch Lomond. The lake is rather long and narrow, with a length of 550m and a mean breadth of only 128m. The maximum depth is 11.1m and the average depth is 4.8m and the catchment area is 110ha. The basin is underlain by schist and schistose grits metamorphosed during the Carboniferous from the Precambrian and Cambrian sedimentary rocks of the Dalradian series (Anderson, 1947). The lake appears to have been formed towards the end of the Younger Dryas, shortly after the disappearance of the Loch Lomond glacier (Stewart et al., 1984). The lake has a well-developed macrophyte flora, including Nuphar lutea, Nymphaea alba, Hippuris vulgaris, Equisetum fluviatile, Juncus bulbosus, Myriophyllum alterniflorum, Lobelia dortmanna, Fontinalis antipyretica, Littorella uniflora and Isoetes lacustris, with a fringe of Phragmites communis and Carex lutea. Carr is developed at the northern end of the lake. Two cores from the lake provide a sedimentary record covering the Holocene (Stewart et al., 1984). DLM is a 4.90m long core, taken in a water depth of 11m from the deepest part of the lake. Core DL is 6.00m long and was taken in an area Myrica-Sphagnum vegetation within the swamp and carr vegetation at the northern end of the lake. Changes in water depth are reconstructed from changes in lithology, sedimentation rates, aquatic pollen and macrophyte assemblages, and the occurrence of diatoms and sponge spicules. The diatom assemblages have not been described. The chronology is provided by five radiocarbon dates from core DLM and a single date spanning the rational limit of Corylus in a core immediately adjacent to core DL (Harkness, 1981). The base of core DL consists of sediments variously described as very fine plastic grey clay and fine grey silt. Stewart et al. (1984) suggest that this material is typical of inwashed sediments. The unit marks the initial formation of the lake, sometime before ca 9400 yr B.P. The absence of diatoms and the limited representation of aquatics and algae suggest that lake productivity was low. The overlying sediments in core DL (5.75-5.95m) are clayey muds, containing diatoms. The presence of macrofossils of Carex, Cyperaceae and Sphagnum are consistent with a moderately shallow lake. The overlying unit in core DL (3.30-5.75m) consists of fine mud. Between 5.00-5.75m the aquatic macrofossil assemblage includes abundant Chara and Nitella, with Nymphaea, Potamogeton and Naias. This assemblage is consistent with a somewhat deeper and more productive lake than formerly, as is the abundance of diatoms and sponge spicules in the sediments. In the deep-water core DLM, this interval is represented by a sequence of mud gyttja (4.49-4.90m) and homogeneous muds (4.11-4.44m) separated by a band of thinly bedded clays (4.44- 4.49m). A sample from near the base of the gyttja (DLM 4.80-4.85m) is radiocarbon dated to 8709+510-480 yr B.P. (SRR-1221), and from within the homogeneous muds (DLM 4.20-4.25m) to 5909+170 yr B.P. (SRR- 1220). The absence of aquatic pollen in the mud gyttja is consistent with moderately deep water. The thinly- bedded clays may represent a short-lived erosion episode, particularly as they are associated with an increased in unidentifiable pollen grains, but the preservation of laminations indicates anoxic conditions and suggests that the water remained moderately deep. The evidence from both cores, then, suggests moderately deep water conditions from ca 9000 yr B.P until ca 5800 yr B.P. The aquatic pollen assemblage in the uppermost part of the fine mud (DL 3.30-5.00m) is characterised by extremely abundant Isoetes, with values generally between 10-40% and peak values of 60%, a shift consistent with decreased water depth. The macrofossil assemblages contain megaspores of Isoetes, statoblasts of Cristatella mucedo and detrital remnants of terrestrial mosses. Cristatella mucedo is generally found attached to macrophytic vegetation and is characteristic of water depths of ca 1-2m (Berglund and Digerfeldt, 1970). The abundance of terrestrial moss fragments is variable but particularly abundant between 4.50-5.00m and again above 3.50m, and suggests considerable erosion input to the lake. The record suggests an initial shallow phase, a moderate increase in water depth, followed by a return to shallower conditions. The sedimentary record from core DLM is consistent with this pattern. The sediments between 3.83-4.08m are banded muds and clays. This unit is overlain by mud gyttja (2.65-3.83m). The basal part of this unit (3.00-3.83m) is devoid of aquatic pollen, consistent with moderately deep water between 5580 and 4920 yr B.P. Above 3.00m there is moderately abundant Isoetes pollen and some Sphagnum, which suggests shallowing after ca 4920 yr B.P. The sediments in the uppermost part of core DL consist of a sequence of cohesive detritus (3.02-3.30m), non- cohesive detritus (2.50-3.02m), humified peat (2.30-2.50m) and coarse peat (0.00-2.30m). Stewart et al. (1984) interpret this as indicating progressive shallowing consequent upon hydroseral development at the marginal core site. The biostratigraphic data are consistent with shallowing. Diatoms gradually become less abundant upcore, and are absent from the peats. Isoetes also declines in abundance and is absent from the uppermost part of the detritus and the peats. C. mucedo is absent from the uppermost 1m of the peat. In core DLM the last ca 4400 yr are represented by organic muds (0.10-2.57m). Changes in the aquatic pollen assemblages may indicate slight changes in water depth during this time. Below 1.80m the assemblages are characterised by decreased abundance of Isoetes, and the presence of Potamogeton, Pediastrum and Nymphaea, suggesting a moderate increase in water depth. The disappearance of Potamogeton and Pediastrum after ca 3710 yr B.P. and the reappearance of Isoetes after ca 1500 yr B.P. suggests a progressive shallowing and may reflect the hydroseral development around the margin of the lake. In the status coding, low (1) is indicated by clayey mud in core DL and a macrofossil assemblage with Carex, Cyperaceace and Sphagnum; intermediate (2) by organic mud in core DLM with moderate or abundant Isoetes and no Pediastrum or Potamogeton, or intervals with abundant terrestrial moss in core DL; high (3) by fine muds in DLM with deepwater aquatics including Potamogeton and Pediastrum; very high (4) by mud or mud gyttja, devoid of aquatic pollen, in core DLM, and fine muds with Potamogeton, Nymphaea, Chara and Pediastrum in core DL. References Anderson, J.G.C., 1947. The geology of the Highland Border: Stonehaven to Arran. Transactions of the Royal Society of Edinburgh 61: 479-515. Berglund, B.E. and Digerfeldt, G., 1970. A palaeoecological study of the Late-Glacial lake at Torreberga, Scania, South Sweden. OIKOS 21: 98-128. Harkness, D.D., 1981. Scottish University research and reactor centre radiocarbon measurements IV. Radiocarbon 23: 252-304. Stewart, D.A., Walker, A. and Dickson, J.H., 1984. Pollen diagrams from Dubh Lochan, near Loch Lomond. New Phytologist 98: 531-549. Radiocarbon Dates SRR-1217 917±105 0.41-0.46m, organic mud, core DLM SRR-1218 2707±70 1.45-1.50m, organic mud, core DLM SRR-1219 4913±85 3.00-3.05m, mud gyttja, core DLM SRR-1220 5909±170 4.20-4.25m, homogeneous muds SRR-1221 8709±510 4.80-4.85m, mud gyttja, core DLM -480 SRR-984 9360±70 6m, diatomaceous mud, adjacent to core DLM Coding -9400 yr B.P. lake forms, (1) 9400-9000 yr B.P. low (1) 9000-5800 yr B.P. very high (4) 5800-5580 yr B.P. intermediate (2) 5580-4920 yr B.P very high (4) 4920-4400 yr B.P. intermediate (2) 4400-3710 yr B.P. high (3) 3710-1500 yr B.P. intermediate (2) 1500- 0 yr B.P. intermediate (2) Preliminary coding: 11th June 1992; Final coding: 21st July 1993 Coded by SPH and GY Ellesmere, UK Ellesmere (52.9 N, 2.90 W, ca 80m above sea level) is one of a group of ca fifty small, mostly eutrophic, lowland lakes in the north west part of the English Midlands. The lake lies in glacial drift. The area was deglaciated between 10,000 and 12,000 years ago (Farr et al., 1990; O'Sullivan, 1990). Archaeological evidence shows that the water level was several metres higher than the today during the Iron Age (Hamlin, 1988; Farr et al., 1990). Three cores, a 4.3m-long Livingstone core, a 1m-long Mackereth core and a 30cm-long frozen core, taken from the deepest part of the lake, provide a sedimentary record back to ca 2200 years (Farr et al., 1990; O'Sullivan, 1990). Changes in lake depth are based on changes in lithology, laminae thickness, and diatom assemblages, and broadly follow those interpreted by Farr et al. (1990) and O'Sullivan (1990). The chronology is based on a single radiocarbon date and varve counting. The basal sediment (450-230m) is laminated clay, suggesting moderately deep water. Changes in laminae thickness and diatom abundance allow the unit to be subdivided. Between ca 450-400cm, the laminae are very thin (7-9 laminae per cm, mean 1.3 mm thick), suggesting deep water conditions. The lower boundary is dated to around 2200 yr B.P. (Nelms, 1984). The top boundary has a radiocarbon date of 1190±60 yr B.P. (OxA-2373, 405cm). Between 400-230cm, the laminae become discontinuous. The disruption of the laminae suggests the water became shallower. The organic matter is less well preserved, which is consistent with shallow conditions. The clay is pink-brown in colour, indicating oxygenated water. Planktonic diatom species are present but are less abundant than in the lowermost part of this unit. Farr et al. (1990) and O'Sullivan (1990) interpret the changes in sediment colour and diatoms as reflecting shallower water. This interval is dated to ca 1190-680 yr B.P. The change to gelatinous finely laminated (1-2mm thick) mud (230-100cm), suggests an increased water depth after 680 yr B.P. The diatom assemblage includes planktonic species, such as Cyclotella spp. and Stephanodiscus rotula, consistent with deep water. O'Sullivan (1990) states this lacustrine mud was deposited in a calm, anoxic depositional environment. This unit is dated to ca 680-290 yr B.P. The overlying sediment (100-10cm) is mud. The absence of laminations suggests the lake became shallower. The diatom assemblage is characterised by planktonic species (Asterionella formosa and Aulacoseira granata), but an increase in Fragilaria spp. is consistent with decreased water depth. There is a layer of grey clay between 50-30cm. O'Sullivan (1990) states that this unit reflects lake-level changes caused by the construction of artificial islands in the late 18th and the early 19th centuries. The uppermost sediment (ca 10-0cm) is laminated mud. The laminations (ca 1-4mm thick) suggest an increase in water depth after ca 100 yr B.P. The diatom assemblage includes planktonic species, such as Stephanodiscus hantzschii and Asterionella formosa, consistent with deep water. In the status coding, low (1) is indicated by non-laminated mud or pink-brown clay with discontinuous laminations; intermediate (2) by laminated clay; high (3) by finely laminated mud with planktonic diatoms. The clay deposited in the late 18th and early 19th centuries as a result of human activity is not coded. References Farr, K.M., Jones, D.M., O'Sullivan, P.E., Eglinton, G., Tarling, D.H. and Hedges, R.E.M., 1990. Palaeolimnological studies of laminated sediments from the Shropshire-Cheshire meres. Hydrobiologia 214: 279-292. Hamlin, A.G., 1988. Ellesmere Historical Town Walk. The Ellesmere society, Ellesmere. 16pp. Nelms, R.J., 1984. Palaeolimnological Studies of Rostherne Mere and Ellesmere Mere. Ph.D thesis, CNAA (Liverpool Polytechnic.). O'Sullivan, P.E., 1990. Studies of varved sediments in the Shropshire-Cheshire meres, UK. In: Saarnisto, M. and Kahra, A. (eds), Geological Survey of Finland, Special Paper 14: 33-46. Radiocarbon date OxA-2373 1190±60 yr B.P. 405cm, clay. Coding ca 2200-1190 yr B.P. intermediate (2) ca 1190-680 yr B.P. low (1) ca 680-290 yr B.P. high (3) ca 290-100 yr B.P. low (1) ca 100-0 yr B.P. high (3) Preliminary coding: 14/5/1994; Final coding: 20/5/1995 Coded by GY and SPH Garten, UK Loch Garten (57 13'N, 3 42'W, 220m above sea level) is a drainage loch, situated within the valley of the River Spey near the border of the Cairngorm foothills (O'Sullivan, 1974). It is one of a series of lochs occupying a former river channel which extends parallel to the modern course of the Spey, from Loch an Eilein to Nethy Bridge, just north of Loch Garten, where it rejoins the river. The lake has an area of 65 ha and a maximum depth of 5m. The catchment area is ca 600ha. The catchment bedrock is Moine granulites with small granite intrusions (Birks, 1970). During glacial periods ice flowed along the Spey valley, resulting in the deposition of morainic material and boulder clay. The overlying soils are acid with mor humus accumulation (Birks, 1970). There are three cores (O'Sullivan, 1974, 1975): a 3m long Mackereth core taken in the deepest part of the lake beneath ca 5m of water (1971 core), and 2m long core taken from the same part of the lake (1974 core), and a 1.47m long core taken beneath 1.30m of water at the south end of the lake (1968 core). Detailed pollen analysis was carried out on the shallow-water core (1968) and on the shorter deepwater core (1974), and a more rudimentary analysis (to allow cross-correlation) on the long deepwater core (1971). Changes in water depth are reconstructed from changes in lithology, sedimentation rates and evidence for reworking of the terrestrial pollen (O'Sullivan, 1975 and Personal communication, 1984). The chronology is established by 3 radiocarbon dates from the 1971 core (O'Sullivan, 1974, 1975; Pearson and Pilcher, 1975). The sediments in the 1971 core consist of undifferentiated detrital mud. Samples from 2.50-2.60m and 2.70- 2.80m are radiocarbon dated to 5860+100 (UB-851) and 7585+335 (UB-852) yr B.P. respectively. The apparent sedimentation rate in the basal part of the core appears very low (0.01 cm/yr), suggesting there may have been an hiatus during the early Holocene (O'Sullivan, personal communication, 1984). An interval of decreased water depth is indicated by the occurrence of a sandy detrital mud layer between 1.90- 2.00m in the 1974 deepwater core. Pollen samples spanning the unit (top of pollen zone LG3) show abrupt changes in the terrestrial pollen sequence, with apparent declines or disappearances of some already established species and increases in species that were previously declining in abundance. These changes occur over adjacent pollen samples and so are unlikely to reflect changes in the actual vegetation cover. O'Sullivan (1975 and personal communication, 1984) suggests reworking as an explanation for the anomalies. Similar changes in terrestrial pollen are seen at the corresponding interval (LGE/LGD transition) in the 1968 shallow-water core. This interval of shallower water appears to correlate with the period of low sedimentation in the 1971 core. On the basis of the terrestrial pollen sequence, O'Sullivan (1975) places this interval of lowered water level between ca 8000 and 6600 yr B.P. In the status coding, low (1) is indicated by deposition of sandy detrital mud in the 1974 core, reworked pollen, and low apparent sedimentation rates in the 1971 deepwater core; high (2) is indicated by coarse detrital mud deposition and increased sedimentation rates. References Birks, H.H., 1970. Studies in the vegetational history of Scotland. Journal of Ecology 58: 827-846. O'Sullivan, P.E., 1974. Two Flandrian pollen diagrams from the east-central highlands of Scotland. Pollen et Spores 16: 33-57. O'Sullivan, P.E., 1975. Early and Middle-Flandrian pollen zonation in the Eastern Highlands of Scotland. Boreas 4: 197-207. O'Sullivan, P.E., 1984. Personal communication. Pearson, G.W. and Pilcher, J.R., 1975. Belfast radiocarbon dates VIII. Radiocarbon 17: 226-238. Radiocarbon Dates UB-850 3635±205 0.80-0.90m detritus mud 1971 deepwater core UB-851 5860±100 2.50-2.60m detritus mud 1971 deepwater core UB-852 7585±335 2.70-2.82m detritus mud 1971 deepwater core Coding ? -8000 yr B.P. high (2) 8000-6600 yr B.P. low (1) 6600-0 yr B.P. high (2) Preliminary coding: 3rd July 1992; Final coding: 14th July 1992 Coded by SPH Hockham Mere, UK Hockham Mere (52 30'N, 0 50'E, 33m above sea level) is the now-drained site of a former small (56 ha) lake in the eastern Breckland (Bennett, 1986). The site was occupied by a lake at least until Tudor times (Bennett, 1983), and appears to have been drained after 1737 A.D. (Mosby, 1935). Today, the site is mostly occupied by alder carr but there is an oligotrophic peat bog at the western end. The catchment area of the former lake was ca 380ha and the lake basin was quite shallow with a maximum depth of 11.8m (Bennett, 1983, 1986). There is no evidence of inflow streams, and the former lake appears to have been fed by direct precipitation and a subterranean spring at its western end (Godwin and Tallantire, 1951). There is an artificial channel from the basin eastwards towards the Breckles Drain. The catchment bedrock is Upper Chalk overlain by a variety of Pleistocene deposits (Bennett, 1983). Two types of till occur, a thin (0.5-2.0m) sand drift partly due to aeolian deposition under periglacial conditions (Watt et al., 1966), and a thick blue chalky till in the north and west. The soils around the lake are drained brown earths and podzols. Most of the inflow come from sandy layers in the drift rather than from chalk groundwater (Anon, 1975). The lake probably owes its origin to chalk solution and collapse of the overlying deposits (Bennett, 1983). Investigations of Hockham Mere have been carried out over the last five decades. There are at least four cores through the lake sediments (DB5, DB10, Hr and HM). A 9m-long core (DB5) from the centre of the lake and a 6m-long core (DB10) from the lake margin provide a sedimentary record covering the Holocene (Godwin and Tallantire, 1951). A more recent 5m-long core (Hr) from the centre of the lake covers the last 7500 yr B.P. (Sims, 1973, 1978). A 11.85m-long core (HM) drilled in deepest part of the basin covers the last 12,620 yr B.P. (Bennett, 1983). The original investigors recognized several intervals of lowered lake level at Hockham Mere. The presence of a wedge-shaped lense of coarse detritus in core DB10 (2.5-3.5m) and other marginal cores was interpreted by Godwin and Tallantire (1951) as evidence of reworking of marginal sediment consequent on shallowing. Godwin and Tallantire (1951) dated this shallow interval to the Late Boreal (ca 6600-7000 yr B.P.) and argued that the lake was ca 3m lower than its natural, pre-drainage level. Sims (1978) recognized two intervals of shallowing (around 6730±120 yr B.P. and 5830±90 yr B.P.) during which the lake sediment becomes coarser and the abundance of riparian or carr-dwelling species and Alnus increases, before the Ulmus decline at ca 5000 yr B.P. Our description of water depth changes broadly follows those reconstructed by previous authors, but provides a more detailed record from the site based on changes in lithology, sedimentary structure, aquatic pollen assemblages and the remains of aquatic plants. The chronology is based on 36 radiocarbon dates from core Hr (Sims, 1973 and 1978) and core HM (Bennett, 1983). The sedimentary sequence from all of the lake cores is basically the same. The lake deposits (below 11.85m in core HM and below 8.80m in core DB5 ) rest on coarse sand with flints and chalky pebbles. The onset of lacustrine sedimentation in the centre of the lake is marked by coarse sand with lake mud (8.75- 8.8m in core DB5) and sandy mud with sand layers (11.85-10.0m in core HM). Between 11.85-11.51m in core HM, the sediment is sandy mud, suggesting moderately deep water, ca 12,620- 11,160 yr B.P. The aquatic assemblage is characterised by Potamogeton, Myriophyllum spicatum, Myriophyllum alterniflorum and Sparganium erectum, consistent with moderately deep water. Between 11.51-11.44m, the sediment is coarse sandy lake mud with high inorganic content. The coarser nature of the sediment suggests decreased water depth ca 11,160-11,050 yr B.P. The aquatic pollen assemblage is characterised by Potamogeton, Typha latifolia and Menyanthes trifoliata. The presence of Typha and Menyanthes trifoliata is consistent with shallowing. Between 11.44-11.27m, the sediment is sandy and silty lake mud, suggesting somewhat increased depth ca 11,050-10,600 yr B.P. A decrease in Menyanthes trifoliata is consistent with deepening. There is a layer of banded moss fragments (11.27m in core HM, ca 10,600 yr B.P.), suggesting shallow water. Between 11.27-11.10m, the sediment is sandy mud. The return to sandy mud suggests increased water depth ca 10,600-9560 yr B.P. Aquatics decrease in abundance, but the presence of Chara and Nitella is consistent with increased depth. There is a layer of sand between 11.10-11.07m, suggesting a decrease in water depth ca 9560-9460 yr B.P. The overlying sediments are silty nekron mud in core DB5 (7.55-8.75m) and detritus lake mud in core HM (11.07-10.00m, ca 9460-8900 yr B.P.), suggesting increased water depth. The unit contains remains of submerged or floating aquatics, such as Naias marina, Potamogeton, Ceratophyllum demersum and Nymphaea alba, consistent with increased water depth. The overlying sediments are nekron mud in core DB5 (2.80-7.55m) and lake mud in core HM (10.0-3.0m, ca 8900-4990 yr B.P.). The decrease in the detrital content of the central core probably reflects deeper water conditions. Changes in the lithology and sedimentary structures of the marginal core and aquatic assemblages in the central core allow this unit to be sub-divided. The preservation of laminations in the lower part of this unit (core DB5: 7.05-7.55m) indicates deep water conditions. The aquatic assemblage in core HM is characterised by Chara, Nitella, Ceratophyllum demersum, Myriophyllum verticillatum and Potamogeton, consistent with relatively deep water. Shallower conditions are marked by a wedge-shaped lense of coarse detritus mud (core DB10: 2.5-3.5m). Godwin and Tallantire (1951) interpreted this as material reworked during an interval when the lake was lower. From the position of this unit in the marginal cores, they argued that the lake must have been ca 3m lower. In the centre of the lake, there is no sign of reworking but the sediment in core HM (4.8-5.2m) is slightly coarser, more highly humified and contains Sphagnum leaves (Bennett, 1983), consistent with shallowing. This interval is marked by coarse detritus mud deposition in core Hr (3.5-3.8m) and an increase in the detritus content in core DB5 (6.75-6.95m), again consistent with shallowing. The presence of abundant Typha latifolia, Menyanthes trifoliata and Nymphaea alba in core HM is also consistent with shallow conditions. The lake level presumably fell as low as the highest point of reworked materials, ca 3m lower than the present lake level (natural, pre-drainage level). Godwin and Tallantire (1951) dated this shallow interval to ca 6600-7000 yr B.P. Sims (1978) dated two samples from the coarser sediment in core Hr (3.8-3.9m and 3.5-3.6m) to 6730±120 yr B.P. (Q-1087, 3.77-3.94m) and 5830±90 yr B.P. (Q-1089, 3.520-3.640m). The shallowing interval between 4.8- 5.2m in core HM is radiocarbon-dated to ca 7050-6600 yr B.P. (Bennett, 1983). A return to lake mud/nekron mud in cores HM (above 4.8m), Hr (above 3.5m) and DB5 (above 3.62m), reflects an increase in water depth after 6600 yr B.P. The aquatic assemblage in core HM is characterised by Chara, Potamogeton, Myriophyllum spicatum and Nymphaea, consistent with deep water. Laminated nekron mud is represented in core DB5 (3.5-3.62m), consistent with increased depth. The overlying unit is detritus lake mud (0.85-3.0m in core HM, 0.90-2.3m in core Hr, 1.0-2.8m in core DB5 and 1.02-2.0m in core DB10), suggesting decreased water depth, ca 4990-1150 yr B.P. The disappearance of lamination from core DB5 reflects shallowing. The aquatic assemblage in core HM is characterised by Sparganium, Typha latifolia (3.42-1.5m) and Polygonum, Menyanthes, Ranunculus (1.5-1.0m). The presence of Typha, Menyanthes and Ranunculus is consistent with rather shallow water. The uppermost sediment is Carex peat and oligotrophic peat (above 0.85m in core HM, 0.9m in core Hr and 1.0m in cores DB5 and DB10), probably reflecting hydroseral development in the basin after ca 1150 yr B.P. In the status coding: very low (1) is indicated by sand layer or moss layer in the centre of the lake; low (2) by wedge-shaped coarse mud with reworked matrix in the lake margin and coarse lake mud in the centre; moderately low (3) by coarse sandy lake mud in the centre, with Typha and Menyanthes; intermediate (4) by sandy/silty mud in the centre, with Potamogeton and Myriophyllum; moderately high (5) by detritus lake mud/nekron mud both in the margin and in the centre; high (6) by lake mud in the margin and laminated nekron mud in the centre, with Chara, Nitella, Myriophyllum and Potamogeton. Peat deposition after 1150 yr B.P. is considered to reflect hydroseral development, and is coded accordingly. Radiocarbon dates Q-1093 734±30 coarse detritus lake mud, 0.520-0.620m, Core Hr Q-1090 1145±30 coarse detritus lake mud, 0.800-0.900m, Core Hr Q-2225 1625±45 coarse detritus lake mud, 1.295-1.346m, Core HM Q-1091 1929±35 coarse detritus lake mud, 1.100-1.200m, Core Hr Q-2224 1980±50 coarse detritus lake mud, 2.575-2.625m, Core HM Q-2223 2660±50 coarse detritus lake mud, 2.895-2.945m, Core HM Q-1094 3020±45 coarse detritus lake mud, 1.700-1.800m, Core Hr Q-1095 3910±55 coarse detritus lake mud, 2.100-2.200m, Core Hr Q-2222 4500±100 detritus lake mud, 3.410-3.465m, Core HM Q-1045 4585±120 detritus lake mud, 2.650-2.740m, Core Hr Q-1046 4750±115 detritus lake mud, 2.810-2.829m, Core Hr Q-1047 4794±115 detritus lake mud, 2.900-2.980m, Core Hr Q-1048 4986±115 detritus lake mud, 3.000-3.080m, Core Hr Q-1049 5210±120 detritus lake mud, 3.160-3.240m, Core Hr Q-1089 5830±90 fine detritus lake mud, 3.520-3.640m, Core Hr Q-2221 6010±100 fine detritus lake mud, 4.259-4.345m, Core HM Q-1087 6730±120 fine detritus lake mud, 3.770-3.940m, Core Hr Q-2220 7080±60 fine detritus lake mud, 5.010-5.060m, Core HM Q-2219 7280±75 fine detritus lake mud, 5.295-5.345m, Core HM Q-1088 7447±125 fine detritus lake mud, 4.320-4.480m, Core Hr Q-2218 7505±90 lake mud, 6.059-6.145m, Core HM Q-2217 8230±150 lake mud, 6.735-6.785m, Core HM Q-2216 8250±80 lake mud, 7.695-7.745m, Core HM Q-2215 8500±80 lake mud, 8.175-8.225m, Core HM Q-2214 8675±60 lake mud, 9.375-9.425m, Core HM Q-2213 8960±95 lake mud, 9.775-9.825m, Core HM Q-2212 9040±110 lake mud, 10.25-10.305m, Core HM Q-2211 9110±115 lake mud, 10.635-10.705m, Core HM Q-2210 9130±600 lake mud, 10.815-10.875m, Core HM Q-2209 9270±150 lake mud, 10.915-10.965m, Core HM Q-2208 9390±140 lake mud, 11.000-11.040m, Core HM Q-2207 9460±100 lake mud, 11.040-11.080m, Core HM Q-2206 9560±95 coarse sandy lake mud, 11.115-11.165m, Core HM Q-2205 10820±900 coarse sandy lake mud, 11.295-11.350m, Core HM Q-2204 11160±190 coarse sandy lake mud, 11.530-11.585m, Core HM Q-2203 12620±85 coarse sandy lake mud, 11.775-11.825m, Core HM References Anon, 1975. Report on a hydrogeological investigation at Cranberry Rough. Anglian Water Authority, Great River Ouse Division. Bennett, K.D., 1983. Devensian Late-glacial and Flandrian vegetational history at Hockham Mere, England. New Phytologist 95: 457-487. Godwin, H. and Tallantire, P.A., 1951. Studies in the post-glacial history of Britain vegetation. Journal of Ecology 39: 285-307. Mosby, J., 1935. Hockham Mere. Transactions of the Norfolk and Norwich Naturalists Society 14: 61-67. Sims, R.E., 1973. The anthropogenic factor in East Anglia vegetational history: an approach using APF techniques. In: Birks, H.J.B. and West, R.G. (eds), Quaternary Plant Ecology, Blackwell Science. Oxford. Sims, R.E., 1978. Man and vegetation in Norfolk. In: Limbrey, S. and Evans, J.G. (eds), The Effect Of Man On The Landscape: The Lowland Zone. Council of British Archaeology Report 21: 57-62. Watt, A.S., Perrin, R.M.S. and West, R.G., 1966. Patterned ground in Breckland: Structure and composition. Journal of Ecology 54: 239-258. Coding 12,620-11,160 yr B.P. intermediate (4) 11,160-11,050 yr B.P. moderately low (3) 11,050-10,600 yr B.P. intermediate (4) 10,600 yr B.P. very low (1) 10,600-9560 yr B.P. intermediate (4) 9560- 9460 yr B.P. very low (1) 9460- 8900 yr B.P. moderately high (5) 8900- 6730 yr B.P. high (6) 7050- 5830 yr B.P. low (2) 6600- 4990 yr B.P. high (6) 4990- 1150 yr B.P. moderately high (5) 1150- 0 yr B.P. infilling, coded as moderately high (5) Preliminary coding: 7/3/1993; Final coding: 27/7/1994 Coded by GY and SPH Hornsea Old Mere, UK Hornsea Old Mere (53 50'N, 0 06'W, 1m above sea level) lies just above high tide level on the coast of eastern Holderness, England. It is a dry depression but was a lake before it was breached by coastal erosion ca 2000 yr B.P. (Beckett, 1975; 1981). The lake would have been up to 300m wide and at least 500m long (Beckett, 1981), with an area of ca 15ha. The former lake occupied the eastern end of a pre-glacial valley. A large (area ca 200ha) extant mere, known as Hornsea Mere, lies to the west of Hornsea Old Mere. The two sub-basins are separated by a low gravel ridge. However, the Steam Dike drains from Hornsea Mere through this ridge and across the former lakebed of Hornsea Old Mere. A terrace 3m above the modern level of Hornsea Mere indicates an earlier highstand. At this elevation, Hornsea Mere and Hornsea Old Mere would have been joined to form a single large lake (Reid, 1885). The bedrock in the catchment is chalk (Valentin, 1957), covered by till from the last glaciation (Devensian Withernsea Till, before 13,000 yr B.P.). A transect of borings across the basin provides a 14m composite sedimentary record back to before 10,000 yr B.P. (Beckett, 1981). Changes in water depth are reconstructed from changes in lithology and aquatic pollen assemblages, and broadly follow those described by Beckett (1981). The Holocene chronology is based on pollen correlation with nearly radiocarbon-dated sites: Roos, ca 2km northwest (Beckett, 1975); Gransmoor Quarry, North Holderness (Beckett, 1975) and North Ferriby (Wright and Churchill, 1965). The pre-Holocene chronology is uncertain because pollen is sparse and poorly preserved. The basal sediment (1380-1260cm) is gravelly clay. These are probably glacial deposits. Between 1260-1230cm, there is clayey fine detritus mud with silt, suggesting shallow water. The unit has sparse pollen. The overlying sediment (1230-930cm) is pinkish grey clay with occasional bands and slight organic matter, suggesting increased water depth. Above 950cm, the aquatic assemblage is characterised by Myriophyllum and abundant Sphagnum, consistent with deeper water. The upper part of unit belongs to pollen zone HO1 (945-895cm, after 10120 yr B.P.). The overlying sediment is fine detritus mud (930-175cm), suggesting moderately deep water. Changes in the aquatic pollen assemblages allow this unit to be subdivided. The lower part of the unit (930-540cm) contains sparse aquatic pollen with only Myriophyllum and Sparganium. Beckett (1981) considers the absence of submerged and floating-leaved macrophytes as indicating a water depth in excess of 7.5m. This interval belongs to pollen zones HO1 and HO2 (945-755cm, ca 10,120- 8507 yr B.P.) and HO3 (755-440cm, ca 8507-5099 yr B.P.), and is dated to ca 9990-5200 yr B.P. The aquatic assemblage between 540-175cm is characterised by an increase in Sparganium and the presence of Typha, Nymphaea, Potamogeton and Polygonum. Beckett (1981) suggests the increase in aquatic pollen indicates shallow water. This subunit belongs to pollen zone HO4 (440-255cm, ca 5099-3400 yr B.P.) and HO5 (255-155cm, after ca 3400 yr B.P.), and is dated to ca 5200-2300 yr B.P. The overlying sediment is clayey detritus mud (175-140cm), suggesting increased water depth. The aquatic assemblage is characterised by Sparganium, Lemna and Myriophyllum, consistent with increased depth. This unit is dated to ca 1900-2300 yr B.P. The topmost sediment is sandy clay (above 140cm). The presence of sand is thought to reflect inputs of dune sand as the result of coastal encroachment. Eventually, the Old Mere was breached and drained (Beckett, 1981). In the status coding: low (1) is indicated by fine detritus mud with abundant Sparganium and presence of Typha, Nymphaea, Potamogeton and Polygonum; intermediate (2) by fine detritus mud or clayey detritus mud with Sparganium and Myriophyllum; high (3) by pinkish grey clay with Myriophyllum. The deposit of sandy clay after ca 1900 is a result of coastal erosion, and is not coded. Radiocarbon dates Birm-405 10,120±180 yr B.P. correlated pollen zone HO1, Roos. SRR-230 8507±55 yr B.P. correlated pollen zone HO2, Gransmoor Quarry. SRR-229 5099±50 yr B.P. correlated pollen zone HO3, Gransmoor Quarry. Q-837 3433±110 yr B.P. correlated pollen zone HO5, Gransmoor Quarry. Q-715 3120±105 yr B.P. correlated pollen zone HO5, Gransmoor Quarry. References Beckett, S.C., 1975. The Late Quaternary Vegetational History of Holderness, Yorkshire. Ph.D thesis, University of Hull. Beckett, S.C., 1981. Pollen diagrams from Holderness, North Humberside. Journal of Biogeography 8: 177- 198. Reid, C., 1885. The geology of Holderness, and the adjoining parts of Yorkshire and Lincolnshire. Memoirs of the Geology Scurvy of London. Valentin, H., 1957. Glazialmorphologische untersuchungen in Ostengland. Abhandlungen Geographischen Institut, Universität Berlin: 1-86. Wright, E.V. and Churchill, D.M., 1965. The boats from North Ferriby, Yorkshire, England. Proceedings of Prehistory Society 31: 1-24. Coding pre 10,100-9900 yr B.P. high (3) ca 9900- 5200 yr B.P. intermediate (2) ca 5200-2300 yr B.P. low (1) ca 2300-1900 yr B.P. intermediate (2) ca 1900-0 yr B.P. not coded Preliminary coding: 17/3/1994; Final coding: 22/5/1994. Coded by GY and SPH Linton Loch, UK Linton Loch basin (55 52 'N, 2 37'W, 91.5m above sea level) is a former lake site, now a partially reclaimed marsh, at the northern edge of the Cheviot massif in the basin of the River Kale, a tributary of the River Teviot, which joins the River Tweed at Kelso (Mannion, 1978a). The marsh has an area of 12 ha. It is fed by several small streams, but there is no natural outflow. An artificial channel cuts through the centre of the marsh and drains to the River Kale. The present vegetation consists of open fen and marsh communities. There are two small areas of open water within the marsh. The underlying bedrock consists of Carboniferous basaltic lavas to the north, and andesitic lavas of Lower Old Red sandstone age to the south. Marls and conglomerates of Old Red Sandstone age occur to the west, in both the Teviot and Kale valleys, but these are downstream of the Linton Loch site. Superficial deposits within the basin consist of calcareous boulder clay. The stratigraphy of the site was reconstructed from 15 boreholes along four transects (Mannion, 1978a). Pollen analysis was conducted on two cores (Mannion, 1978a): a central core (core B) and a nearshore core (core A). Core A was also used for diatom and chemical analyses (Mannion, 1978b, 1981). The chronology is provided by pollen correlation with the radiocarbon-dated site of Din Moss (55 35'N, 2 20'W; Switsur and West, 1973; Hibbert and Switsur, 1976) which lies 3 km northeast of Linton Loch. The mid-Holocene lake-level changes at the site have been discussed by Mannion (1982). The basal deposits, exposed only in the more marginal cores, are gravels. In all but the most central of the cores (e.g. cores 3, 15, 16, 27), the gravels are overlain by clays. The clays show a tripartite division into lower blue (grey) clays, pink clays and upper blue clays. The blue clays are calcareous. Very little pollen is found in the clays and the organic content is low. On the basis of chemical analyses, in particular changes in the sodium and potassium content, Mannion (1978a) suggests the blue clay may represent a phase of algal activity because sodium and potassium content is low, but calcium content is high, whereas the pink clay is characterised by high sodium and potassium ratios suggesting it was derived by erosion (Mannion, 1978b). The concentration of diatoms is very low. The assemblages are dominated by Fragilaria construens, F. construens var. venter and F. pinnata. Amphora spp., Cocconeis spp. and epiphytic Epithemia spp. are also recorded. The overlying unit is white or yellow marl, containing freshwater snail shells (Planorbis, Limnaea) and Chara and Plumatella. This marl deposition is thought to represent biogenic deposition in open-water (Mannion, 1982) though probably within the littoral zone. Increasing frequencies of Myriophyllum spicatum, Typha latifolia and Nuphar lutea reflect a decrease in water depth. The marl unit is not found in the cores from the centre of the basin (e.g. cores 3, 15, 16, 27) and its thickness varies from ca 90cm in the deepwater core B to ca 2.65m in the nearshore core A. The transition to marl deposition in core A is dated to ca 9825 yr B.P. The diatom assemblages at the base of the marl (5.20-5.80m in core A) are dominated by Fragilaria spp. but Epithemia spp. are more abundant than formerly consistent with shallowing. In the uppermost part of the marl Epithemia spp. are dominant and Fragilaria spp. are relatively scarce. Planktonic diatoms, including Cyclotella comta reach their greatest abundance during this interval. The overlying unit is a coarse detrital mud containing freshwater snail shells (Planorbis, Limnaea), indicating a further decrease in water level. The transition to this unit in core B is dated to ca 8450 yr B.P. However, marl continued to be deposited at the core A site for much longer and the transition to detrital mud did not occur until ca 7160 yr B.P. The erratic pollen concentration values towards the top of the detritus mud unit suggests fluctuating water levels, and the presence of a thin marl band within the unit in core A may indicate a short- lived increase in water depth ca 6850-6500 yr B.P. The diatom assemblages between 1.85-2.16m in core A are characterised by an increase in epiphytic species such as Cocconeis and Achnanthes. The overlying unit is a coarse detrital mud containing abundant terrestrial macrofossils (e.g. Corylus nuts) and wood fragments. This unit represents a continuation of the shallowing trend (Mannion, 1982). The reduction in abundance of aquatic pollen and Cyperaceae is consistent with this hypothesis. Further evidence of the lowering of water level is provided by the fact that in core B 80cm of detrital mud was deposited during pollen zone LB2 (ca 6500-5350 yr B.P.) while only 8 cm of sediment was deposited during the same interval in core A (Mannion, 1978a, 1982). The abrupt changes in terrestrial pollen assemblages in core A, which are not seen in core B, strongly suggest an hiatus in sedimentation (Mannion, 1982). The diatom assemblages are characterised by a reduction in frustule numbers, an abrupt reduction in the abundance of Cyclotella, a decline in Epithemia spp. and an increase in Fragilaria spp. Mannion (1978b, 1981) suggest that these changes are consistent with the palynological evidence of a reduction or hiatus in sedimentation. The overlying unit in the marginal cores is a fine detrital mud or diatomaceous gyttja, indicating a return to deeper water conditions. An increase in the aquatic pollen and Cyperaceae is consistent with deeper water. The increase in the concentration of diatom frustules is also consistent with increased depth. Fragilaria spp. are the overwhelmingly dominant group. The onset of fine detrital mud deposition in core B is dated to ca 4790 yr B.P. and, as might be expected, starts somewhat later at ca 3860 yr B.P. in core A. The uppermost unit in all cores is a fen peat. Peat overgrowth occurs first in the more marginal sites, and is dated to ca 1780 yr B.P. in core A and ca 900 yr B.P. in core B. The presence of peat is assumed to reflect hydroseral development and marginal infilling rather a drop in lake level after ca 900 yr B.P., and is coded accordingly. In the status coding, 0 indicats the potential hiatus in core A during pollen zone LA2; low (1) by coarse detritus mud deposition in both cores A and B or by recent peat deposition; intermediate (2) by coarse detritus mud with shells in both cores; moderately high (3) by coarse detritus mud deposition in core B and marl deposition in core A; high (4) by marl deposition in both cores, or by fine detrital mud (algal gyttja) deposition in core B with either coarse detrital gyttja or peat deposition in core A; very high (5) by fine detrital mud (diatomaceous gyttja) deposition. Note that the lake status during clay deposition seems uncertain and, as the dating is also unclear, no attempt has been made to code this interval. References Hibbert, F.A. and Switsur, V.R., 1976. Radiocarbon dating of Flandrian pollen zones in Wales and northern England. New Phytologist 77: 227-256. Mannion, A.M., 1978a. Late Quaternary deposits from Linton Loch, southeast Scotland. I. Absolute and relative pollen analyses of limnic sediments. Journal of Biogeography 5: 193-206. Mannion, A.M., 1978b. Late Quaternary deposits from Linton Loch, southeast Scotland. II. The diatom assemblage of a marl core. Journal of Biogeography 5: 301-318. Mannion, A.M., 1981. Chemical analyses of a marl core from S.E. Scotland. Chemosphere 10: 495-504. Mannion, A.M., 1982. Palynological evidence for lake-level changes during the Flandrian in Scotland. Transactions of the Botanical Society of Edinburgh 44: 13-18. Switsur, V.R. and West, R.G., 1973. University of Cambridge natural radiocarbon measurements, XII. Radiocarbon 15: 534-544. Radiocarbon dates from Din Moss Q-1062 5341+70 0.50-0.54m, Elm decline. LA2-LA3a boundary Q-1063 5392+70 0.54-0.58m, Elm decline. LA2-LA3a boundary Q-1064 5441+70 0.58-0.62m, Elm decline. LA2-LA3a boundary Q-1065 6008+100 1.06-1.10m Q-1066 6528+100 1.80-1.84m, Alnus rise. LA2-LA1c3 boundary Q-1067 6708+100 1.84-1.88m, 2nd Alnus rise. Q-1068 6778+100 1.88-1.92m, 2nd Alnus rise. Q-1069 6858+100 2.40-2.44m, 1st Alnus rise. Q-1070 7146+120 2.44-2.48m, 1st Alnus rise Q-1071 7360+140 2.48-2.52m, Alnus rise. LA1c3-LA1c2 boundary Q-1072 7670+150 2.86-2.90m. Q-1073 8684+170 3.18-3.22m, Corylus maximum Q-1074 8940+170 3.68-3.72m, Corylus rise. LA1c1-LA1b boundary Q-1075 9120+170 3.72-3.76m, Corylus rise. Q-1076 9275+170 3.76-3.80m, Corylus rise. Q-1077 9824+190 4.02-4.06m. LA1b-LA1a boundary Q-1078 10337+200 4.12-4.16m, Juniperus maximum Q-1080 12251+250 4.52-4.60m. Coding ca 9825-8500 yr B.P high (4) ca 8500-7160 yr B.P. moderately high (3) ca 7160-6850 yr B.P. intermediate (2) ca 6850-6500 yr B.P. moderately high (3) ca 6500-5350 yr B.P. potential hiatus (0) ca 5350-4790 yr B.P. low (1) ca 4790-3860 yr B.P. high (4) ca 3860-1780 yr B.P. very high (5) ca 1780- 0 yr B.P. high (4) Preliminary coding: 15th June 1992; Final coding: 14th July 1993 Coded by SPH Llangorse Lake, UK Llangorse Lake (51 57'N, 3 15'W, 155m above sea level) is the largest natural body of freshwater in southern Wales with an area of 153ha (Jones et al., 1978). The catchment area is 2170ha (Jones, 1984). The lake is predominantly shallow (average depth 2.6m) but there are two localised deeper troughs where the water depth exceeds 7m (maximum depth 7.8m). The major inflow is from the south via the Afon Llynfi; there are several small spring-fed streams debouching on the north and east shores, but these have only minimal flow in summer. The Afon Llynfi outflows from the lake northwards to join the River Wye. There are three cores from the lake (A, B and C), all taken within the two deep troughs. The short Mackereth cores (core B is 3.23m long and core C is 3.18m long) are described by Jones et al. (1978). These cores provide a record spanning the last ca 4000 years. A 12.35m core (core A) is described by Jones et al. (1985). This long core provides a record back to beyond 9000 years. Publications describing the lake's sedimentary history (Jones, 1978; Jones et al., 1978, 1985) have concentrated on describing the record of human impact and have not discussed water-level changes. Changes in water depth are reconstructed here from changes in sediment lithology, sedimentation rates, diatom assemblages and geochemistry. The chronology is based on nine radiocarbon dates on core A and one date on core B (Harkness and Wilson, 1974). The uppermost sediments in core A have also been dated using 210Pb. The basal deposits in core A (ca 10-12.35m) are laminated clays. The preservation of laminations indicates relatively deep, anoxic waters. The sediments between ca 9.75-10m are marl, suggesting a marked decrease in water depth. The overlying sediments (8.10-9.75m) are non-laminated clays, indicating an increase in water depth. Brief intervals of reduced water depth are indicated by thin marl bands at ca 9.00-9.10m and ca 9.15- 9.25m. The water level changes indicated by these basal units can not be reliably dated. The overlying sediments in core A (ca 4.0-8.10m) are organic (nekron) muds. A sample from near the base of the unit is radiocarbon dated to 8720+80 yr B.P. (SRR-2384). The sedimentation rate within the nekron mud is extremely variable. The lowest rates of sediment accumulation (0.02 cm/yr) occur between ca 8200 and 4200 yr B.P., suggesting that there may be an hiatus in sedimentation some time during this interval. Between 7.30 and 7.36m the nekron muds are lighter in colour, more compacted and contain a higher proportion of carbonate. These changes are consistent with a reduction in water depth or a possible hiatus. The increased sediment rates in the uppermost part of the unit (0.17 cm/yr, 0.48 cm/yr) are consistent with increased water depths after ca 4200 yr B.P. The radiocarbon sample from 6.04-6.14m (SRR-2381) is somewhat older than expected, which suggests slight contamination with older carbon. This would be consistent with sediment slumping or shoreline erosion consequent on rising water levels. Diatom analysis from the organic (nekron) muds in core C (2.3-3.25m) allows the unit to be subdivided. We assume the age of the nekron mud is synchronous across the basin. Radiocarbon samples from the transition from nekron mud to silty clays from core A and B have been dated at 1980+80 (SRR-2378) and 1790+60 yr B.P. (SRR-129) respectively. We use the sedimentation rate from the upper part of the nekron mud in the radiocarbon dated core A (0.05 cm/yr) to assign dates to the diatom subunits. The lowermost subunit (3.25- 3.0m) contains dominantly benthic (Fragilaria construens) diatoms, consistent with the lithological evidence, suggesting moderate water depth (ca 4200-2900 yr B.P.). Between 3.0-2.7m (ca 2900-2000 yr B.P.) there is an increase in planktonic taxa (Melosira granulata reaches 20%), and the assemblage contains some typical indicators of large lakes (such as Stephanodiscus astraea), while benthic taxa disappeared, suggesting that the lake became deeper than before. The top of sediments (0.0-4.0m in core A, 0-2.4m in core B and 0-2.7m in core C) are relatively inorganic, silty clays. These are thought to reflect increased erosion from the catchment, which Jones et al. (1978, 1985) attribute to increased human impact. However, there is no consistent change in heavy metal concentrations in the sediments across this transition (Jones, 1984) although heavy metal concentrations do show a pronounced increase in the recent (post ca 1840 A.D.). In core C (2.7-2.5m), planktonic diatoms decrease but keep moderately percentage (ca 5%). We interpret that the unit represent a relatively high water level after ca 1900 yr B.P. In the status coding, (0) indicates a possible hiatus; low (1) is indicated by nekron mud with high sedimentation rates and benthic diatoms dominant; intermediate (2) by nekron mud with planktonic diatoms and some taxa typical of large lakes; high (3) by silt clays with planktonic diatom. The record before 9000 yr B.P. is not coded because of difficulties in dating it. References Harkness, D. and Wilson, H., 1974. Scottish University research and reactor centre radiocarbon measurements II. Radiocarbon 16: 238-251. Jones, R., 1984. Heavy metals in the sediments of Llangorse Lake, Wales, since Celtic-Roman times. Verhandlungen Internationale Vereinigung Limnologie 22: 1377-1382. Jones, R., Benson-Evans, K. and Chambers, F.M., 1985. Human influence upon sedimentation in Llangorse Lake, Wales. Earth Surface Processes and Landforms 10: 227-235. Jones, R. and Benson-Evans, K., 1974. Nutrient and Phytoplankton studies of Llangorse Lake, a eutrophic lake in the Brecon Beacons National Park, Wales. Field Study 4: 61-75. Jones, R., Benson-Evans, K., Chambers, F.M., Seddon, B.A. and Tai, Y.C., 1978. Biological and chemical studies of sediments from Llangorse Lake, Wales. Verhandlungen Internationale Vereinigung Limnologie 20: 642-648. Radiocarbon Dates SRR-129 1790+60 clay/mud transition, 240-244cm, Core B SRR-2376 2530+90 silty clay, 302-311cm, Core A, ATO SRR-2377 2230+80 silty clay, 376-386cm, Core A, ATO SRR-2378 1980+80 clay/mud transition, 406-416cm, Core A SRR-2379 3080+80 organic nekron mud, 451-461cm, Core A SRR-2380 3240+70 organic nekron mud, 527-537cm, Core A SRR-2381 4380+80 organic nekron mud, 604-614cm, Core A SRR-2382 4140+80 organic nekron mud, 677-687cm, Core A SRR-2383 8150+90 organic nekron mud, 759-769cm, Core A SRR-2384 8720+80 organic nekron mud, 797-805cm, Core A Coding ?-8800 yr B.P. high (3) 8800-8200 yr B.P. low (1) 8200-4200 yr B.P. possible hiatus (0) 4200-2900 yr B.P. low (1) 2900-1900 yr B.P. intermediate (2) 1900-0 yr B.P. high (3) Preliminary coding: 5/8/1992; Final coding: 27/7/1993 Coded by: SPH and GY Llyn Clyd, UK Llyn Clyd (53 5'N, 4 10'W, 746.8m above sea level) is a mountain tarn in Snowdonia, North Wales. The tarn surface area is 0.65ha and the maximum depth is 6.1m. The lake is oligotrophic with a pH of around 6. The basin is a late glacial cirque (Seddon, 1957), occupied by ice until the early Holocene (Evans and Walker, 1977). The lake formed soon after the ice melted. The bedrock in the basin is Ordovician metamorphic rock. The height of the tarn was probably near or above the tree limit during maximum forest development in the Holocene and shows minimum interference from man (Evans and Walker, 1977). Three cores (216cm, 301.5cm and 316cm long respectively) were taken from the tarn (Evans and Walker, 1977). Typical late glacial deposits of clay-silt nekron-mud (Brown Mud) occur in all three cores, indicating that lacustrine deposition began in the early Holocene (Evans and Walker, 1977). Changes in the water depth are reconstructed from diatom assemblages, aquatics and sedimentation rate from core I. The chronology is based on pollen correlation with the nearby radiocarbon-dated site of Melynllyn (core 1), ca 10km northeast of Llyn Clyd (Walker, 1978). The basal nekron mud (220-180cm in core I) is marked by a diatom assemblage of Fragilaria brevistriata, together with benthic diatoms, such as Achnanthes minutissima, Navicula seminulum and Melosira distans. This mixed assemblage suggests moderately shallow water. The unit belongs to pollen zones Sn3 (below 210cm, 8800-7150 yr B.P.) and Sn4 (210-175cm, 7150-4650 yr B.P.) and can be dated to ca 7900-5010 yr B.P. In the middle part of nekron mud (180-95cm), the diatom assemblage is characterised by the dominance of Cyclotella comensis and a decrease in Fragilaria brevistriata. The dominance of planktonic diatoms suggests an increase in water depth. A relatively low sedimentation rate (0.014 cm/yr) is consistent with deep water. The unit belongs to pollen zone Sn5A (175-70cm, 4650-2150 yr B.P.) and can be dated to ca 5010-2880 yr B.P. The overlying unit (95-30cm) is dominated by Achnanthes minutissima var. cryptocephala. There is a marked decrease in Cyclotella comensis. The change in the diatom assemblage suggests shallower conditions (Evans and Walker, 1977). A peak of Sphagnum (90-70cm) is consistent with decreased water depth. An increase in sedimentation rate to 0.033 cm/yr is also consistent with shallow water. This unit belongs to the upper part of pollen zone Sn5A and Sn5B (0-70cm, after 2150 yr B.P.) and can be dated to after 2880 yr B.P. Changes in diatom assemblage above 30cm, in particular an increase in Cyclotella comensis and a decrease in epiphytic and benthic species (e.g. Achnanthes, Eunotia, Navicula), suggest that water depth has increased somewhat in recent years (ca 900 yr B.B. by sedimentation rate). In the status coding, low (1) is indicated by nekron mud with benthic diatom assemblage, abundant Sphagnum and high sedimentation rate; high (3) by nekron mud with planktonic diatom assemblage and low sedimentation rate. The present is coded as intermediate (2). Radiocarbon dates SRR-635 1625±90 yr B.P. pollen zone Sn5B, Melynllyn, core 1. SRR-636 2665±120 yr B.P. pollen zone Sn5A, Melynllyn, core 1. SRR-637 3422±110 yr B.P. pollen zone Sn 5A, Melynllyn, core 1. SRR-638 4755±90 yr B.P. pollen zone Sn5A/Sn4, Melynllyn, core 1. SRR-639 7378±160 yr B.P. pollen zone Sn4/Sn3, Melynllyn, core 1. References Evans, G.H. and Walker, R., 1977. The late Quaternary history of the diatom flora of Llyn Clyd and Llyn Glas, two small oligotrophic high mountain tarns in Snowdonia (Wales). New Phytologist 78: 221-236. Seddon, B., 1957. Late-glacial cwm glaciers in Wales. Journal of Glaciology 3: 94-98. Walker, R., 1978. Diatom and pollen studies of a sediment profile from Melynllyn, a mountain tarn in Snowdonia, North Wales. New Phytologist 81: 791-804. Coding ca 7900-5010 yr B.P. low (1) ca 5010-2880 yr B.P. high (3) ca 2880-900 yr B.P. low (1) ca 900-0 yr B.P. intermediate (2) Preliminary coding: 10/11/1993; Final coding: 26/9/1994 Coded by GY and SHP Melynllyn, UK Melynllyn (53 7'N, 4 7'W, 632.5m above sea level) is a deep mountain tarn in Snowdonia, North Wales. The tarn surface area is 7.36ha and the maximum water depth is 20m. The lake is oligotrophic with a pH of 6.2 and has a conductivity of only ca 30 µmho. The basin is a late-glacial cirque (Seddon, 1957). The lake formed ca 12,000-10,000 yr B.P. (Walker, 1978). The bedrock in the basin is Ordovician slates, shales and rhyolites. The lake level was artificially raised 1.5-2m in 1879 AD when the outflow was dammed so the lake could be used a reservoir. The dam was demolished in 1970 and the water returned to its natural level (Walker, 1978). Two cores (core 1, 522cm long from a water depth of 17m, and core 2, 415cm long from a water depth of 20m) provide a sedimentary record back to before 10,260 yr B.P. (Walker, 1978). Change in water depth is reconstructed from changes in lithology, laminated structures and diatom assemblages. Six samples from core 1 are radiocarbon-dated. They are generally consistent with the regional pollen chronology except for SRR-634 which is stratigraphically inverted (Walker, 1978). The chronology is based on the remaining five radiocarbon dates for the last 8800 radiocarbon years (pollen zones Sn5B-Sn3). The older part of the record (below pollen zone Sn3) is dated by pollen correlation with Scaleby Moss (Godwin et al., 1957; Godwin and Willis, 1959). The basal sediment is silty clay (481-522cm in core 1 and 395-415cm in core 2). Walker (1978) considers this is a glacial deposit. The overlying sediments are silty mud with macroscopic plant remains (460-481cm in core 1), suggesting shallow water conditions. The presence of Typha is consistent with shallow conditions. The diatom assemblage is characterised by dominance of epiphytes (Fragilaria brevistriata, Achnanthes minutissima and A. suchlandti), also consistent with shallow water. The abundance of Melosira italica in this unit suggests turbulent and organic water conditions, consistent with the lithological interpretation. This unit covers part of pollen zone Sn2 (481- 445cm in core 1, 10,260-8800 yr B.P.), and is dated to ca 10,260-9040 yr B.P. The overlying sediment is fine detritus mud with fine bands (460-428cm in core and 395-377cm in core 2). The occurrence of laminated sediments indicates an increase in water depth. Abundant Isoetes with some Sphagnum is present in this unit. An assemblage with Isoetes and Sphagnum and no other aquaticscharacterises the modern surface sediment in a water depth of ca 17m (Walker, 1978), so the presence of abundant Isoetes is consistent with deep water conditions. The diatom assemblage is characterised by a decrease in epiphytes (Achnanthes minutissima, Fragilaria brevistriata and Synedra rumpens) and an increase in benthics (Navicula spp., Anomoeoneis exilis and Cymbella spp.) and planktonics (Melosira distans, M. distans var. lirata), suggesting increased water depth. The decrease in species that like to live in turbulent and organic water (such as Melosira italica, Fragilaria brevistriata and Achnanthes minutissima), and increase in species that like to live in clear and inorganic water conditions (such as Cymbella cesati), is consistent with increased water depth. The unit covers the upper part of pollen zone Sn2 and the lower part of Sn3 (405-445cm in core 1, 8800-7150 yr B.P.), and is dated to ca 9040-7640 yr B.P. The overlying unit is unbanded fine detritus mud (350-428cm in core 1 and 306-377cm in core 2). The disappearance of laminae suggests decreased water depth. The diatom assemblage is characterised by an increase in Cyclotella kützingiana and decrease in Melosira distans. The increase in planktonic species which like a clear water and inorganic water conditions (Melosira distans) and decrease in planktonic species which like turbulent and organic water conditions (Cyclotella kützingiana) might imply a decreased water depth, consistent with the lithological interpretation. Samples from near the bottom and the top of this unit are radiocarbon-dated to 7378±160 yr B.P. (SRR-638, 410cm) and 4755±90 yr B.P. (SRR-638, 350cm) respectively. The overlying sediment is finely banded fine detritus mud (153-350cm in core 1 and 168-306cm in core 2). The reappearance of laminated structures suggests increased water depth. The presence of Myriophyllum and abundant Isoetes is consistent with deeper water. There is a marked increases in Melosira distans (300-250cm) and decrease in Cyclotella kützingiana (300-280cm) in core 1, supporting this interpretation. Three samples from this unit are radiocarbon-dated to 3422±110 yr B.P. (SRR-637, 290cm), 2665±120 yr B.P. (SRR-636, 230cm) and 1625±90 yr B.P. (SRR-635, 170cm) respectively. This unit is dated to ca 4760-1470 yr B.P. The topmost unit (above 153 cm in core 1 and 168cm in core 2) is fine detritus mud. The absence of laminations suggests decreased water depth. The diatom assemblage is characterised by an increase in Achnanthes minutissima, consistent with decreased water depth during the last ca 1470 years. In the status coding, low (1) is indicated by silty mud with epiphytic diatoms dominant, and the presence of Typha; intermediate (2) by unbanded fine detritus mud with dominance of benthic diatoms, or with decrease in planktonic diatoms which need turbulent and organic water conditions and increase in planktonic diatoms which need clear and inorganic water conditions; high (3) by finely banded fine detritus mud with highest abundance of planktonic diatoms, and with Myriophyllum and Isoetes. Radiocarbon dates SRR-635 1625±90 yr B.P. 170cm, fine detritus mud core 1. SRR-634 2062±60 yr B.P. 110cm, fine detritus mud core 1. Stratigraphically inverted. SRR-636 2665±120 yr B.P. 230cm, fine detritus mud core 1. SRR-637 3422±110 yr B.P. 290cm, fine detritus mud core 1. SRR-638 4755±90 yr B.P. 350cm, fine detritus mud core 1. SRR-639 7378±160 yr B.P. 410cm, fine detritus mud core 1. Q-151 10,264±350 yr B.P. pollen zone Sn1/Sn2, from Scaleby Moss. * * There is a slight discrepancy between the date (10,264±350 yr B.P.) as published in American Journal of Science Radiocarbon Supplement (Godwin and Willis, 1959), which we use here, and that (10,257 yr B.P.) cited by Walker (1978). References Seddon, B., 1957. Late-glacial cwm glaciers in Wales. Journal of Glaciology 3: 94-98. Walker, R., 1978. Diatom and pollen studies of a sediment profile from Melynllyn, a mountain tarn in Snowdonia, North Wales. New Phytologist 81: 791-804. Coding ca 10260-9040 yr B.P. low (1) ca 9040-7640 yr B.P. high (3) ca 7640-4760 yr B.P. intermediate (2) ca 4760-1470 yr B.P. high (3) ca 1470-0 yr B.P. intermediate (2) Preliminary coding: 13/3/1994; Final coding: 10/5/1994 Coded by GY, SPH and MYP Old Buckenham Mere, UK Old Buckenham Mere (52 30'N, 1 1'E, ca 35m above sea level) is a small mere (3ha in area) in the centre of a large fen (ca 32ha in area). There is a stream flowing into the fen from the north-east, which eventually drains westward via the main fen dyke (Tallantire, 1954). The fen is often partially flooded in winter and is probably also fed from subterranean springs (Tallantire, 1954). The fen has been subject to artificial drainage for at least 100 years (Bennett, 1884), but many of the drains are now overgrown. The basin is situated in an area of glacial outwash material and boulder clay (Tallantire, 1954). The underlying bedrock is mainly Upper Chalk. The soils are mostly calcareous. The gross stratigraphy of the lake deposits was reconstructed by Tallantire (1954) from a transect of 11 borings. The basal deposits, attributed to the late glacial on the basis of their terrestrial pollen assemblage, are calcareous lake muds grading into shelly calcareous lake muds towards the lake margin. These units are overlain by a relatively pure lake chalk, which grades upwards into a shell-marl. Lenses of fine detritus and traces of Cladium rhizomes are found within this unit. Tallantire (1954) suggests the lake chalk and shell-marl are evidence of lower water-level, at least seasonally, during the Late Boreal and Atlantic (pollen zone VI and VII). A return to deeper water conditions is indicated by the overlying unit, which is calcareous mud. This mud grades upward into a shelly calcareous mud containing more detritus. A more detailed pollen record covering the last ca 11000 years is provided by two borings from the centre of the basin (Godwin, 1967). Boring I is 9m long (50-950cm) and boring II is 3m long (-7m to -10m depth) (Godwin, 1967). There are no radiocarbon dates on these cores. The chronology is established by correlation with Hockham Mere, which is ca 15km away and has more than 30 radiocarbon dates (Sims, 1978; Bennett, 1983). The base of the sequence consists of chalk pebbles in a matrix of lake mud. In some place there is sand with flint pieces, suggesting quite shallow water in the initial phase of lacustrine sedimentation, before ca 10,500 yr B.P. The overlying sediment (900-908cm in boring I and 929-940cm in boring II) consists of slightly calcareous fine detritus lake mud, suggesting shallow water. It contains Chara fruits, abundant Equisetum, Menyanthes and Typha pollen, and a few small wood or bark fragments, consistent with shallow water. This unit was just before pollen zone V of Boreal and was dated to late glacial (Godwin, 1967), ca 10,500-10,000 yr B.P. The overlying sediment (844-924cm in boring I and 850-929cm in boring II) is clayey lake mud (gyttja). It has a banded structure with thin, dark streaks of organic material, which Godwin suggests those are probably reworked organic mud. The transition from calcareous fine detritus mud to clayey mud suggests increased water depth. The presence of reworked organic material is consistent with erosion consequent upon rising water level. This unit belongs to pollen zone V, ca 10,000-7000 yr B.P. The absence of sediments covering pollen zone V and VI from boring I indicates an hiatus in sedimentation at ca 844cm (ca 850cm in boring II) (Godwin, 1967). Since the core comes from the centre of the basin, this implies that the lake was very low. The missing pollen zones cover the interval between ca 6900 and 5850 yr B.P., although the lake was not necessarily low for the whole of this period. The overlying sediment (767-828cm in boring I and 790-850cm in boring II) is chalk mud, indicating a return to deeper water conditions after ca 5850 yr B.P. The overlying sediment (700-767 in boring I and 650-790cm in boring II) is fine detritus lake mud. There are lenses of coarse detritus mud and traces of Naias rhizomes and Carex fruits, reflecting shallow conditions between ca 5000-4100 yr B.P. The overlying sediment (550-650cm in boring II) is nekron mud, suggesting the water became deeper. The aquatic assemblage is characterised by an increase in Potamogeton, Sparganium and Nuphar, consistent with deeper water. This unit is dated to 4100-3300 yr B.P. The overlying sediment (150-550cm in boring II) is fine detritus mud with shells, suggesting a decrease in water depth. The aquatic assemblage is characterised by an increase in Sparganium, Typha and Alisma, consistent with shallowing ca 3300-1000 yr B.P. The uppermost sediment (above 1.5m in boring II) is foetid mud, indicating the lake was closed and water not very deep during the last 1000 years. The surface sediments in the central part of the mere are fen peat with a floating reedmat of Phragmites, consistent with hydroseral development and infilling in the recent past. In the status coding: 0 indicates an hiatus; low (1) is indicated by calcareous fine detritus mud (with or without shells) and with shallow water aquatics such as Menyanthes/Alisma or traces of Naias rhizomes; intermediate (2) by clayey lake mud with reworked material or foetid mud; high (3) by chalk mud or nekron mud with increase in Nuphar, Myriophyllum and Potamogeton. References Bennett, F.G., 1884. Geological Memoirs (O.S.), Attleborough: Watton and Wymondham. Bennett, K.D., 1983. Devensian Late-glacial and Flandrian vegetational history at Hockham Mere, England. New Phytologist 95: 457-487. Godwin, H., 1967. Studies of the Post-glacial history of British vegetation, XV. Organic deposits of Old Buckenham Mere, Norfolk. New Phytologist 67: 95-107. Godwin, H., 1968. The development of Quaternary palynology in the British Isles. Review of Palaeobotany and Palynology 6: 9-20. Sims, R.E., 1978. Man and vegetation in Norfolk. in: Limbrey, S. and Evans, J.G. (eds), The effect of man on the landscape: the lowland zone, Council of British Archaeology Report 21: 57-62. Tallantire, P.A., 1954. Old Buckenham Mere, Data for the study of Post-glacial history. New Phytologist 53: 131-139. Coding ca 10,500-10,000 yr B.P. low (1) ca 10,000-6900 yr B.P. intermediate (2) ca 6900- 5850 yr B.P. hiatus (0) ca 5850- 5000 yr B.P. high (3) ca 5000- 4100 yr B.P. low (1) ca 4100- 3300 yr B.P. high (3) ca 3300- 1000 yr B.P. low (1) ca 1000- 0 yr B.P. high (3) Preliminary coding 10/3/1993; Final coding: 22/5/1994 Coded by GY and SPH Pityoulish, UK Loch Pityoulish (57 12'N, 3 48'W, 210m above sea level) is a drainage loch, situated within the valley of the River Spey near the border of the Cairngorm foothills, Scotland (O'Sullivan, 1976). It is one of a series of lochs occupying a former river channel which extends parallel to the modern course of the Spey, from Loch an Eilein to Nethy Bridge, just north of Loch Garten, where it rejoins the river. There is a single inflow into the loch from the south and an outflow northwards. However the loch also receives direct drainage from the steep surrounding slopes, particularly from Creag Pityoulish to the east. The lake has an area of 40 ha and reaches a maximum depth of 20m at the north end. The area of the drainage basin is about 600ha. The catchment bedrock is Moine granulites with small granite intrusions (Birks, 1970). During glacial periods ice flowed along the Spey valley, resulting in the deposition of morainic material and boulder clay. The overlying soils are acid, with mor humus accumulation (Birks, 1970). Two 6m long cores (A and B) from the deepest part of the lake provide a stratigraphic record back to the Late Devensian (O'Sullivan, 1975, 1976). The top 3.05m of core A was used for pollen analysis and radiocarbon dating. Chemical analyses were carried out on core B. A short core of the uppermost sediments, including the mud-water interface, was also obtained. Changes in water depth are reconstructed from changes in stratigraphy, sedimentation rates and aquatic pollen assemblages. The chronology is provided by 8 radiocarbon dates (O'Sullivan, 1976; Harkness, 1981). The basal deposits are grey clay (2.67-2.76m), coarse sand (2.76-2.78m) and sandy clay (2.78-3.05m). These units are devoid of pollen and are presumed to be of late Devensian age (O'Sullivan, 1976). The transition to the overlying unit at 2.67m is extremely sharp. This is consistent with an hiatus in sedimentation prior to the onset of organic deposition in the basin. O'Sullivan (1976) suggests that this hiatus may have lasted between 500-1000 years. He also suggests an alternative explanation, namely that the loch was experiencing a level of throughflow at a rate too great to allow richly polliniferous sediments to accumulate. The overlying unit (1.75-2.67m) is a very dark and compact fine detritus mud. A series of four samples from the lower half of the unit provide radiocarbon dates in the range 5550 (SRR-459, ca 2.14-2.26m) to 8390 (SRR-572, 2.56-2.62m) yr B.P. The extremely low sedimentation rates (between 0.012-0.02 cm/yr) and the compact nature of the sediments suggests that sedimentation was sporadic, and is consistent with low and/or fluctuating water levels. The aquatic assemblage is consistent with low and/or fluctuating water levels, being characterised by low abundances of Cyperaceae and Equisetum and the sporadic occurrence of Potamogeton, Nymphaea, Isoetes and Myriophyllum. The sedimentation rate in the upper part of the unit is greater (0.26 cm/yr), and Isoetes becomes more abundant. These changes might indicate an increase in water depth or more stable conditions after ca 5550 yr B.P. O'Sullivan (1976) does not claim that the water depth at Loch Pityoulish was low during the early Holocene, but he does point out that other lakes in the region were low between ca 8000-6650 yr B.P. The overlying unit (0.72-1.75m) is a medium detritus mud. A sample from the transition to this unit (1.70- 1.80m) is radiocarbon dated to 3800+60 yr B.P. (SRR-586). The increase in sedimentation rate and the less compacted nature of the sediment is consistent with increased water depths after ca 3800 yr B.P. The aquatic pollen assemblage is characterised by a gradual increase in the abundance of Isoetes, Equisetum and Cyperaceae and the occurrence of Potamogeton, Myriophyllum and Nymphaea, and is consistent with increased water depth. The overlying unit (0.70-0.72m) is a band of coarse detrital material, including birch twigs. The unit is thought to have originated as an inwash layer, probably due to a phase of soil erosion, and as such unrelated to changes in water level (O'Sullivan, 1984, personal communication). A radiocarbon sample from 0.65-0.74m yielded an anomalous date of 2700+95 yr B.P. (SRR-588); interpolation between the other radiocarbon dates suggests an age of ca 1650 yr B.P. for the inwash event. O'Sullivan (1976) suggests that the anomaly is due to incorporation of older carbon by erosion. The overlying unit (0-0.70m) is a medium detritus mud. The lower part of the unit between 0.62-0.70m is mottled. Sphagnum becomes an increasingly important component of the aquatic assemblage, while Equisetum declines in abundance. These changes are consistent with hydroseral development. In the status coding, the hiatus in sedimentation between the Late Devensian clays and the organic deposits is indicated by 0; low (1) is indicated by the deposition of compact fine detritus mud with low sedimentation rates; intermediate by deposition of fine detritus mud with increased sedimentation rates and moderate abundances of Isoetes; high (3) by the deposition of medium detritus mud. The detrital organic unit at 0.70-0.72 is assumed to reflect an inwash event in the catchment rather than a change in water levels. References Birks, H.H., 1970. Studies in the vegetational history of Scotland. Journal of Ecology 58: 827-846. Harkness, D.D., 1981. Scottish University research and reactor centre radiocarbon measurements IV. Radiocarbon 23: 252-304. O'Sullivan, P.E., 1975. Early and Middle-Flandrian pollen zonation in the Eastern Highlands of Scotland. Boreas 4: 197-207. O'Sullivan, P.E., 1976. Pollen analysis and radiocarbon dating of a core from Loch Pityoulish, Eastern Highlands of Scotland. Journal of Biogeography 3: 293-302. O'Sullivan, P.E., 1984. Personal communication by letter. Radiocarbon Dates SRR-589 1010+60 30-40cm medium detritus gyttja SRR-588 2710+100 65-74cm medium detritus gyttja, ATO, contaminated by inwash. SRR-587 2990+60 130-140cm medium detritus gyttja SRR-586 3800+60 170-180cm fine detritus gyttja SRR-459 5550+50 214-226cm fine detritus gyttja SRR-460 6630+60 229-238cm fine detritus gyttja SRR-571 7970+60 246-256cm fine detritus gyttja SRR-572 8390+70 256-262cm clay Note: There are slight discrepancies between the depths of the radiocarbon samples as given in Harkness (1981), which we use here, and those inferred from O'Sullivan (1976). Coding 8900 (or 9400)-8400 yr B.P. hiatus (0) 8400-5550 yr B.P. low (1) and fluctuating 5550-3800 yr B.P. intermediate (2) 3800-0 yr B.P. high (3) Preliminary coding: 30th June 1992; Final coding: 14th July 1993 Coded by SPH Roos, UK Roos (The Bog, Roos, 53 40'N, 0 4'E, 5m above sea level) is a peat bog, but was formerly on an area of open water in Holderness, England. It lies 6km from the coast. The former lake had an area of ca 26ha (220mx120m). The basin lies in an oval depression in last glacial till (Devensian Withernsea Till, before 13,000 yr B.P.), formed as a kettle hole. The lake formed after 13,050 yr B.P. and became infilled after ca 3500 yr B.P. (Beckett, 1981). The peat bog was artificially drained recently and is now covered by woodland (Beckett, 1981). The bedrock in the catchment is Upper Chalk (Valentin, 1957). A transect of borings from the basin provides a 11.5m composite sedimentary record back to ca 13,000 yr B.P. (Beckett, 1981). Changes in water depth are reconstructed from changes in lithology, aquatic pollen assemblages and sedimentation rates. The chronology is based on five radiocarbon-datings from Roos, which provide ages between 13,000-10,000 yr B.P., and pollen correlation with the nearby radiocarbon-dated sites (Beckett, 1975) of Gransmoor Quarry, North Holderness (Beckett, 1975) and North Ferriby (Wright and Churchill, 1965). The basal sediment (1150-1136cm) is gravelly clay. These are probably glacial deposits from before 13,050 yr B.P. (Beckett, 1975). The overlying sediment (1136-1133cm) is fine detritus mud, suggesting moderately deep water. The aquatic assemblage is characterised by Typha, Sparganium and Nymphaea, consistent with moderately deep water. A sample from the bottom of this unit is radiocarbon-dated to 13,045±270 yr B.P. (Birm-217, 1133-1140cm). The overlying sediment (1133-1116cm) is a slightly organic grey clay, suggesting increased water depth. Aquatics are less abundant, and characterised by decreased Typha and the presence of Myriophyllum alterniflorum, consistent with increased water depth. The unit has a quite low sedimentation rate (0.016 cm/yr), supporting deep water conditions. This unit is dated to ca 12,900-11,600 yr B.P. The overlying sediment is fine detritus mud (1116-1090cm), suggesting decreased water depth. The aquatic assemblage is characterised by decreased Myriophyllum alterniflorum, consistent with decreased water depth. Three samples from this unit are radiocarbon-dated to 11,500±170 yr B.P. (Birm-318, 1110-1115cm), 11,450±230 yr B.P. (Birm-407, 1102-1105cm) and 11,220±220 yr B.P. (Birm-406, 1091-1095cm) respectively. The overlying sediment is pinkish grey clay (1090-930cm). The sediment contains fragments of the moss Fontinalis antipyretica, suggesting shallow water. The aquatic assemblage is characterised by abundant Typha latifolia, Sparganium and Nymphaea, consistent with shallowing. An increase in sedimentation rate from 0.08 cm/yr to 0.16 cm/yr is also consistent with this interpretation. This unit is dated to ca 11,200-10,100 yr B.P. The overlying sediment is fine detritus mud (930-390cm), suggesting increased water depth. There is a marked increase in Myriophyllum and decrease in Typha latifolia ca 930cm. The disappearance of moss fragments and decline in Typha suggest increased water depth. The aquatic assemblage in the main part of the unit includes Myriophyllum, Sparganium and Typha, consistent with a moderately deep water. This unit belongs to pollen zone RB4, RB5 and RB6 (ca 900-400cm), and is dated to ca 10,100-5100 yr B.P. The upper boundary is dated 5099±50 yr B.P. (SRR-229) at Gransmoor Quarry (Beckett, 1981). The overlying sediment is coarse detritus mud (390-200cm), suggesting decreased water depth. The aquatic assemblage is marked by an increase in Menyanthes, Myriophyllum, Sparganium and Typha, consistent with shallow water. This unit belongs to pollen zone RB7 (ca 400-220cm) and is dated to ca 5100-3400 yr B.P. The upper boundary is dated by two samples 3433±110 (Q-837) and 3120±105 (Q-715) from pollen zones RB8, RB9 and RB10 at North Ferriby (Beckett, 1981). The topmost sediment is peat with plentiful Sphagnum, Menyanthes trifoliata seeds, Ericaceae stems and Polytrichum spp., indicating hydroseral development and infilling process in the basin after ca 3400 yr B.P. In the status coding, low (1) is indicated by coarse detritus mud with Menyanthes, Myriophyllum, Sparganium and Typha; intermediate (2) by pinkish grey clay with moss fragments and abundant Typha, Sparganium and Nymphaea; moderately high (3) by fine detritus mud with abundant Myriophyllum; high (4) by grey clay with low aquatics and low sedimentation rate. Peat deposition after ca 3400 yr B.P. reflects lake infilling, and this interval is not coded. Radiocarbon dates Birm-217 13,045±270 1133-1140cm, fine detritus mud Roos core. Birm-318 11,500±170 1110-1115cm, fine detritus mud Roos core. Birm-407 11,450±230 1102-1105cm, fine detritus mud Roos core. Birm-406 11,220±220 1091-1095cm, fine detritus mud Roos core. Birm-405 10,120±180 920-925cm, fine detritus mud Roos core. SRR-230 8507±55 pollen zone RB5/RB6, Gransmoor Quarry. SRR-229 5099±50 pollen zone RB6/RB7, Gransmoor Quarry. Q-837 3433±110 pollen zone RB8, 9, 10, Gransmoor Quarry. Q-715 3120±105 pollen zone RB8, 9, 10, Gransmoor Quarry. References Beckett, S.C., 1975. The Late Quaternary vegetational history of Holderness, Yorkshire. Ph.D thesis, University of Hull. Beckett, S.C., 1981. Pollen diagrams from Holderness, North Humberside. Journal of Biogeography 8: 177- 198. Gilbertson, D.D., 1984. Late Quaternary environments and man in Holderness. BAR British Series 134: 159- 175. Valentin, H., 1957. Glazialmorphologische untersuchungen in Ostengland. Abhandlungen Geographischen Institut, Universität Berlin: 1-86. Wright, E.V. and Churchill, D.M., 1965. The boats from North Ferriby, Yorkshire, England. Proceedings of the Prehistory Society 31: 1-24. Coding 13,050-12,900 yr B.P. intermediate (3) 12,900-11,600 yr B.P. high (4) 11,600-11,200 yr B.P. intermediate (3) 11,200-10,100 yr B.P. moderately low (2) 10,100- 5100 yr B.P. intermediate (3) 5100-3400 yr B.P. low (1) 3400-0 yr B.P. infilling, not coded. Preliminary coding: March 1994; Final coding: May 1994 Coded by GY and SPH Saham Mere, UK Saham Mere (52 34'N, 0 48'E, 38m above sea level) is a small lake in East Anglia, England. The lake is roughly circular with an area of ca 6.7ha (250 x 275m) and a maximum water depth of 1m. The catchment is 30ha in area and only ca 29m deep. There is an outflow from the lake southwest into the River Wissey, but it is probably artificial (Bennett, 1884). The bedrock in the catchment is Upper Chalk, covered by chalky clay till. The basin probably originated as a hollow in till. The lake does not undergo marked variations in depth under modern conditions, which suggests that water levels are probably controlled by the water table in the till (Bennett, 1983, 1988). A ca 30m-long Livingstone core from the centre of the lake provides a lithological and pollen record back to ca 17,400 yr B.P. (Bennett, 1988). Core depths were measured from a fixed point 40cm above lake surface, such that the sediment surface is at 1.4m. The upper part of core (above 23.64m) has not been described. Change in water depth is reconstructed from changes in lithology, lamination structures and sedimentation rate. Ten samples from the core are radiocarbon-dated (Bennett, 1988). The dates form a conformable sequence though showing considerable variation in sedimentation rates. Bennett (1988) states that, although approximate support for most of the dates can be found from other sites, these dates are too old due to old carbonate contamination. However, five of the dates are on material that contains no significant calcium carbonate, and these fit well with the rest of sequence. There does not seem to be overwhelming evidence in favour of rejecting these dates, and the chronology is therefore based on the complete sequence of ten dates. The basal sediment is calcareous clay mud (28.59-29.18m below water surface). The unit was probably derived from till underlying the lake sediments. Two radiocarbon-dates at the top (Q-2284, 29.03-29.13m) and near bottom (Q-2285, 28.51-28.61m) give ages of 14,100±170 and 17,400±190 yr B.P. for this unit. The overlying sediment is sand (28.56-28.59m), suggesting shallow water in the initial phase of lacustrine sedimentation. This unit is dated to ca 14,100-14,000 yr B.P. A change to slightly calcareous sandy lake mud (28.39-28.56m), suggests the onset of stable lacustrine conditions in the basin and deeper water in the lake. The unit is dated to ca 14,000-13,250 yr B.P. The overlying sediment is slightly calcareous silty lake mud (28.10-28.39m). The finer lithology suggests a continued increase in water depth. The low sedimentation rate (0.02 cm/yr) is consistent with increased water depth. The unit is dated to 11,800-13,250 yr B.P. A change to non-calcareous sandy lake mud (27.68-28.10m), suggests a return to shallow conditions. An increase in sedimentation rate from 0.02 to 0.6 cm/yr is consistent with this interpretation. The absence of calcium carbonate could indicate reduced leaching from the catchment. This unit is dated to ca 10,200-11,800 yr B.P. The overlying sediment is non-calcareous detritus lake mud (25.40-27.68m). The finer nature of the sediment suggests increased water depth. A decrease in sedimentation rate to 0.15 cm/yr is consistent with this interpretation. Three samples from this non-calcareous unit are radiocarbon-dated (Q-2276, Q-2277 and Q- 2278), suggesting it formed ca 8200-10,200 yr B.P. The overlying sediment is non-calcareous humified detritus lake mud (25.00-25.40m), suggesting the lake remains moderately deep. A drop in sedimentation rate to 0.09 cm/yr is consistent with this. Humification may suggest oxygenation and slight shallowing. A sample from this non-calcareous unit is radiocarbon-dated to 7970±60 yr B.P. (Q-2279, 25.13-25.23m). A marked increase in water depth after 6580 yr B.P. is indicated by deposition of calcareous laminated lake mud (23.64-25.00m). The unit contains humified detritus and shells of Bithynia tentaculata. A low sedimentation rate (0.05 cm/yr) is consistent with deepening. Two samples from the top (Q-2282, 23.59-23.69m) and the bottom (Q-2280, 24.89-24.99m) of the unit are radiocarbon-dated to 4200±50 yr B.P. and 6580±60 yr B.P. respectively. The record for the last 4200 years has not been studied. Sedimentation rate increases markedly (0.53 cm/yr above 23.64m). Bennett (1988) attributes this to eutrophication. In the status coding, very low (1) is indicated by initial sand layer; low (2) by sandy lake mud; intermediate (3) by silty lake mud; moderately high (4) by humified detritus lake mud; high (5) by non-humified detritus lake mud; very high (5) by laminated detritus lake mud. References Bennett, F.J., 1884. The Geology of the Country Around Attleborough, Watton and Wymondham. Memoirs of the Geological Survey of England and Wales. Bennett, K.D., 1983. Devensian Late-glacial and Flandrian vegetational history at Hockham Mere, England. New Phytologist 95: 457-487. Bennett, K.D., 1988. Holocene pollen stratigraphy of central East Anglia, England, and comparison of pollen zones across the British Isles. New Phytologist 109: 237-253. Radiocarbon dates Q-2282 4200±50 yr B.P. 2359-2369cm, calcareous laminated mud. Q-2281 5520±55 yr B.P. 2451-2461cm, calcareous laminated mud. Q-2280 6580±60 yr B.P. 2489-2499cm, calcareous laminated mud. Q-2279 7970±60 yr B.P. 2513-2523cm, non-calcareous humified mud. Q-2278 8700±65 yr B.P. 2581-2591cm, non-calcareous mud. Q-2277 9280±80 yr B.P. 2667-2677cm, non-calcareous mud. Q-2276 9850±85 yr B.P 2741-2751cm, non-calcareous mud. Q-2283 10500±110 yr B.P. 2779-2789cm, non-calcareous sandy mud. Q-2285 14100±170 yr B.P. 2851-2861cm, calcareous clay mud. Q-2284 17400±190 yr B.P. 2903-2913cm, calcareous clay mud. Coding ca 14,100-14,000 yr B.P. very low (1) ca 14,000-13,250 yr B.P. low (2) ca 13,250-11,800 yr B.P. intermediate (3) ca 11,800-10,200 yr B.P. low (2) ca 10,200-8200 yr B.P. high (5) ca 8200-6580 yr B.P. moderately high (4) ca 6580-4200 yr B.P. high (5) ca 4200-0 yr B.P. no record. Preliminary coding: 18/5/1994; Final coding: 22/5/1994 Coded by GY and SPH Sea Mere, UK Sea Mere (52 34'N, 1 00'E, 38m above sea level) is a small lake in England, with an area of ca 7ha and a maximum depth of 4m. The catchment area is ca 520ha. There are two small inflow streams entering the lake from the west and the south, and one outflow in the southeast to the River Yare (Hunt and Birks, 1982). The basin is situated in chalky boulder clay (Sims, 1973). It is mantled by till and the soils are calcareous. The basin is not a ground-ice depression (Sparks et al., 1972), but probably owes its origin to the solution of the underlying chalk bedrock and collapse of the overlying deposits (Hunt and Birks, 1982). There are two cores (SM, S) from Sea Mere. A ca 20m long core (core SM), taken in ca 4m of water in the centre of the lake, has been studied by Hunt and Birks (1982) and by Bennett (1988). Core S, a marginal core covering the last ca 7500 year B.P. has been studied by Sims (1973, 1978). Changes in relative water depth are based on changes in lithology and aquatic assemblages. The chronology is based on terrestrial pollen correlation with Hockham Mere (Bennett, 1983a, 1988; Sims, 1978). Hockham Mere is 10km away from Sea Mere and the chronology is based on over 30 radiocarbon dates (Hunt and Birks, 1982; Sims, 1978). The basal sediment in core SM (19.66-18.51m below the water surface) is chalky silt and chalky rubble of very low organic content, suggesting the sediment was deposited in shallow water. The pollen grains are poorly preserved. The macrophyte pollen is sparse, but includes Potamogeton, Chara and Nitella. This unit is dated to ca 13,870-13,000 yr B.P. (Hunt and Birks, 1982). The overlying sediment in core SM (18.51-18.11m below the water surface) is detritus clay and silty clay mud, suggesting increased depth. Aquatic taxa are well represented, mainly Potamogeton type with Chara, Nitella, Plumalella, Daphnia and some Myriophyllum spicatum, consistent with deeper water ca 12,000-13,000 yr B.P. The overlying unit in core SM (18.11-17.81m below the water surface) consists of organic mud with sand and silt, indicating that the lake was shallow. Aquatics are rare with scattered grains of Sparganium and Myriophyllum spicatum. This interval is dated ca 12,000-11,000 yr B.P. The overlying sediment in core SM (16.50-17.81m below the water surface) is silty detritus mud with fine sand and some coarse sand, indicating the lake became shallower. The presence of woody detritus and moss fragments (including Bryum sp., Calliergon cuspidatum, Drepanocladus sp., Homalothecium sp. and Philontis fontana), consistent with shallow water. The aquatic assemblage is marked by increases in Equisetum, Typha, Potamogeton, Nymphaea and abundant sedges, consistent with shallow water. The interval is dated between ca 11,000 and 10,000 yr B.P. The overlying unit in core SM (15.64-16.50m below the water surface) is banded silty fine detritus mud and marl, banded marl and mud, indicating the lake became deep. The aquatic assemblage is characterised by Myriophyllum spicatum and Potamogeton, with some Sparganium, Nymphaea and Nitella. This interval is dated ca 10,000-9200 yr B.P. The sediment in core SM (15.71-11.40m below the water surface, ca 9200-1980 yr B.P.) is calcareous lake mud, suggesting deeper water than the before. The skull bones of a pike (Esox Lucius L.) are found at 15.09m below the water surface (Bennett, 1983b), consistent with the interpretation of deep water. Core S has more detailed record of change during the late Holocene (after 7200 yr B.P.). The basal sediment in core S (7.2-6.5m, ca 7200-5000 yr B.P.) consists of detritus mud with sand. The aquatic assemblage is marked by Typha, Cyperaceae with Ranunculus, Nymphaea and Nuphar. The overlying unit in core S (6.5-5.5m, ca 5000-3800 yr B.P.) is pure mud and marl containing little detritus, suggesting the lake became deeper. The aquatic plants are represented by Potamogeton, consistent with deeper water. The overlying sediment in core S (5.5-4.5m, ca 3800-2600 yr B.P.) is mud and marl with coarse detritus, suggesting shallowing. The aquatic assemblage is characterised by Ranunculus, Typha with some Potamogeton and Myriophyllum. Increases in Typha and Ranunculus suggest shallower conditions. The overlying sediment in core S (4.5-2.5m, ca 2600-1900 yr B.P.) is coarse detritus mud. The increase in coarse detritus indicates shallower water. The aquatic assemblage is characterised by Ranunculus and Typha with Menyanthes, Nuphar and Nymphaea, consistent with shallowing. The top of sediment in the core S (2.5-0m, last ca 1900 yr B.P.) is mud and marl. The decrease in the detrital component suggests increased water depth. The aquatic pollen assemblage is marked by increases in Potamogeton and Myriophyllum, consistent with deeper water. In the status coding: very low (1) is indicated by chalky silt/ rubble with poor pollen preservation in central core; low (2) by organic mud with silt and sand, and containing moss fragments, in central core; moderately low (3) by organic mud with silt and sand in central core; intermediate (4) by calcareous lake mud in central core, and coarse detritus mud with Menyanthes in marginal core; high (5) by calcareous lake mud in central core, and detritus mud with diverse aquatic assemblage in marginal core; very high (6) by detritus clay and silty clay mud with diverse aquatic assemblage in central core, or calcareous lake mud in central core and calcareous mud with sparse aquatic assemblage in marginal core. References Bennett, K.D., 1983a. Devensian Late-glacial and Flandrian vegetational history at Hockham Mere, England. New Phytologist 95: 457-487. Bennett, K.D., 1983b. An occurrence of pike (Esox lucius L.) in the early post-glacial at Sea Mere, Norfolk, and the origin of British freshwater fishes. Quaternary Newsletter 41: 7-10. Bennett, K.D., 1988. Holocene pollen stratigraphy of central East Anglia, England, and comparison of pollen zones across the British Isles. New Phytologist 109: 237-253. Hunt, T.G. and Birks, H.J., 1982. Devensian late-glacial vegetational history at Sea Mere, Norfolk. Journal of Biogeography 9: 517-538. Sims, R.E., 1973. The anthropogenic factor in East Anglia vegetational history: an approach using A.P.F. techniques. In: Birks, H.J.B. and West, R.G. (eds), Quaternary Plant Ecology. Blackwell Science Publication, Oxford. Sims, R.E., 1978. Man and vegetation in Norfolk. in: Limbrey, S. and Evans, J.G.(eds), The Effect of Man on the Landscape: the Lowland Zone. Council of British Archaeology Report 21: 57-62. Sparks, B.W., Williams, G. and Bell, G., 1972. Presumed ground-ice depressions in Eastern England, Proceedings of the Royal Society of London 327 (A): 329-343. Coding ca 13,870-13,000 yr B.P. very low (1) ca 13,000-12,000 yr B.P. very high (6) ca 12,000-11,000 yr B.P. moderately low (3) ca 11,000-10,000 yr B.P. low (2) ca 10,000-9200 yr B.P. intermediate (4) ca 9200-5000 yr B.P. high (5) ca 5000-3800 yr B.P. very high (6) ca 3800-2600 yr B.P. high (5) ca 2600-1900 yr B.P. intermediate (4) ca 1900-present very high (6) Preliminary coding: 23/2/1993; Final coding: 15/6/1994 Coded by GY and SPH Traeth Mawr, UK Traeth Mawr (51 55'N, 3 30'W, 330m above sea level) lies on the undulating plateau of the Mynydd Illtydd to the north of the Brecon Beacons, Wales. The basin probably formed by melting of dead ice (Walker, 1982a) during the last deglaciation. The basin has an approximate area of ca 100ha and is occupied by a bog, but was formerly the site of a large lake. The bog is characterised by numerous small pools. It is drained by two streams which flow northwestwards into Cwm Camlais and ultimately into the River Usk. The Brecon Beacons are sandstone uplands. They were extensively glaciated during the last glacial maximum, and there is evidence for more restricted glacial activity during the Loch Lomond Stadial (Walker 1982b), which is considered equivalent to the Younger Dryas. A core (2m long) taken near the centre of Traeth Mawr bog provides a sedimentary record back to ca 12000 yr B.P. (Walker, 1982a). Changes in water depth are reconstructed from changes in lithology, sedimentation rates, aquatic pollen assemblages and pollen preservation. The chronology is based on three radiocarbon dates (Walker, 1982a). Material for radiocarbon dating was obtained by combining 2cm slices (across key lithological transitions at 2.89m, 3.69 and 3.99m) from 6 closely spaced cores. The basal sediments (4.25-5.07m) are rhythmically-bedded sands, silts and clays, almost devoid of pollen. They appear to have been formed rapidly (maybe in as little as 100 years) in a proglacial environment at a time when the Late Devensian ice cover was wasting away. The preservation of bedding argues that the lake was relatively deep with anoxic bottom waters. The overlying unit (3.99-4.25m) is a red silt clay. The aquatic assemblage is characterised by abundant Potamogeton, with Myriophyllum and occasional Nymphaeae, and is consistent with moderately deep water. The overlying unit (3.69-3.99m) is fine brown gyttja. A sample from the transition to gyttja was radiocarbon dated at 11620+140 yr B.P. (SRR-1562). The aquatic assemblage in the lower part of the unit, below 3.83m, is characterised by a marked decrease in Potamogeton and Myriophyllum, and by the presence of shallow-water aquatics including Menyanthes and Littorella. The lithology and the aquatic assemblage are both consistent with shallower conditions after ca 11620 yr B.P. There are two ca 1cm-thick silt clay bands at 3.83 and 3.88m. These minerogenic bands are marked by an increase in deteriorated pollen and a slight increase in apparent sedimentation rates. Walker (1982) suggests that these silt clay bands could represent phases of soil inwash or could have been caused by the collapse and reworking of basin edge sediments. He argues that the gentle slope angles and the absence of sharp breaks of slope within the modern basin seems inconsistent with erosion of basin edge sediments. However, subaerial erosion of newly exposed and unconsolidated marginal sediments would be consistent with the shallowing indicated by the aquatic assemblages. The uppermost gyttja, above the silt-clay bands, is characterised by increased abundance of Potamogeton and Myriophyllum, the presence of Nymphaea and the absence of Menyanthes, suggesting increased water depth after ca 11090 yr B.P. The overlying unit (2.89-3.69m) is a red silt/clay. A sample spanning the transition to this unit was radiocarbon dated to 10620+140 yr B.P. (SRR-1561). There is a fourfold increase in sedimentation rate at this transition, and the terrestrial pollen shows an increase in broken and crumpled grains. This suggests that the deposition of minerogenic sediments reflects an increase in soil erosion within the catchment (Walker, 1982a). Across the transition from gyttja to minerogenic sediments and in the lowermost few centimetres of the silt/clay, the aquatic pollen assemblages are characterised by a decrease in Potamogeton and Myriophyllum and the reappearance of Menyanthes. The aquatic assemblage in the remaining part of the unit is characterised by low abundances of Potamogeton and Myriophyllum. Shallow water aquatics such as Menyanthes and Littorella are not registered. This suggests that the lake was deeper, which could be considered consistent with increased runoff and increased catchment erosion. The deposition of clay gyttja between 2.87-2.89m suggests shallowing after ca 9970 yr B.P. The marked increase in Potamogeton and Myriophyllum is consistent with shallowing. The overlying muddy gyttja (2.60- 2.87m) is characterised by the occurrence of several silt/clay bands (at 2.78, 2.81 and 2.83m). These lithological changes suggest fluctuating or unstable water levels. The zone between 2.49-2.60m marks a transition from organic muds into fine amorphous peat as the lake infilled. The presence of Menyanthes and Typha, and the decline in abundance of Potamogeton, Myriophyllum and Nymphaea, is consistent with shallowing. The uppermost 2.49m of sediment consist of peat. The increase in corroded pollen grains above 2.50m is consistent with oxidation in the loosely-compacted accumulating peats. These changes may reflect hydroseral development in the basin. In the status coding, low (1) is indicated by gyttja with an aquatic assemblage including shallow water species such as Menyanthes; intermediate (2) by gyttja and an aquatic assemblage with abundant Potamogeton, Myriophyllum and Nymphaea; high (3) by red silt clays and the absence of shallow-water aquatics; and very high (4) by laminated sands, silts, clays. Note that peat deposition after 9100 yr B.P. may indicate infilling and this part of the record may not reflect a climatic signal and so is excluded from the coding. References Walker, M.J.C., 1982a. The late-glacial and early Flandrian deposits at Traeth Mawr, Brecon Beacons, South Wales. New Phytologist 90: 177-194. Walker, M.J.C., 1982b. Early- and mid-Flandrian environmental history of the Brecon Beacons, South Wales. New Phytologist 91: 147-165. Radiocarbon Dates SRR-1560 9970±115 2.88-2.90m red silt/clay SRR-1561 10620±100 3.68-3.70m red silt/clay SRR-1562 11660±140 3.98-3.90m brown gyttja Coding pre-11860 yr B.P. very high (4) 11860-11660 yr B.P. high (3) 11660-11090 yr B.P. low (1) 11090-10780 yr B.P. intermediate (2) 10780-10535 yr B.P. low (1) 10535- 9970 yr B.P. high (3) 9970- 9100 yr B.P. intermediate (2) 9100- 0 yr B.P. infilling, not coded. Preliminary coding: 13th August 1992; Final coding: 14th July 1993 Coded by SPH and GY Malo Jezero, Yugoslavia Malo Jezero (42 47'N, 17 21'E, 0m above sea level) is a saltwater "lake", connected to the sea by a narrow channel, on the island of Mjlet (Beug, 1961a). The lake has an area of about 18ha and a maximum depth of 30m. The basin originated as a doline in limestone. Fore cores (III, IV, V and VI) provide a sedimentary record of most of the Holocene (Beug, 1961a, b, 1962, 1967, 1975). Core VI (1.90m) was taken in a water depth of about 23m. The other three cores are much shorter (ca 0.7m, 1.2m and 0.5m respectively) and were taken in a depth of about 29m. The basal sediments are freshwater peats and gyttja, formed when the basin was isolated from the sea. Beug (1961a, 1967) argues that the occurrence of brackish-water aquatics in the uppermost sediments indicates that the basin was breached about 2000 yr B.P. and has been subject to marine influence continuously since then. There appears to have been no sedimentation in the basin since 2000 yr B.P., presumably because of tidal scour. Changes in water depth before 2000 yr B.P., when the basin was an isolated freshwater lake, can be reconstructed from changes in sediment lithology and in aquatic plant assemblages as registered by pollen and macrofossils. The chronology is established by three radiocarbon dates. The lowermost sediments in core VI (1.6-1.9m) are clays. There is no evidence that these clays are lacustrine, but they appear to have sealed the basin and allowed a lake to form within the doline. A basal sample (1.70- 1.90m) has been radiocarbon dated to 9000 yr B.P. The overlying deposits are clayey sedge peats (1.48-1.60m) and sedge peats (1.36-1.48m). A sample from 1.36-1.52m has been dated 8400 yr B.P. The overlying sediments are coarse detritus gyttja (1.33-1.36m) grading up into pure, calcareous gyttja (0.98-1.33m). This sequence (peat, detritus gyttja, calcareous gyttja) is indicative of a gradual increase in water depth. Aquatic pollen is abundant in both the peats and the gyttjas. Sparganium is recorded alone between 1.48-1.58m (clayey sedge peat), and then occurs with Nymphaea within the sedge peat. Nymphaea is most abundant (over 3%) around 1.3m, after which Potamogeton become dominant within the calcareous gyttja. These changes in the aquatic assemblages are consistent with a gradual increase in water depth. The occurrence of Chara within the calcareous gyttja is consistent with moderately deep water. The overlying sediments (0.60-0.98m) are clay gyttja. The virtual absence of aquatic pollen suggests that the water was deeper than before. The interval between 0.42-0.60m in core VI consists of several thin units of calcareous clayey gyttja or clay gyttja in alternation. The deposits of similar age (pollen zones B2/C1) in the deepwater cores are laminated, which suggests they were deposited under anoxic conditions in a deep lake. A sample from just below the B2/C1 boundary in core V (0.37-0.5m) has been radiocarbon dated to 6800±125 yr B.P., which suggests that the laminated sediments were deposited between 6000-7000 yr B.P. The uppermost sediments in the deepwater cores are unlaminated, indicating that water depth decreased after ca 6000 yr B.P. The uppermost sediments in core VI (0-0.60m) are calcareous gyttja, which also suggests that the lake was shallower. In the status coding, very low (1) is indicated by peat deposition with abundant aquatic pollen; low (2) by coarse detritus gyttja deposition with Sparganium and very abundant Nymphaea; intermediate (3) by calcareous gyttja deposition with Potamogeton and Chara; high (4) by clay gyttja deposition in core VI, with virtually no aquatic pollen deposition; very high (5) by laminated sediments in the deepwater cores. References Beug, H-J., 1961a. Beiträge zur postglazialen Floren- und Vegetationsgeschichte in Süddalmatien: Der See "Malo Jezero" auf Mljet. Teil 1. Vegetationsentwicklung. Flora 150: 600-631. Beug, H-J., 1961b. Beiträge zur postglazialen Floren- und Vegetationsgeschichte in Süddalmatien: Der See "Malo Jezero" auf Mljet. Teil II: Häufigkeit und Pollenmorphologie der nachgewiessenen Pflanzensippen. Flora 150: 632-655. Beug, H-J., 1962. Über die ersten anthropogenen Vegetationsveränderungen i Süddalmatien an Hand eines neuen Pollendiagrammes vom "Malo Jezero" auf Mljet. Sonderdruck aus den Veröffentlichungen des Geobotanischen Institutes der Eidg. Techn. Hochschule, Stiftung Rübel (Zürich) 37: 9-15 Beug, H-J., 1967. On the forest history of the Dalmation coast. Review of Palaeobotany and Palynology 2: 271- 279. Beug, H-J., 1975. Man as a factor in the vegetational history of the Balkan Peninsula. Proceedings of the First International Symposium on Balkan Flora and Vegetation, Varna, June 1973, pp. 72-78. Radiocarbon Dates N/A 6800±125 yr B.P. 0.37-0.50m, Core V, below B2/C1 boundary, clayey gyttja N/A 8400 yr B.P. 1.36-1.52m, Core VI, peat N/A 9000 yr B.P. 1.70-1.90m, Core VI, clay Coding 8730-8270 yr B.P. very low (1) 8400-8200 yr B.P. low (2) 8200-7600 yr B.P. intermediate (3) 7600-7000 yr B.P. high (4) 7000-6000 yr B.P. very high (5) 6000-2000 yr B.P. intermediate (3) Preliminary coding: pre-September 1991; Final coding: January 1994 Coded by SPH Palu, Yugoslavia Lake Palu (45 01'36''N, 13 42'10''E) is a brackish-water lake, situated in a sink hole near the Adriatic coast (Beug, 1977, 1977). The modern lake has an area of ca 2ha and a mean water depth of about 70cm. The doline has an area of 20-25ha, mostly occupied by marsh vegetation. The lake has an artificial outlet to the sea, via a narrow channel about 250m long, which was created in 1916 in order to minimise the breeding grounds for malaria. The catchment bedrock is limestone. A single profile (Palu II), taken in a water depth of 70cm, provides a sedimentary record back to ca 6000 yr B.P. Note that the core depths in Beug (1977), and used here, are given from the water surface not from the sediment/water interface. Changes in water depth are reconstructed on the basis of changes in lithology, aquatic pollen and macrofossil assemblages (Beug, 1977). The chronology is based on a single radiocarbon date and the fact that the earliest occurrence of Castanea and Juglans on the Adriatic coast is dated to ca 2000 yr B.P. (Beug, 1977). The basal sediments (4.60-4.90m) are clay. The overlying unit (3.65-4.60m) is clay gyttja. The aquatic assemblage includes Nymphaea, Myriophyllum-type and Ranunculus. The overlying unit (2.70-3.65m) is coarse detritus gyttja. The change in lithology is consistent with shallower conditions. The appearance of Alisma is also consistent with shallowing. A sample from near the base of this unit (350-360cm) was radiocarbon dated to 4490+125 yr B.P. (Hv-1640). The overlying unit (2.14-2.70m) is fine detritus gyttja, indicating somewhat deeper conditions. The presence of molluscs is consistent with deeper water. The overlying unit (1.90-2.70m) is coarse detritus gyttja, indicating shallowing. The uppermost unit (0.70-1.90m) is fine detritus gyttja, again containing mollusc shells, consistent with deeper water conditions. The aquatic macrofossil record shows that Palu was a freshwater lake until the end of Pollen Zone 2 (after ca 2000 yr B.P.). At the beginning of Pollen Zone 3, freshwater aquatics were replaced by Ruppia and other plants characteristic of brackish-water environments. According to Beug (1977) the lake became brackish because of seawater incursions, via fractures in the bedrock. In the status coding, low (1) is indicated by coarse detritus gyttja, intermediate (2) by fine detritus gyttja, and high (3) by clay or clay gyttja. The interval after ca 2000 yr B.P. is not coded because of the possibility that the record is affected by marine incursions. Reference Beug, H-J., 1975. Man as a factor in the vegetational history of the Balkan Peninsula. Proceedings of the First International Symposium on Balkan Flora and Vegetation, Varna, June 1973, pp. 72-78. Beug, H-J., 1977. Vegetationsgeschichtliche Untersuchungen im Küstenberiech von Istrien (Jugoslawien). Flora 166: 357-381. Radiocarbon Date Hv-1640 4490±125 yr B.P. 350-360cm, coarse detritus gyttja Pollen Date ca 260cm beginning of Castanea and Juglans curves, 2000 yr B.P. Coding 6000-4490 yr B.P. high (3) 4490-3400 yr B.P. low (1) 3400-2400 yr B.P. intermediate (2) 2400-2000 yr B.P. low (1) Preliminary coding: March 1987; Final coding: September 1988 Coded by: SPH 4. 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Dubh Lochan, UK Dubh Lochan, UK 330 329 Hockham Mere, UK Ellesmere, UK Ellesmere, UK Garten, UK Garten, UK Hockham Mere, UK Hockham Mere, UK Hornsea Old Mere, UK Hornsea Old Mere, UK Linton Loch, UK Linton Loch, UK Llangorse Lake, UK Llangorse Lake, UK Llyn Clyd, UK Llyn Clyd, UK Melynllyn, UK Melynllyn, UK Old Buckenham Mere, UK Old Buckenham Mere, UK Pityoulish, UK Pityoulish, UK Roos, UK Roos, UK Saham Mere, UK Saham Mere, UK Sea Mere, UK Sea Mere, UK Traeth Mawr, UK Traeth Mawr, UK Malo Jezero, Yugoslavia Malo Jezero, Yugoslavia Data Base References Data Base References