Goplo Lake, Poland Goplo Lake (52 36'N, 18 19'E, 77m above sea level) lies about 45km to the southwest of Torún. The lake is rather large (24 km long and up to 2.5 km wide), with an area of 2154ha, and a maximum depth of 16.6m. Goplo Lake is connected to Pakosc Lake by the Notéc River. There appears to be an outflow today. The basin is thought to have formed as a subglacial channel during the Poznán phase of the last glaciation. The lake itself formed through ice block melting, probably during the Alleröd (Niewiarowski, 1978). Historical records indicate that the lake was formerly larger than today. The lake was artificially lowered by ca 2.7m sometime during the 19th century to establish the lake at its modern level. A terrace (I) at an elevation of 77.5-78.5m above sea level marks the position of the shoreline before this lowering. Earlier high stands are also marked by terraces. Terrace II lies at an elevation of 79-80m above sea level (+2-3m) and probably corresponds to the water level during the later part of the Middle Ages. A sand and gravel terrace (III) at an elevation of 81- 82m above sea level, overlying till deposits, marks a lake ca 4-5m higher than today. This terrace probably dates to the last glaciation, and corresponds to a relatively shallow lake formed when the channel was filled with buried dead ice blocks (Niewiarowski, 1978). The history of Lake Goplo has been reconstructed on the basis of lithological records and associated archaeological settlements (Niewiarowski, 1978). The chronology is established by three radiocarbon dates and archaeological dating. According to the pollen record the lake formed during the Alleröd and Younger Dryas. During the initial stages of its formation the lake was probably no higher than today. A section from a former bay of Goplo Lake, situated in the Gluszynska Valley near Mietlica, provides a Holocene sedimentary record (Niewiarowski, 1978). The top of the section lies at 77.3 m above sea level. The basal sediments (3.3-3.7m) are fine-grained lacustrine sands containing mollusc shells. The lithology and the presence of molluscs suggests relatively shallow conditions. The overlying unit (1.9-3.3m) is peat, indicating shallowing. A sample from a depth of 1.9-2.0m was radiocarbon dated to 8170±250 yr B.P. (Gd-395). From the position of the peat unit, the lake was at least 1.5- 3m lower than today (74-75.5m above sea level) during the Boreal. This corresponds to the lowest known level during the Holocene (Niewiarowski, 1978). The overlying units (1.7-1.9m) are sands with peat interbeds, and fine-grained lacustrine sands (1.4-1.7m). The change in lithology marks an increase in water depth. According to Niewiarowski (1978), this transgression occurred during the Atlantic period. Interpolation between the radiocarbon dates on this section would place the onset of deepening to ca 8030 yr B.P. The overlying unit (0.95-1.4m) is gyttja, with an admixture of plant detritus. The lithology is consistent with moderately deep water between ca 6600 and 5300 yr B.P. The overlying detritus gyttja (0.7-0.95m) contains an admixture of charcoal and sand, and marks a decrease in water depth. A sample from ca 0.8m was dated to 4850±260 yr B.P. (Gd-403), and suggests that shallowing began ca 5300 yr B.P. The overlying unit is sand (0.25-0.4m), marking continuing shallowing after 4570 yr B.P. The uppermost unit is a muck soil developed in a sandy unit containing abundant mollusc shells. Archaeological evidence provides some further information on the water levels of Goplo Lake. Remains of a settlement dated to the funnel beaker period (3600-2200 B.C., ca 5600-4400 yr B.P.) on the shores of the modern lake indicate that the lake could not have been higher than present (Niewiarowski, 1978). Comparison with records from the nearby Pakosc Lake suggest that this interval was terminated by a transgression of +2m. Unfortunately, deposits related to this transgression have not been dated precisely. However, the lake fell again during the Hallstadt D epoch of Lusatian culture (ca 650-400 B.C., 2560-2400 yr B.P.) to approximately the same level as today. The abandonment of Hallstadt D settlements is attributed to an increase in water levels ca 400 B.C. during the Subatlantic. Between 100 B.C. and 100 A.D., water level increased to ca 82.5m above sea level, the maximum recorded in the basin (+5-6m). Between 500-1000 A.D. the lake fell to 77-78m. The muck soil from the Gluszynska Valley section is correlated with this regression. During the later Middle Ages the water level reached 80m above sea level It appears to have persisted at this level until the lake was artificially lowered in the 19th century. In the status coding, very low (1) is indicated by peat deposition in the Gluszynska Valley section; low (2) by lacustrine sands in the Gluszynska Valley section; intermediate (3) by detritus gyttja deposition in the Gluszynska Valley section and lake levels of ca 77m above sea level; high (4) by gyttja deposition in the Gluszynska Valley section and lake levels in the range 78-81 m above sea level; very high (5) by lake levels greater than 81m above sea level For the purposes of coding, the modern level is taken to be 80m above sea level, presumed to be equivalent to the natural level before the lake was artificially lowered. Reference Niewiarowski, W., 1978. Fluctuations of water-level in the Goplo Lake and their reasons. Polskie Archiwum Hydrobiologii 25: 301-306. Radiocarbon Dates Gd-404 760±160 ca 0.2m, muck soil, Gluszynska Valley section, ATY, modern contamination Gd-403 4850±260 ca 0.8m, gyttja, Gluszynska Valley section Gd-395 8170±250 1.9-2.0m, peat, Gluszynska Valley section Coding ca 8500-8030 yr B.P. very low (1) 8030-6600 yr B.P. low (2) 6600-5300 yr B.P. high (4) 5300-4570 yr B.P. intermediate (3) 4570-2560 yr B.P. low (2) 2560-2400 yr B.P. intermediate (3) 2400-2100 yr B.P. high (4) 2100-1900 yr B.P. very high (5) 1900-1500 yr B.P. high (4) 1500- 800 yr B.P. intermediate (3) 800- 0 yr B.P. high (4) Preliminary coding: April 1987; Final coding: October 1994. Coded by: SPH Kepa, Poland Kepa (49.4 N, 22 E, 320m above sea level) lies in a secondary depression within the Jasielska-Sanockie Depression in the central Carpathians. The basin is drained by a small tributary of the Wislok River. Like many of the secondary depressions in this region, the basin was formerly occupied by a lake. The basin is currently occupied by a peat bog, with an area of ca 40ha. The bog is underlain by between 1.5-2.5m of Quaternary deposits. The underlying bedrock is flysch. The stratigraphy of the former lake has been reconstructed from a series of sections and trenches across the basin (Gerlach et al., 1972). Two sections (Kepa II and Kepa IIa) have been used for detailed sedimentological, minerological and biological analyses. Changes in relative water depth are reconstructed here from changes in lithology, aquatic pollen and macrofossil assemblages, and the abundance of molluscs and ostracodes. Although the diatom record has been studied, it does not provide information on changes in water depth since diatom abundance is very low and it would appear that most specimens have been blown into the basin (Gerlach et al., 1972). The chronology of water depth changes is based on 2 radiocarbon dates and the regional pollen chronostratigraphy, but is poorly constrained. The basal sediments (1.25-1.75m) are silty, with some fine sand, and are the result of in situ weathering of the underlying flysch bedrock. The overlying unit (1.10-1.25m) is primarily composed of weathered material but contains some concretions of lacustrine chalk and occasional mollusc shells, and probably marks the initial phase of lacustrine conditions. The overlying unit (0.8-1.1m) is a pure lacustrine chalk, indicating relatively deep water conditions. The presence of abundant mollusc (gasteropod and lamellibranch) shells, of ostracodes and of Chara oogonia are consistent with lacustrine conditions. The aquatic pollen and macrofossils indicate an assemblage with Potamogeton and Sparganium, consistent with relatively deep water. The overlying units are clayey peat (0.7-0.8m) and peat (0.0-0.7m), indicating a decrease in water depth and infilling of the basin. The aquatic pollen and macrofossil assemblages are characterised by a decline in Potamogeton, an increases in Ranunculaceae, the virtual disappearance of Sparganium and the occurrence of Alisma, consistent with shallowing. The absence of molluscs and ostracodes is also consistent with this interpretation. The dating of the open-water lacustrine phase is problematic (Gerlach et al., 1972). The terrestrial pollen assemblages suggest that the chalk was deposited during the Younger Dryas and Preboreal (ca 11,000-9800 yr B.P.). However, since vegetation development during the whole of the late glacial and Holocene is based on only 14 samples, the record is somewhat lacking in detail and this makes it difficult to be precise about the pollen- based chronology. Extrapolation of the sedimentation rate (0.06 mm/yr) between radiocarbon dates in the overlying peat unit suggest that the lacustrine chalk was deposited between ca 7835 and 12,835 yr B.P. However, the calculated accumulation rate is very low for peat and the resulting age range for the lacustrine unit seems unreasonably large. Furthermore, Gerlach et al. (1972) point out that modern roots penetrate the section down to considerable depths, and this may have affected the radiocarbon dating. Thus, the record from Kepa suggests wetter conditions were characteristic of the earlier part of the record. However, the dating control is poor and it is uncertain whether this wetter phase occurred during the late glacial, early or mid-Holocene. In the status coding, low (1) is indicated by peat deposition; high (2) is indicated by lacustrine chalk deposition. Reference Gerlach, T., Koszarski, L., Koperowa, W. and Kosta, E., 1972. Sédiments lacustres postglaciaires dans la dépression de Jaslo-Sanok. Studia Geomorphologia Carpatho-Balcanica 6: 37-61. Radiocarbon Dates GrN-6067 2275±40 yr B.P. 0.43-0.48m, peat, Kepa IIa GrN-6066 4920±60 yr B.P. 0.60-0.65m, peat, Kepa IIa Coding 11,000-7835 yr B.P. high (2) 9800- 0 yr B.P. low (1) Preliminary coding: March 1987; Final coding: March 1988 Coded by: SPH Kolno Lake, Poland Kolno Lake (53 46'N, 23 01'E, 121m abovel sea level) has a surface area of 264.4 ha, a mean depth of 1.2m and a maximum depth of 3.3m (Czeczuga and Golebiewski, 1966). The lake is fed by five small rivers and drained by the River Kolniczanka, a tributary of the Netta River. The lake is fringed by reeds, and the bed of the central section is completely covered by Chara. The lake basin is thought to have been formed during the last glaciation (Czeczuga and Golebiewski, 1966). A 4.7m core from the central part of the lake, taken in a water depth of 0.6m, provides a sedimentary record back to before 6500 yr B.P. Changes in water depth are reconstructed from changes in lithology and the presence of molluscs. The chronology is based on a single radiocarbon date. The basal unit (4.51-4.7m) is a soil developed in sandy sediments. This is overlain by a sand (4.30-4.51m). These units indicate dry conditions in the basin. Czeczuga and Golebiewski (1966) argue that the absence of sedimentary chlorophyll in the sediments is consistent with dry conditions. By correlation with other records from the region, they attribute this unit to the Boreal. Increased water depth is marked by lacustrine deposits with an admixture of sand between 4.15-4.25m. The overlying unit (0.0-4.15m) is peaty gyttja, indicating increased water depth. Czeczuga and Golebiewski (1966) argue that the increases in sedimentary chlorophyll, organic content and calcium are consistent with deep water and favourable conditions for aquatic plant growth. Changes in colour, and the presence of mollusc shells or plant remains allow this unit to be subdivided. The interval between 3.75-4.10m is characterised by the presence of mollusc shells, consistent with comparatively shallow water. A sample spanning this unit (3.80-4.10m) has been radiocarbon dated to 6250±330 yr B.P. The overlying gyttja is grey (3.05-3.70m) grading into greenish-cream (2.20-3.00m), suggesting deeper water conditions after ca 5900 yr B.P. Tha absence of molluscs is consistent with increased depth. A return to shallower water after ca 3250 yr B.P. is indicated by the abundance of mollusc shells in the overlying unit (2.15-2.05m). This shallowing culminated ca 2800-2750 yr B.P., as indicated by the presence of plant trichomes within the gyttja between 1.85-1.90m. The uppermost sediments consist of dark-coloured peaty gyttja, indicating a return to deeper water after ca 2750 yr B.P. In the status coding, low (1) is indicated by sand deposition and soil development; intermediate (2) by peaty gyttja deposits containing abundant molluscs or plant trichomes; high (3) by peaty gyttja deposits with no molluscs. Reference Czeczuga, B. and Golebiewski, Z., 1966. History of Kolno Lake as revealed by the bed sediments. Schweiz Zeitschrift für Hydrologie 28: 173-183. Radiocarbon Date n/a 6250±330 yr B.P. 3.80-4.10m, peaty gyttja with molluscs Coding 7500-6500 yr B.P. low (1) 6500-5900 yr B.P. intermediate (2) 5900-3250 yr B.P. high (3) 3250-2750 yr B.P. intermediate (2) 2750-0 yr B.P. high (3) Preliminary coding: April 1987; Final coding: December 1990 Coded by: SPH Kruklin Lake, Poland Kruklin Lake (54 4'N, 21 52'E, 127m above see level) lies in the Masurian Lake District, near the watershed between the Vistula and Goldopiwo river systems. End moraines attributed to a recessional phase of the last glaciation occur to the west, north and east of the Kruklin Basin, but the lake lies beyond these moraines. The lake has the form of a rather deep, elongated channel with a narrower central neck. Its form and position suggest that the basin was produced by glacial meltwater erosion. Geomorphological evidence shows that the lake basin was occupied by dead ice during the late glacial. The modern lake area is 356.4ha; the maximum depth in the northern sub-basin is 25.1m and 12m in the southern sub-basin; and the mean depth is 4.9m (Czeczuga and Golebiewski, 1969; Stasiak, 1963). The lake was originally closed. In 1854, a canal was excavated from Kruklin Lake to Goldopiwo Lake, resulting in a 6m lowering of the lake and the extensive exposure of lacustrine sediments around the margin. Stasiak (1963) has reconstructed changes in the level of Kruklin Lake since the Alleröd by lithological study of the exposed sediments. Additional information on changes in relative water depth is provided by the aquatic pollen and macrofossil records, and by the presence of molluscs, ostracodes and oligochaetes (Stasiak, 1963). The chronology is based on a single radiocarbon date and terrestrial pollen correlation with the regional pollen chronostratigraphy. Stasiak (1963) argues that during the early part of the lake history the water-level changes are due to melting of buried ice blocks. However, the ice had disappeared from the basin by the beginning of the Atlantic period, so the subsequent changes in water level are thought to reflect climatic changes. The bottom sediments from the lake have also been studied (Czeczuga, 1969; Czeczuga and Golebiewski, 1969) by means of a 7.7m long core taken in a water depth of 1.30m. Given that the lake has been artificially lowered, the coring site provides a record of deepwater sedimentation in the basin. The basal units are coarse sand (6.35- 7.7m) and fine sand (5.8-6.35m). The overlying unit (5.05-5.8m) is striated loam, grading into homogeneous loam (4.65-5.05m). The uppermost unit (0-4.65m) is lacustrine carbonate. The absence of nearshore deposits or intercalated peat layers places a limit on the shallowing indicated by the more marginal deposits. Geochemical analysis (chlorophyll, total organics, iron, carbonate, silica and nitrogen) show considerable variation in the nature of the bottom sediments. Unfortunately, the core has not been dated either by radiometric or palynological means, so the core record cannot be correlated with the record from the marginal exposures. The basal sediments in the marginal sections are gravel and sand. This unit is overlain by a fossil soil, containing pine trunks in situ. Soil development indicates that the basin was dry. A sample from these pine trunks was radiocarbon dated to 11,390±210 yr B.P. The overlying sediments are bluish-grey mineral clays. The maximum thickness of this unit is ca 40cm. The presence of Carex and Phragmites roots indicates that the water depth was very shallow (<0.5m). According to the terrestrial pollen assemblages, this unit was formed in the Younger Dryas. The overlying sediments are lacustrine chalk. According to the pollen assemblages, chalk formation began in the Preboreal. The lower part of the chalk is annually laminated. An increase in the abundance of deep-water aquatics (e.g. Najas marina) in the middle part of the chalk unit is consistent with deep water conditions during the Atlantic. A marked increase in the importance of Chara, and in the abundance of molluscs, ostracodes and oligochaetes in the uppermost part of the unit indicates shallower conditions. The uppermost sediments (125-126.5m above sea level.) are peat. According to the pollen assemblages, peat deposition started during the Subboreal. In the sections closest to the modern lake, this interval of peat deposition is interrupted by an interval of lacustrine chalk deposition, indicating a short-lived increase in lake level. Stasiak (1963) states that there is an hiatus in sedimentation during the Subboreal. According to Stasiak (1963), the lake was much lower (4-5m) than present natural (i.e. pre-artificial lowering) during the Alleröd and younger Dryas. Lake level increased gradually during the Preboreal and Boreal, reaching levels higher than present during the later part of the Boreal. This increase in water level is thought to reflect the gradual melting out of the buried ice block. The lake was 2m higher than present level during the Atlantic (ca 7000-5000 yr B.P.). At this stage the lake would have had an area of ca 1500 ha (Stasiak, 1963). The lake was 2m lower than present during the Subboreal (5000-2,500 yr B.P.), with an area of ca 600ha and similar to present during the Subatlantic (2,500 to 0 yr B.P.), with an area of ca 1000ha. The possible climatic significance of the observed changes in water depth at Lake Kruklin have been discussed by Kondracki et al. (1966) and Kondracki (1969). Kondracki (1969) attributes the changes in water depth to changes in mean annual precipitation of the order of -285 to +80mm per year. In the status coding, low (1) is indicated by water levels below the modern natural level; intermediate (2) by levels similar to the modern level; high (3) by levels above the modern level. No attempt is made to code the shorter changes in water depth indicated by e.g. lacustrine chalk deposition during the Subboreal because of the inadequacy of the dating and of the elevation information. The record before 7000 yr B.P., believed to reflect ice melting, is not coded. References Czeczuga, B., 1969. The history of some lakes in the north-eastern region of Poland, based on chemical investigations of the sediments. Mittelungen Internationale Vereinigung fuer Theoretische und Angewandte Limnologie 17: 351-355. Czeczuga, B. and Golebiewski, Z., 1969. Chemical studies of the bed sediment of the lake Kruklin. Acta Hydrobiologia 11: 261-272. Kondracki, J., 1969. Changements du niveau des lacs comme résultat des oscillations du climat pendant l'holocène (Sur l'exemple du Ne de la Pologne). Geographia Polonica 17:119-131. Kondracki, J., Korolec, H., Stasiak, J., Szostak, M. and Wieckowski, K., 1966. Histoire des lacs masuriens. Verhandlugen Internationale Vereinigung fuer Theoretische und Angewandte Limnologie 16: 270- 273. Stasiak, J., 1963. Historia jeziora Kruklin w swietle osadów strefy litoralnej. Polska Akademia Nauk Instytut Geografii, Prace Geograficzne 42: 1-94. Radiocarbon Date n/a 11,390±210 yr B.P. pine trunks in fossil soil Coding pre-7000 yr B.P. not coded 7000-5000 yr B.P. high (3) 5000-2500 yr B.P. low (1) 2500-0 yr B.P. intermediate (2) Preliminary coding: April 1987; Final coding: December 1990.Coded by: SPH Lukcze, Poland Lake Lukcze (51.50 N, 23.00 E, 170m above see level) is a closed-basin lake in the Leczna Lake District, Lublin Polesie (Balaga, 1982). The basin probably originated through karstic solution and collapse. The lake consists of a nearly circular southern basin, which reaches a maximum depth of 8.9m, and a more elongated, shallower (maximum depth 6.4m), flat-bottomed northern basin, joined together by a narrow channel only ca 2.4m deep. There are several artificial channels that drain from the surrounding basin into the lake, but apparently no natural inflow or outflow. The lake has an area of 23ha. A 10.72m-long core from the centre of the southern basin in a water depth of 5.5m (Lukcze I) provides a sedimentary record back to ca 11,000 yr B.P. (Balaga, 1982). Two cores, taken about 10m apart and about 20m from the shore in the peatbog on the western side of the northern basin extend the record to ca 12,300 yr B.P. (Balaga, 1982; Pazdur et al., 1985). One of these cores is 3.5m long (Lukcze II) and consists solely of sedge- peat (Pazdur et al., 1985), the other is 4.50m long (Lukcze III) and includes intercalated layers of detritus or peaty gyttja towards the base (Balaga, 1982). Changes in relative water depth are reconstructed from changes in lithology and sedimentation rates. The chronology is established by ten radiocarbon dates (Balaga, 1982; Pazdur et al., 1985). We have assumed that the dates and depths given in Pazdur et al. (1985) are correct. However, it should be noted that Lukcze II is labelled as Profile TL in this reference. The basal sediments of both cores are silts (10.72m+ in Lukcze I, 4.30-4.50m in Lukcze III). The overlying unit in the marginal core (Lukcze III) is sedge-moss peat (3.80-4.30m), dated to between 12,330+160 (Gd-1183) and 10,680+190 (Gd-824) yr B.P. The presence of moss peat in the central core (Lukcze I) between 10.27-10.72m and again between 9.82-10.07m suggests the lake may have been dry for at least part of this interval. However, a short-lived interval of deeper water is registered by detritus gyttja deposition between 10.07-10.27m. The subsequent deposition of peaty gyttja (3.40-3.80m), overlain by calcareous gyttja (2.60-3.40m) in the marginal core indicates increased water depth after ca 10,680 yr B.P. This interval is represented by detrital gyttja deposition in the central core. The low sedimentation rate (0.07 cm/yr) in the lowermost part of the detrital gyttja unit is consistent with relatively deep water conditions. Balaga (1982) argues that the increase in water depth registered by the transition from moss peat to detrital gyttja in Lukcze I resulted from the sinking of the lake bed and the melting of dead ice at the beginning of the Holocene. A decrease in water depth after ca 9250 yr B.P. is indicated by renewed deposition of peaty gyttja in the marginal core (2.30-2.60m). There is no change in the lithology of the central core. However, the observed increase in sedimentation rate (0.12 cm/yr) is consistent with shallowing. The uppermost 2.30m of the marginal core consists of sedge-moss peat, suggesting relatively stable water depth since ca 8750 yr B.P. This is corroborated by the continuing deposition of detritus gyttja, at relatively constant sedimentation rates (0.09 cm/yr), in the centre of the lake. In the status coding, low (1) is indicated by moss peat deposition in the central core; intermediate (2) by detritus gyttja deposition in the central core and sedge moss peat in the marginal core; high (3) by peaty gyttja in the marginal core and low sedimentation rates in the central core; very high (4) by calcareous gyttja deposition in the marginal core. Reference Balaga, K., 1982. Vegetational history of the Lake Lukcze environment (Lublin Polesie, E. Poland) during the Late-Glacial and Holocene. Acta Palaeobotanica 22: 7-22. Pazdur, M.F., Awsiuk, R., Bluszcz, A., Goslar, T., Pazdur, A., Walanus, A. and Zastawny, A., 1985. Gliwice radiocarbon dates X. Radiocarbon 27: 52-73. Radiocarbon Dates Gd-1177 980±50 0.50-0.55m, sedge-moss peat, Lukcze II Gd-1178 6420±70 0.90-0.95m, sedge-moss peat, Lukcze II Gd-1179 7790±70 1.65-1.70m, sedge-moss peat, Lukcze II Gd-1180 9080±90 2.50-2.60m, peaty gyttja, Lukcze III Gd-822 10660±210 3.40-3.50m, peaty gyttja, Lukcze III, SS, ATO? hardwater effect Gd-824 10680±190 3.75-3.85m, peaty gyttja, Lukcze III, SS Gd-1181 10900±100 2.50-2.55m, sedge-moss peat, Lukcze II Gd-1182 10930±90 2.80-2.85m, sedge-moss peat, Lukcze II, ATY? Gd-825 11160±110 4.00-4.10m, peaty gyttja, Lukcze III (given as 11116±210 in text) Gd-1183 12330±160 4.25-4.30m, moss peat, Lukcze III (given as 12333±140 in text) Coding 12,300-10,950 yr B.P. low (1) 10,950-10,900 yr B.P. intermediate (2) 10,900-10,680 yr B.P. low (1) 10,680-10,600 yr B.P. high (3) 10,600- 9250 yr B.P. very high (4) 9250 - 8750 yr B.P. high (3) 8750 - 0 yr B.P. intermediate (2) Preliminary coding: March 1987; Final coding: October 1994 Coded by: SPH Steklin, Poland Lake Steklin (52 57'N, 19 E, 73.3m above see level) lies in the southwestern part of the Dobryzn Lake District (Noryskiewicz, 1982). The basin originated as a subglacial channel, and is consequently long, narrow and steep- sided. This channel is carved into a relatively flat morainic plateau (92-94m above see level). The lake has an area of 112.3 ha but a maximum width of only 340m. The maximum depth is 18.5m. The lake is fed by a permanent stream from a smaller lake, Lake Wygoda, and is drained by the Gnilszczyzna, a tributary of the Drwecu River. Terraces at 4m and 10m above modern lake level indicate that the lake has been higher than today. These terraces are undated. A 9.40m core, taken in a water depth of 7.5m from the western end of the lake provides a sedimentary record dating back to about 11,700 yr B.P. (Noryskiwicz, 1982). Changes in water depth are reconstructed from changes in lithology, mollusc and aquatic macrofossil assemblages, and from the presence and abundance of fish remains. Most of the core sediments are highly calcareous and have therefore not been radiocarbon dated. The chronology is based on a single date on organic silts from near the base of the core (Noryskiewicz, 1982; Pazdur et al., 1985), four dates from a peatbog profile to the west of the lake (Pazdur et al., 1985), and correlation with the regional pollen chronology (Ralska-Jasiewiczowa, 1990, pers. comm.). The basal sediments in the core (9.30-9.40m) are well-sorted inorganic sands, overlain by more organic, silty sands (9.20-9.30m). The sediments between 9.15-9.20m, which consist of organic silts containing detrital plant material, have been radiocarbon dated to 11,630±110 yr B.P. This unit is overlain by a thin layer of lake marl (9.10-9.15m) containing abundant mollusc shells, representing the onset of lacustrine conditions. The lake was relatively shallow. The overlying sediments (8.60-9.10m) are clayey gyttja, indicating deepening. The uppermost 8.60m of sediments consist of calcareous gyttja. According to the pollen, the transition from clayey to calcareous gyttja occurred at ca 10,200 yr B.P. The presence of fish scales and vertebrae within both the clayey and calcareous gyttja units suggests that the lake was relatively deep. The sporadic occurrence of molluscs characteristic of shallow, stagnant waters is probably due to inwashing. The rapid increase in both diversity and abundance of molluscs between 4.40-5.80m suggests that the coring site was nearer the source of inwashed material and implies that the lake was lower. This is also the only interval when ostracodes and aquatic plant macrofossils (specifically of Carex and Lycopus) are recorded, which is consistent with lowering. On the basis of extrapolation from the near-basal radiocarbon date, and assuming a constant sedimentation rate, this shallower interval is dated to between ca 7340 and 5570 yr B.P. On the basis of the pollen record, the interval of shallower conditions is dated to between 7050 and 4350 yr B.P. The subsequent decrease in mollusc abundance and the increased abundance of fish remains indicates that the lake became deeper. In the status coding, low (1) is indicated by marl deposition; intermediate (2) by gyttja deposition, with an abundant and diverse inwashed mollusc assemblage and aquatic plant macrofossils; high (3) by gyttja sedimentation with abundant fish remains. Reference Noryskiewicz, B., 1982. Lake Steklin - a reference site for the Dobrzyn-Chelmno Lake District, N. Poland. Report on palaeoecological studies for the IGCP-Project No. 158B. Acta Palaeobotanica 22: 65-83. Pazdur, M.F., Awsiuk, R., Bluszcz, A., Goslar, T., Pazdur, A., Walanus, A. and Zastawny, A., 1985. Gliwice radiocarbon dates X. Radiocarbon 27: 52-73. Radiocarbon Dates Gd-840 750±90 1.10m, peat, peatbog section, west of Steklin channel Gd-841 1870±60 2.30m, peat, peatbog section, west of Steklin channel Gd-842 2330±120 3.40m, peat, peatbog section, west of Steklin channel Gd-1303 4470±60 4.20m, peat, peatbog section, west of Steklin channel Gd-1115 11630±110 9.20-9.28m, silt with plant detritus, core from the lake Coding 11700-11500 yr B.P. low (1) 11500-7050 yr B.P. high (3) 7340-4350 yr B.P. intermediate (2) 5570- 0 yr B.P. high (3) Preliminary coding: March 1987; Final coding: December 1990 Coded by: SPH Wielke Gacno, Poland Wielke Gacno (53.73 N, 17.20 E, 130m above see level) lies in s subglacial channel in the sandy outwash plain of the Brda River (Hjelmroos-Ericsson, 1981). There are several lakes on this outwash plain, including Lake Charzykowskie and Ostrowite Lake. Wielkie Gacno was formerly joined to the adjacent Malo Gacno, but the two lakes are now separated by lake terrace deposits. The area of Wielke Gacno is 13.1ha. The mean water depth is 3.5m and the maximum water depth, which occurs in the northeastern part of the lake, is 6.1m. There is no surface inflow or outflow, but groundwater fluxes may play an important role in the lake water balance. The modern lake is oligotrophic and slightly alkaline. The catchment area has a radius of 15-20 km. The general stratigraphy of the lake bottom sediments is reconstructed from one longitudinal and five transverse transects across the basin. An 8.05m core, taken in a water depth of 5.05m in the deepest part of the lake, provides a pollen record back to ca 10,000 yr B.P. (Hjelmroos, 1981). The basal deposits are silty sands dated to the late glacial. These are overlain by algal gyttja, which grades in colour upwards from dark greenish-brown (5.50-8.0m in main core) to dark brown (3.85-5.50m in main core). The uppermost sediments (0-3.85m) are fine detritus gyttja. Changes in water level since ca 12,000 yr B.P. have been reconstructed from a transect of four cores (A1, A2, A3, B1) taken in the southwestern bay of the lake and are based on changes in lithology (proportion of coarse organic and minerogenic fractions), the sediment limit and aquatic macrofossil assemblages (Hjelmroos- Ericsson, 1981; Hjelmroos, 1982), according to the methods proposed by Digerfeldt (1986). Additional information on changes in water depth is provided by changes in aquatic pollen, diatom, Chironomid and Cladoceran assemblages, and in geochemistry (Brodin, 1985a, 1985b; Hjelmroos-Ericsson, 1981; Hjelmroos, 1981, 1982). The chronology is based on 23 radiocarbon dates. The age-depth curve does not follow a straight line, since the uppermost dates appear slightly older than predicted. Hjelmroos (1982) suggests that this is due to human impact through agriculture in the catchment, resulting in erosion and the incorporation older organic material into the lake sediments. Although the supposed errors are quite small, she applies a correction to the dates from the main core based on the assumption that sedimentation rates were constant throughout the history of the lake. Given the fact that the lake has varied in depth, this assumption is unlikely to hold. The chronology used here is therefore based on uncorrected radiocarbon dates, and differs slightly from that in Hjelmroos-Ericsson (1981) and Hjelmroos (1982). According to Hjelmroos (1982) there were five periods of lowered water level during the history of the lake. The oldest lowering, which occurred during WG1 and 2, was the strongest and is marked by an hiatus in sedimentation in core A1. The lake level was estimated to be ca 3m below presnt level. This interval is dated to between 10,100 and 9100 yr B.P. A second phase of lowered water level occurred during WG 3.2 and was again marked by an hiatus in core A1. The lake was estimated to be ca 2.7-2.8m lower than present. This interval is dated to between 7550-8450 yr B.P. Subsequent lowerings occurred during WG 4.2 (5500-6750 yr B.P.), during the later part of WG 5.1 and the early to middle part of WG 5.2 (4000-4800 yr B.P.), and during WG 6.2 and 7.1 (1860-2700 yr B.P.). Brodin (1985a, 1985b) shows that each of these intervals is characterised by increases in the proportion of littoral species in the chironomid assemblages, consistent with shallowing. In the status coding, low (1) is indicated by water-level lowerings of > 2.5m and resulting in an hiatus in core A1; intermediate (2) by water-level lowerings of < 2.5m and not resulting in an hiatus in core A1; high (3) by lake levels similar to present. References Brodin, Y.-W., 1985a. Lake history and climatic change in Northern Europe interpreted from subfossil Chironomidae (Diptera). Acta Universitatis Upsaliensis, Abstracts of Uppsala Dissertations from the Faculty of Science 787: 1-27. Brodin, Y.-W., 1985b. The Holocene development of Lake Wielke Gacno, Northern Poland, interpreted from remains of aquatic insects. Manuscript, from thesis, 34 pp. plus figures. Digerfeldt, G., 1986. Studies on past lake-level fluctuations. In Berglund, B. (ed.), Handbook of Holocene Palaeoecology and Palaeohydrology: 127-144. John Wiley & Sons, New York. Hjelmroos, M., 1981. The Post-Glacial development of Lake Wielke Gacno, NW-Poland. The human impact on the natural vegetation - recorded by means of pollen analysis and 14C dating. Acta Palaeobotanica 21: 129-144. Hjelmroos, M., 1982. The Holocene development of Lake Wielke Gacno, NW Poland. Acta Palaeobotanica 22: 23-46. Hjelmroos-Ericsson, M., 1981. Holocene development of Lake Wielke Gacno area, northwestern Poland. Ph.D thesis, Lund University, Sweden. Radiocarbon Dates Lu-1541 780±50 5.30-5.35m detritus gyttja, main core Lu-1637 810±50 wood from SE shore of the lake Lu-1540 1220±50 5.80-5.85m detritus gyttja, main core Lu-1613 1790±50 6.30-6.35m detritus gyttja, main core Lu-1612 2250±50 6.80-6.85m detritus gyttja, main core Lu-1611 2650±55 7.30-7.35m detritus gyttja, main core Lu-1610 3320±55 7.80-7.85m detritus gyttja, main core Lu-1609 3740±55 8.30-8.35m detritus gyttja, main core Lu-1608 4230±60 8.80-8.85m detritus gyttja, main core Lu-1470 4810±60 9.30-9.35m algal gyttja, main core Lu-1539 5130±60 9.50-9.55m algal gyttja, main core Lu-1538 5430±65 9.80-9.85m algal gyttja, main core Lu-1537 5950±65 10.30-10.35m algal gyttja, main core Lu-1469 6590±75 10.80-10.85m algal gyttja, main core Lu-1536 7160±65 11.30-11.35m algal gyttja, main core Lu-1535 8120±80 11.80-11.85m algal gyttja, main core Lu-1534 8350±80 12.30-12.35m algal gyttja, main core Lu-1533 8830±85 12.55-12.60m algal gyttja, main core Lu-1532 9280±90 12.80-12.85m algal gyttja, main core Lu-1531 9870±90 13.04-13.08m algal gyttja, main core Lu-1481 11000±100 3.35-3.40m clay gyttja, core A1 Lu-1480 11000±105 3.48-3.52m sandy clay gyttja, core A1 Lu-1679 11380±100 3.56-3.60m clayey algal gyttja, core A1 Lu-1678 11840±110 3.67-3.71m algal gyttja, core A1 Coding 12000-10100 yr B.P. high (3) 10100- 9100 yr B.P. low (1) 9100- 8450 yr B.P. high (3) 8450- 7550 yr B.P. low (1) 7550- 6750 yr B.P. high (3) 6750- 5500 yr B.P. intermediate (2) 5500- 4800 yr B.P. high (3) 4800- 4000 yr B.P. intermediate (2) 4000- 2700 yr B.P. high (3) 2700- 1860 yr B.P. intermediate (2) 1860- 0 yr B.P. high (3) Preliminary coding: February 1987; Final coding: May 1987 Coded by: SPH Comprida, Portugal Lagoa Comprida (39 45'N, 8 W, 1600m above sea level) is a moderate-sized lake in the Serra da Estrela, central Portugal. This granite and schist mountain range was glaciated during the Weichselian (Daveau, 1969). The Lagoa Comprida basin is probably of glacial origin (Janssen and Woldringh, 1981). The modern water level of the Lagoa Comprida is artificially high because the lake has been dammed. During times of high water a number of small depressions to the north of the lake become inundated, but it is unlikely that these depression were connected to the lake in the past (Janssen and Woldringh, 1981). Two cores (Lagoa Comprida I and II) from small (ca 0.15ha), shallow ponds in two of the closed depressions to the north of the lake provide a sedimentary record spanning most of the Holocene (Janssen, 1985; Janssen and Woldringh, 1981; Van den Brink and Janssen, 1985). These ponds are between 0.5-1.0m deep in early spring, but may dry out in the autumn (Janssen, 1988, pers. comm.). Changes in water depth are reconstructed from changes in sediment lithology and aquatic pollen assemblages. The chronology is established by nine radiocarbon dates. The Lagoa Comprida I core (Janssen and Woldringh, 1981; Van den Brink and Janssen, 1985) is about 5.3m long. The basal sediments are clays and clayey gyttja. A sample from 5.01-5.05m has been radiocarbon dated to 9200±270 yr B.P. (GrN-9918), which suggests that lacustrine sedimentation began around 9300 yr B.P. The overlying sediments (4.60-4.90m) are gyttja, suggesting relatively deep water. A decrease in water depth after about 8780 yr B.P. is suggested by sandy gyttja deposition between 4.20-4.60m. The aquatic pollen suite is dominated by Potamogeton although Ranunculaceae pollen is moderately abundant. A return to deeper water is indicated by gyttja deposition between 2.50-4.20m. The decline in abundance of both Ranunculaceae and Cyperaceae pollen above 4.0m is consistent with a gradual increase in water depth. Ranunculaceae pollen increases in abundance above 3.20m and Potamogeton disappears from the record above 2.90m, suggesting a gradual decrease in water depth. This decrease in depth culminated in the deposition of peat between 1.55- 2.50m. A prominent charcoal layer occurs between 1.50-1.55m. An increase in water depth is marked by the deposition of sandy gyttja above 1.50m. Van den Brink and Janssen (1985) argue that comparison of the terrestrial pollen records of the two Lagoa Comprida cores suggests that there may be hiatuses in the uppermost part of the Lagoa Comprida I core. A prominent chaocoal lens at 1.50-1.55m, lying between the peat and uppermost sandy gyttja, may mark one such hiatus in sedimentation. Since there may be hiatuses it is not possible to date the peat by interpolating between the radiocarbon dates from the upper metre and the base of the core. The Lagoa Comprida II core (Janssen, 1985; Van den Brink and Janssen, 1985), a 4.85m long core taken at the edge of a peatbog adjacent to the shallow pond, is thought to provide a more complete sedimentary record. The basal sediments are clays, overlain by sandy gyttja (4.60-4.75m) and gyttja with discrete moss layers (4.40- 4.60m). The moss layers suggest that the initial rise in water level was rapid. Correlation of the terrestrial pollen suggests that these units were deposited at the same time as the basal deposits of Lagoa Comprida I, which are also relatively coarse and contain organic debris. The overlying sediments (2.50-4.40m) are gyttja, indicating deep water. The aquatic pollen suite is characteristic of open-water communities (Van den Brink and Janssen, 1985) and includes Nymphaea and Potamogeton. Decreasing water depth after about 5000 yr B.P. is indicated by detritus gyttja (1.80-2.50m) deposition. This trend culminated between ca 3500 and 4300 yr B.P. when peat was deposited, the aquatic pollen suite was dominated by Cyperaceae and Ranunculaceae, and Potamgeton disappeared from the record. The deposition of gyttja between 1.0-1.32m indicates an increase in water depth. A sample from the middle of this unit (ca 1.15m) was radiocarbon dated to 3280±70 yr B.P. (GrN-11057). The abundance of Ranunculaceae pollen in this gyttja suggests that the water depth was shallower than during the previous phase of gyttja deposition. The overlying sediments (0.75-1.0m) are sandy gyttja and sandy detritus gyttja, indicating decreasing water depth. A prominent charcoal layer occurs between 0.60-0.75m. The uppermost sediments are peat, and indicate a decrease in water depth over the last 2000 yr. In the status coding, low (1) is indicated by peat deposition and abundant Ranunculaceae and Cyperaceae; intermediate (2) by sandy or detritus gyttja; moderately high (3) by gyttja where Ranunculaceae is still moderately abundant; high (4) by gyttja with pollen characteristic of open-water communities, including Potamogeton and Nymphaea. References Daveau, S., 1969. Structure et relief de la Serra da Estrela. Finisterra 7, 8: 31-63. Janssen, C.R. 1985. História da vegetação. In: Glaciacao da Serra da Estrela; aspectos do Quaternario da Orla Atlantica, Livro guia da prereuniao, I reuniao do Quaternario Iberico de Grupo de trabalho portugues para o estudo do Quaternario and Grupo espanol de trabajo del cuaternario. pp 66-72. Janssen, C.R. and Woldringh, R.E., 1981. A preliminary radiocarbon dated pollen sequence from the Serra da Estrela, Portugal. Finisterra 16: 299-309. Janssen, C.R., 1988. Personal communicationn. Letter. Van den Brink, L.M. and Janssen, C.R. 1985. The effect of human activities during cultural phases on the development of montane vegetation in the Serra da Estrela, Portugal. Review of Palaeobotany and Palynology 44: 193-215. Radiocarbon dates GrN-11056 850±90 ca 0.20m, peat, Lagoa Comprida II GrN-9913 1050±60 0.56-0.60m, sandy gyttja, Lagoa Comprida I GrN-9914 2680±80 0.86-0.90m, sandy gyttja, Lagoa Comprida I, ATO? GrN-9915 2680±100 1.00-1.04m, sandy gyttja, Lagoa Comprida I, ATO? GrN-11057 3280±70 ca 1.15m, gyttja, Lagoa Comprida II GrN-11058 4340±90 ca 1.90m, gyttja, Lagoa Comprida II GrN-9916 8310±160 4.30-4.34m, gyttja, Lagoa Comprida I GrN-9917 9080±200 4.76-4.80m, gyttja, Lagoa Comprida I GrN-9918 9200±270 5.01-5.05m, gyttja, Lagoa Comprida I Coding 9300-8780 yr B.P. high (4) 8780-8100 yr B.P. intermediate (2) 8100-5000 yr B.P. high (4) 5000-4300 yr B.P. intermediate (2) 4300-3500 yr B.P. low (1) 3500-2800 yr B.P. moderately high (3) 2800-2000 yr B.P. intermediate (2) 2000-0 yr B.P. low (1) Final coding: September 1988. Coded by SPH Madres, Spain The Laguna de las Madres (37 10'N, 6 51'W, ca 20m above sea level) is an enclosed, peat-filled depression 13km east of Huelva, southwest Spain (Stevenson, 1985). The basin, which is excavated into Plio-Pleistocene sands, originally drained to the sea. This outflow was stopped when dunes blocked the mouth of the river sometime before 4500 yr B.P. Two small streams flow into the northern end of the Laguna. The basin has been artificially drained for peat exploitation. Four cores provide a sedimentary record from the site: a 5.50m core from the centre of the lake (Menèndez Amor and FlorschÜtz, 1964), two short cores (LM1 and LM2, 2.64m and 2.84m respectively) from the southwestern end of the Laguna, near the former mouth, and a 2.86m-long core (LM3) from the northern end of the Laguna (Stevenson, 1985). Changes in water depth are reconstructed from changes in lithology and aquatic pollen. Core LM2 provides the best record of both changes in lithology and aquatic vegetation but is not radiocarbon dated. The chronology is established by correlation of the terrestrial pollen record from core LM2 with the central core from which there are two radiocarbon dates. There is also a single date on core LM3. The basal sediments in core LM2 are sands. Stevenson (1985) argues that the poor pollen preservation and the abundance of Isoetes spores in the bottom part of this unit (2.56-2.84m) indicates that there was outflow from the basin. The increase in Nuphar above 2.56m reflects increased water levels, which Stevenson (1985) suggests was due to drainage impedence when the mouth of the river was blocked by dunes. The sediments between 2.10- 2.20m are limnic clays. This unit is presumably equivalent to the gyttja found near the base(2.60-2.80m) of core LM3. A sample from near the top of the gyttja was radiocarbon dated to 4480±150 yr B.P. Thus lacustrine deposition in the Laguna began some time before 4500 yr B.P. A decrease in water level is marked by peat deposition overlying both the gyttja of core LM3 and the limnic clay of core LM2. The aquatic pollen is initially dominated by Cyperaceae, and subsequently by Filicales, and then marked by a sharp rise in the abundance of Nymphaea. The occurrence a prominent silt band between 0.90- 1.0m in core LM2 is consistent with a rise in water level and erosion of shore zone. This rise in water level is reflected by an increase in Potamogeton and Nymphaea between 1.30 and 1.65m in core LM3. A fall in water level after about 1000 yr B.P. is reflected by the disappearance of Nymphaea and the dominance of Cyperaceae and Filicales in both cores. In the status coding, low (1) is indicated by peat deposition and an aquatic assemblage dominated by Cyperaceae, Filicales or Typha; high (2) by either gyttja and limnic clay deposition or peat deposition with Nymphaea. Radiocarbon dates GrN-3258 2220±80 2.85-2.95m, peat, central core Beta-4224 4480±150 2.60-2.65m, peat, core LM3 GrN-3240 4550±75 4.60-4.70m, central core References Stevenson, A.C., 1985. Studies in the vegetational history of S.W. Spain. II. Palynological investigations at Laguna de las Madres, S.W. Spain. Journal of Biogeography 12: 293-314. Menèndez Amor, P.J. and FlorschÜtz, F., 1964. Resultados del anàlisis paleobotànico de una capa de turba en las cercanìas de Huelva (Andalucìa). Estudios Geololgcos XX: 183-186. Coding ca 5000-4440 yr B.P. high (2) 4440-2200 yr B.P. low (1) 2220-1000 yr B.P. high (2) 1000-0 yr B.P. low (1) Final coding: September 1991. Coded by SPH Padul, Spain Padul (37 2'N, 3 40'W, 785m above sea level) is a peatbog in the eastern foothills of the Sierra Nevada, about 20km from Granada, southern Spain. The basin is thought to be tectonic in origin (Pons and Reille, 1988a and 1988b). The site was originally investigated by Menéndez Amor and Florschütz (1962). Five cores (I, length unknown; II, 20m; IV, 50m; V, 100m; and VI, length unknown) provide a sedimentary record believed to date back to the Holsteinian interglacial (Menéndez Amor and Florschütz, 1962, 1963, 1964; Florschütz et al., 1971; Vogel and Waterbolk, 1972; Taayke, 1988, pers. comm.). The stratigraphy of all the cores appears to be similar. The upper 72m consists of alternating peat and lake marl, between 72-99.4m there are sands and sandy loams, and below 99.4m there is dark clay. There are 25 radiocarbon dates on these cores (Menéndez Amor and Florschütz, 1964; Vogel and Waterbolk, 1972; Taayke, 1988, pers. comm.), but two are infinite (GrN-2657 and GrN-2630) and only seven have yielded ages less than 30,000 yr B.P. Changes in water depth since 30,000 yr B.P. can be reconstructed from changes in sediment lithology and aquatic pollen assemblages in the upper 8m of these cores. Between 5.25-8.0m the deposits are lake marls, indicating relatively deep water. The presence of Potamogeton is consistent with this interpretation. A sample from 6.9m has been radiocarbon dated to 30,270±450 yr B.P. (GrN-2955), while a sample from 5.93m has been dated to 17,000±145 yr B.P. (GrN-2327). Florschütz et al. (1971) argue that this extremely low sedimentation rate (0.07 mm/yr), coincident with high values of Gramineae, Cyperaceae and Typha, is consistent with a depositional hiatus some time between 30,000 and 18,000 yr B.P. The uppermost 5.25m of the core is peat, indicating decreased water depth from ca 15,200 yr B.P. The marked increase in Typha, and the presence of Ranunculus and Sparganium-type, is consistent with decreased depth. The top of the peat has been radiocarbon dated to 4980±60 yr B.P., which suggests that conditions became drier in the last 5,000 yr B.P. so that peat has been stopped forming. The site has been reinvestigated by Pons and Reille (1988a and 1988b). An 8m-long core (Padul III), taken near the site cored by Menéndez Amor and Florschütz, provides a record back to ca 30,000 yr B.P. The chronology is established by 17 radiocarbon dates. The basal sediments (7.0-8.0m) are peats. A sample from ca 7.75-8.0m has been radiocarbon dated to 29,300±600 yr B.P., while a sample from 7.10-7.20m has been dated to 23,600±500 yr B.P. The aquatic assemblage is characterised by abundant Cyperaceae and Sparganium, and the presence of Myriophyllum, and is consistent with relatively shallow conditions. This interval of peat deposition can be correlated with the depositional hiatus postulated by Florschütz et al. (1971). The overlying sediments (5.35-7.0m) are marls, indicating an increase in water depth sometime between 22,175 and 22,350 yr B.P. The moderate and variable abundance of Cyperaceae in the lower part of the marl is consistent with an increase in depth. Maximum water depth appears to have been reached after ca 18,750 yr B.P., when values for Cyperaceae are extremely low and no other aquatics are recorded. The overlying sediments (4.95-5.35m) are peats, indicating a decrease in water depth. The increased abundance of Cyperaceae and Sparganium is consistent with shallow conditions. A sample from the base of the unit (5.25- 5.35m) has been radiocarbon dated to 15,200±80 yr B.P. A similar transition from marl to peat in the older cores (at ca 5.25m) also occurs at 15,200 yr B.P. The overlying sediments (4.0-4.95m) are marl, indicating an increase in water depth around 12,400 yr B.P. The reduced abundance of Cyperaceae and Sparganium is consistent with increased depth. A sample from near the top of the marl (4.05-4.30m) has been radiocarbon dated to 12,080±180 yr B.P. This interval of increased water depth is not registered in the older cores. The uppermost sediments (0.0-4.0m) are peat, indicating a decrease in water depth sometime between 10,300- 11,500 yr B.P. The aquatic assemblage is characterised by abundant Cyperaceae, Typha and Sparganium. A sample from near the top of the core (0.1-0.25m) has been radiocarbon dated to 4450±60 yr B.P. The absence of peat deposits over the last 4000 or so years, shown in all the cores from this site, is consistent with maximum aridity in the late Holocene. In the status coding, an hiatus is registered as (0); low (1) is indicated by peat deposition; intermediate (2) by marl deposition with moderately abundant Cyperaceae and Myriophyllum; high (3) by marl deposition with low Cyperaceae. Radiocarbon dates GrN-6209 4450±60 ca 0.1-0.25m peat, Padul III GrN-2185 4980±60 0.11m peat, organic residue, Padul IV GrN-6210 5460±70 ca 0.9-1.0m peat, Padul III GrN-6394 5980±70 ca 1.2-1.3m peat, Padul III GrN-6211 6340±70 ca 1.5-1.6m peat, Padul III GrN-1949 6360±85 1.40m peat, Padul II GrN-2187 6750±90 1.87m peat, organic residue, Padul IV GrN-6005 7840±100 ca 1.9-2.0m peat, Padul III GrN-6393 8200±80 ca 2.4-2.5m peat, Padul III GrN-6392 9300±90 ca 3.0-3.1m peat, Padul III GrN-6006 9930±110 ca 3.9-4.0m peat, Padul III Reversal GrN-6212 10000±110 ca 3.50-3.60m peat, Padul III GrN-2191 10110±85 3.87m peat, organic residue, Padul IV GrN-1950 10470±120 3.90m peat, organic residue, Padul II GrN-6391 12080±180 ca 4.0-4.3m clay, Padul III GrN-2952 13000±100 4.40m peat, organic residue, Padul V GrN-6007 13200±150 ca 5.15-5.25m peat, Padul III GrN-6008 15200±180 ca 5.25-5.35m peat, Padul III GrN-2327 17000±145 5.87m peat (lake sediment?), organic residue, Padul IV GrN-6390 18300±300 ca 5.7-6.0m clay, Padul III GrN-6714 19100±160 ca 6.0-6.3 clay, Padul III GrN-6389 19800±220 ca 6.5-6.8m clay, Padul III GrN-6009 23600±500 ca 7.1-7.2m peat, Padul III GrN-6388 29300±600 ca 7.8-8.0m peat, Padul III GrN-2955 30270±450 6.90m peat (lake sediment?), organic residue, Padul V GrN-850 32830±1200 7.90m peat (lake sediment?), organic residue, Padul II GrN-2145 34370±900 7.37m peat (lake sediment?), organic residue, Padul IV GrN-2146 38540±1300 8.37m peat, organic residue, Padul IV GrN-4805 39150±920 12.35-12.45m peat, organic residue, Padul VI GrN-4943 41400±1000 peat, organic residue, Padul VI GrN-2658 43220±900 9.37m peat, Padul IV GrN-5026 45000±330 11.87-12.32m peat, organic extract, Padul VI GrN-2192 >46000 peat, organic residue, Padul IV GrN-2147 46440±2000 10.37m peat, organic residue, Padul IV GrN-4808 >47000 12.50-12.55m peat, organic residue, Padul VI GrN-4956 49000±2500 peat, organic residue, Padul VI GrN-8645 49150+3630 15.02-15.47m peat, Padul I -2480 GrN-2657 >51000 10.87m peat, organic residue, Padul IV GrN-2630 >54000 11.37m peat, organic residue, Padul IV GrN-7611 56700±500 peat, organic extract, Padul I GrN-8190 57200±500 15.02-15.47m peat, organic extract, Padul I GrN-7559 58500+1100 13.67-14.57m peat, Padul I -1000 Note: The depths of samples at Padul III are not given in Pons and Reille (1988a and 1988b) but approximate depths have assessed from enclosed diagram (Pons and Reille, 1988b). References Florschütz, F., Menéndez Amor, J. and Wijmstra, T.A., 1971. Palynology of a thick Quaternary succession in southern Spain. Palaeogeography, Palaeoclimatology, Palaeoecology 10: 233-264. Menéndez Amor, J. and Florschütz, F., 1962. Un aspect de la végétation en Espagne méridionale durant la dernière glaciation et l'Holocène. Geologie en Mijnbouw 41: 131-134. Menéndez Amor, J. and Florschütz, F., 1963. Sur les éléments steppiques dans la végétation quaternaire de l'Espagne. Boletín de la Real Sociedad Española de Historia Natural (Sección Geológica) 61: 121- 133. Menéndez Amor, J. and Florschütz, F., 1964. Results of the preliminary palynological investigation of samples from a 50m boring in southern Spain. Boletín de la Real Sociedad Española de Historia Natural (Sección Geológica) 62: 251-255. Pons, A. and Reille, M., 1988a. Nouvelles recherches pollenanalytiques à Padul (Granada): la fin du dernier glaciaire et l'Holocene. In: López-Vera, F. (ed), Quaternary Climate in Western Mediterranean. Universidad Autónoma de Madrid. 405-420 pp. Pons, A. and Reille, M., 1988b. The Holocene- and Upper Pleistocene pollen record from Padul (Granada, Spain): a new study. Palaeogeography, Palaeoclimatology, Palaeoecology 66: 243-263. Taayke, E., 1988. pers. comm. Letter. Vogel, J.C. and Waterbolk, H.T., 1972. Groningen radiocarbon dates X. Radiocarbon 14: 6-110. Coding pre 30000-22175 yr B.P. low (1) 22335-18750 yr B.P. intermediate (2) 18750-15200 yr B.P. high (3) 15600-12400 yr B.P. low (1) 12400-10300 yr B.P. high (3) 11500-4400 yr B.P. low (1) 4400-0 yr B.P. hiatus (0) Final coding: March 1988 Coded by SPH Sanguijuelas, Spain La Laguna de las Sanguijuelas (42.10 N, 6.73 W, 1050m above sea level) is a lake at high elevation near the Spanish-Portuguese border. The basin is thought to be of glacial origin, and to have been occupied by a lake since the retreat of the glacier (Menéndez Amor and Florschütz, 1961). The region is characterised by Cambrian and Silurian rocks, mostly granitic. A single core (8.6m long) provides a sedimentary record back to ca 15,500 yr B.P. (Menéndez Amor and Florschütz, 1961, 1963). Changes in water depth are based on changes in lithology, sedimentation rates and aquatic pollen assemblages. The chronology is based on 7 radiocarbon dates (Menéndez Amor and Florschütz, 1961). The core bottoms out in an impenetrable clay layer (856-860cm). The overlying unit (835-856cm) is gyttja, indicating the onset of lacustrine conditions in the basin. The aquatic pollen assemblage is dominated by Isoetes with some Cyperaceae. The sediments between 805-835cm are sandy clay. The presence of sand suggests that the lake became shallower. An increase in Filicales is consistent with this interpretation. The sediments between 260-805cm are gyttja, suggesting increased water depth. A sample from ca 775cm has been radiocarbon dated to 13,700±300 yr B.P., indicating that this increase in water depth occurred ca 14,000- 15,000 yr B.P. The low initial sedimentation rates (0.0023 mm/yr), and the abundant representation of Isoetes and Cyperaceae, are consistent with moderately shallow conditions initially. A decline in Cyperaceae above 780 cm, and in Isoetes above ca 700 cm, coupled with an increase in sedimentation rates (0.004-0.006 mm/yr), is consistent with a gradual increase in water depth. The absence of both Cyperaceae and Isoetes above 310 cm, and a further increase in sedimentation rate (0.007 mm/yr) is consistent with maximum depth after ca 5750 yr B.P. The overlying unit (215-260cm) is peaty gyttja, indicating shallowing after ca 4475 yr B.P. There is a gradual increase in the peatiness of the sediments, culminating in peat deposition between 35-155cm. This lithological change is accompanied by an increase in Cyperaceae and the occasional representation of Sphagnum. The uppermost sediments (0-35cm) are gyttja, indicating an increase in water depth after ca 520 yr B.P. The aquatic assemblage is characterised by the presence of Cyperaceae. In the status coding, low (1) is indicated by peat deposition or by sandy clay deposition; moderately low (2) by peaty gyttja deposition; intermediate (3) by gyttja deposition with abundant Isoetes and Cyperaceae, and low sedimentation rates; high (4) by gyttja deposition with moderate representation of Isoetes and Cyperaceae; very high (5) by gyttja deposition and the absence of Isoetes and Cyperaceae. References Menéndez Amor, J. and Florschütz, F., 1961. Contribución al conocimiento de la historia de la vegetación en España durante el Cuaternario. Estudios Geologicos XVII: 83-99. Menéndez Amor, J. and Florschütz, F., 1963. Sur les éléments steppiques dans la végétation quaternaire de l'Espagne. Boletín de la Real Sociedad Española de Historia Natural (Sección Geológica) 61: 121- 133. Radiocarbon Dates Gro-698 730±80 peat, ca 0.50m Gro-1002 4190±60 peaty gyttja, ca 1.95m Gro-704 6670±145 gyttja, ca 3.75m Gro-703 8160±190 gyttja, ca 5.10m Gro-688 11585±220 gyttja, ca 7.05m Gro-702 12830±280 gyttja, ca 7.55m Gro-705 13700±300 gyttja, ca 7.75m Coding 15500-14000 yr B.P. low (1) 15000-11600 yr B.P. intermediate (3) 11600- 5750 yr B.P. high (4) 5750- 4475 yr B.P. very high (5) 4475- 3200 yr B.P. moderately low (2) 3200- 520 yr B.P. low (1) 520- 0 yr B.P. high (4) Preliminary coding: January 1987; Final coding: August 1988 Coded by: SPH Ageröds mosse, Sweden Ageröds mosse (56 56'N, 13 26'E, 55m above sea level) is a raised bog in the Rönneholm-Ageröds basin, north of Ringsjön, central Skåne. Ageröds mosse has an area of ca 155 ha. The adjacent raised bog, Rönneholms mosse, is more than twice as large. The Rönneholm-Ageröds basin was formerly occupied by a lake. The stratigraphy of the former lake deposits has been reconstructed from 30 borings (Nilsson, 1964, 1967). These cores show a general sequence from basal clay gyttjas, through more- or less-detrital gyttjas, into peats. Nilsson (1964) reconstructed changes in water level in the Ageröd basin on the basis of changes in lithology and the position of the sediment limit, and of changes in the aquatic pollen assemblages. The chronology is based on 33 radiocarbon dates (Östlund and Engstrani, 1963). According to Nilsson (1964), the lake was low during the middle part of the Boreal, reached its maximum depth during the early part of the Atlantic, and experienced a second lowering during the later Atlantic. This second lowering was not as large as that during the Boreal. The lake rose in a step-like fashion from the early Sub-boreal, reaching a maximum in the Subatlantic. Harrison and Digerfeldt (1993) have presented a summary of the lake status history of Ageröds mosse. The status codings given here are derived from that summary. Radiocarbon dates St-976 430±80 peat, 34-38cm, a dug wall, central bog St-977 1090±85 peat, 85-90cm, a dug wall, central bog St-978 1250±85 peat, 94-98cm, a dug wall, central bog St-979 1495±85 peat, 118-121cm, core P100 St-982 1645±95 peat, 122-127cm, core P100 St-983 1935±80 peat, 169-175cm, core P100 St-985 2140±85 peat, 175-181cm, core P100 St-986 2205±85 peat, 181-186cm, core P100 St-987 2845±90 peat, 190-194cm, core P100 St-988 3205±85 peat, 211-216cm, core P100 St-989 3315±90 peat, 218-224cm, core P100 St-1050 3560±65 peat, 232-235cm, core P100 St-990 4000±90 peat, 256-260cm, core P100 St-996 4510±80 peat, 269-299cm, core P100 St-997 5090±80 peat, 325-329cm, core P100 St-998 5060±90 peat, 329-333cm, core P100 St-792 5950±95 peat, 371-375cm, core P100 St-790 6170±120 peat, 375-379cm, core P100 St-1000 6570±95 peat, 404-409cm, core P100 St-791 6800±100 peat, 427-431cm, core P100 St-794 7320±100 muddy peat, 477-481cm, core P100 St-1001 7950±85 gyttja, 507-509cm, core P100 St-1002 8160±110 algae gyttja, 536.5-539cm, core P100 St-1004 8450±160 algae gyttja, 540-542cm, core P100 St-795 8550±110 algae gyttja, 542-544cm, core P100 St-796 9180±110 algae gyttja, 546.5-549cm, core P100 St-797 8980±120 algae gyttja, 551.5-554cm, core P100 St-1018 9590±120 algae gyttja, 561-563cm, core P100 St-800 9590±160 fine detritus-lime gyttja, 563-566cm, core P100 St-801 9880±160 fine detritus-lime gyttja, 566-569cm, core P100 St-805 9920±150 fine detritus-lime gyttja, 569-572cm, core P100 St-799 10430±180 clay gyttja, 572-574cm, core P100 St-798 10680±280 clay gyttja, 574.5-578cm, core P100 References Digerfeldt, G., 1986. Studies on past lake-level fluctuations. In Berglund, B. (ed.), Handbook of Holocene Palaeoecology and Palaeohydrology: 127-144. John Wiley & Sons, New York. Harrison, S.P. and Digerfeldt, G., 1993. European lakes as palaeohydrological and palaeoclimatic indicators. Quaternary Science Reviews 12: 233-248. Nilsson, T., 1964. Entwicklungsgeschichtliche Studien im Ageröds mosse, Schonen. Lunds Universitets Årsskrift. N.F. Avd. 2. Bd 59: 34 pp. Nilsson, T., 1967. Pollenanalytische datierung mesolitischer siedlungen im Randgebiet des Ageröds mosse im mittleren Schonen. Acta Universitatis Lundensis II 16: 1-80. Östlund, H.G. and Engstrani, L.G., 1963. Stockholm natural radiocarbon measurements V. Radiocarbon 5: 203-227. Coding 10000-9500 yr B.P. high (3) 9500-9300 yr B.P. intermediate (2) 9300-8700 yr B.P. low (1) 8700-7600 yr B.P. intermediate (2) 7600-6300 yr B.P. high (3) 6300-5800 yr B.P. intermediate (2) 5800-3700 yr B.P. low (1) 3700-3100 yr B.P. intermediate (2) 3100-0 yr B.P. high (3) Final coding: June 1989 Coded by: GD and SPH Bjäresjö, Sweden Lake Bjäresjö (55 27'N, 13 45'E, 48m above sea level) is a small lake in southern Sweden. The lake has an area of ca 2ha and a maximum depth of 1.7m. There is an outlet to the Svartån. The basin was formed by melting of dead-ice. The basin was a bog during the early and mid-Holocene and was a lake after ca 2700 yr B.P. (Gaillard and Berglund, 1988). The lake was artificially lowered by canalization in 1888 AD. The catchment area is ca 10ha. The bedrock in the catchment is Cretaceous limestone (Ekström, 1950). The stratigraphy of the lake deposits has been reconstructed from 5 transects, with at least 27 cores taken across the basin (Gaillard and Berglund, 1988; Gaillard et al., 1991). Changes in the position of the sediment limit were established from a transect (section C) across the central part of the basin. Section C has 11 cores (cores C01-CO4 and cores C1-C7) taken at distances between 35m and 200m from the western lake shore. The basal sediment is 3m+ of peat. The overlying sediment is clayey fine detritus gyttja with two inter-layers of clayey coarse detritus gyttja. The sediment sequences are generally similar in each core. Gaillard and Berglund (1988) and Gaillard et al. (1991) have reconstructed lake-level changes since ca 2700 yr B.P. on the basis of changes in lithology, aquatic plant macrofossil and diatom assemblages following the method described in Digerfeldt (1986). The record of changes in relative depth presented here follows these reconstructions. The chronology is base on six radiocarbon dates from core C3. A lake-level curve based on the status codings has been presented in Harrison and Digerfeldt (1993). A relatively low lake level ca 2700 yr B.P. is indicated by the deposition of clayey coarse detritus gyttja in the central part of the basin. The diatom assemblage in the central core (core C3, 125m from the western shore) is dominated by Fragilaria species, consistent with shallow conditions. The replacement of clayey coarse detritus gyttja by clayey fine detritus gyttja in the central part of the basin indicates an increase in water level between ca 2400-1600 yr B.P. The aquatic pollen assemblage in core C3 is characterised by Lemna minor, Potamogeton, and Myriophyllum spicatum, consistent with moderately deep water. Deposition of clayey coarse detritus gyttja in the central part of the basin, indicates a decrease in water level after ca 1600 yr B.P. The aquatic pollen assemblage in core C3 is characterised by Myriophyllum spicatum, Equisetum and Nuphar. The disappearance of Potamogeton and the presence of Equisetum is consistent with shallowing. A slight increase in water level after ca 800 yr B.P. is indicated by a sediment limit close to the shore (core C5, 75m from the western shore) and the deposition of clayey fine detritus gyttja in the central cores. Abundant planktonic diatoms, such as Cyclotella spp. are present in core C3, consistent with deeper water. A sediment limit up to core C6 (50m from the western shore), with continuous clayey fine detritus gyttja deposition in the central part of the basin, indicates a continuous increase in water level after ca 400 yr B.P. In the status coding, low (1) is indicated by clay coarse detritus gyttja deposition in the central part of the basin; intermediate (2) by clayey fine detritus gyttja deposition in core C5; high (3) by clayey fine detritus gyttja deposition in core C6. Radiocarbon dates Lu-2491 1240±45 yr B.P. 264.5-267.5cm, coarse gyttja, core C3 Lu-2490 1310±45 yr B.P. 270-273cm, coarse gyttja, core C3 Lu-2489 1810±50 yr B.P. 302-305cm, coarse gyttja, core C3 Lu-2488 2760±50 yr B.P. 357-360cm, coarse gyttja, core C3 Lu-2486 2680±50 yr B.P. 369-375cm, moss peat, core C3 Lu-2487 2690±60 yr B.P. 361-364cm, moss peat, core C3 References Ekström, G., 1950. Skånes åkerjordsområden. Socker 6: 53. Malmö (English summary). Gaillard M-J., and Berglund, B.E., 1988. Land-use history during the last 2700 years in the area of Bjäresjö, Southern Sweden. In: Birks, H.H., Kaland, P.E. and Moe, D. (eds.), The cultural landscape - Past, Present and Future. Cambridge University Press, pp 409-428. Gaillard M-J., Dearing, J.A., El-Daoushy, F., Enell, M. and Håkansson, H., 1991. A late Holocene record of land-use history, soil erosion, lake trophy and lake-level fluctuations at Bjäresjösjön (South Sweden). Journal of Paleolimnology 6: 51-81. Harrison, S.P. and Digerfeldt, G., 1993. European lakes as palaeohydrological and palaeoclimatic indicators. Quaternary Science Reviews 12: 233-248. Håkansson, S., 1986. University of Lund radiocarbon dates XIX. Radiocarbon 30: 1111-1132. Coding 2700-2400 yr B.P. low (1) 2400-1600 yr B.P. intermediate (2) 1600-800 yr B.P. low (1) 800-400 yr B.P. intermediate (2) 400-0 yr B.P. high (3) Final coding: June 1989. Coded by GD, SPH and GY Bysjön, Sweden Lake Bysjön (55 40'N, 13 32'E, 22m above sea level) is a small lake on the Vomb Plain, southern Sweden. The lake has an area of 12ha and a maximum water depth of ca 8m. There is an outlet northwestwards to the Klingvallsån but no surface channelled inflow to the lake. The water balance is dominated by groundwater (Digerfeldt, 1988). The catchment area is ca 200ha. The Vomb Plain consists mainly of glaciofluvial and glaciolacustrine sand and gravel (Ekström, 1961). The underlying bedrock is Cretaceous limestone. The lake lies in a kettle hole which originated from melting of dead-ice during deglaciation about 11200 yr B.P. (Håkansson, 1986; Digerfeldt, 1988). The lake level was lowered by 1-1.5m and the area reduced by 6ha through artificial drainage in 1892 AD (Digerfeldt, 1988). The stratigraphy of the lake deposits has been reconstructed from a transect of seven cores taken at distances between 45m and 80m from the shore (cores 45m, 50m, 55m, 60m, 65m, 70m and 80m), a core from the centre of the lake (core B taken in a water depth of 7.8m) and an additional nearshore core (core C) (Digerfeldt, 1988). The basal sediment is terrestrial peat (8.1-8.2m), overlain by sand (7.6-8.1m in core B). The overlying sediment is algal gyttja (7.5-7.6m), lake marl (6.9-7.5m) and calcareous gyttja (4.2-6.9m). The uppermost sediment is algal gyttja (0-4.2m in core B). Digerfeldt (1988) has reconstructed lake-level changes during the Holocene on the basis of changes in lithology, sediment limit and aquatic assemblages following the method described in Digerfeldt (1986). The record of changes in relative depth presented here follows this reconstruction. A lake-level curve based on the status codings has been presented in Harrison and Digerfeldt (1993). There is a single radiocarbon date on the basal peat from core 80m (Håkansson, 1986). No radiocarbon datings were carried out on the lacustrine deposits because of the high carbonate content and the possibility of hardwater errors. The chronology is therefore based on pollen correlation with Ageröds mosse, a radiocarbon-dated site about 25 km away (Digerfeldt, 1988). An interval of lowered water level at the boundary of pollen zone PO/BO1 is indicated by a lowering of sediment limit. Algal gyttja dating to this interval is only found in cores 65m, 70m and 80m. Digerfeldt (1988) suggests that, at the culmination of this shallow interval around 9000 yr B.P., the lake was ca 5-6m lower than present. An increase in the sediment limit occurred during pollen zone BO1 and BO2: lacustrine sediment is found in core 55m during BO1 and in core 60m during BO2 respectively. Sediment from pollen zone AT1 is found in core 65m, but is missing from sites closer to the shore, indicating a lowering of the sediment limit and decreased water depth between ca 5700 and 5200 yr B.P. A thin layer of sandy gyttja, which has a minerogenic content up to ca 70%, is found in core 65m, consistent with shallowing. The layer of sandy gyttja is found in core 70m, dated to the later part of pollen zone AT2, indicating that the maximum lowering was ca 3m lower than the present (Digerfeldt, 1988). An increase in the water depth during pollen zone SB1 is indicated by the presence of lacustrine sediments in cores 55m, 50m and 45m. The lacustrine unit becomes thinner towards the shore. A decrease in water depth at the boundary between pollen zones SB1 and SB2 is indicated by a very low sediment limit (below core 70m), and lacustrine sediment with a minerogenic content up to ca 95% in cores 70 and 80m. Digerfeldt (1988) suggests the lake level was ca 4-5m lower than the present at ca 4800-4400 yr B.P. (Digerfeldt, 1988). Sediment from zone SB2 is well represented at all sites in the transect, indicating an increase in water depth between ca 2900 and 1900 yr B.P. Sediment limit was lowered in pollen zone SA1, with lacustrine sediment only found in cores 70m and 80m. Pure sands were found in cores 65m and 60m, consistent with a decrease in water depth. At the culmination of shallowing ca 1900-900 yr B.P. the lake level was 2-3m lower than present (Digerfeldt, 1988). Throughout most of zone SA2 there was a progressive increase in the position of the sediment limit up to core 45m, indicating a gradual increase in water depth up to present. In the status coding, low (1) is indicated by a sediment limit 3m or more below present and high minerogenic content of sediments in the central cores; intermediate (2) by a sediment limit of ca 2m below present; high (3) by a sediment limit similar to present and fine lacustrine sediments with low minerogenic content in the central core. References Digerfeldt, G., 1986. Studies on past lake-level fluctuations. In Berglund, B. (ed.), Handbook of Holocene Palaeoecology and Palaeohydrology: 127-144. John Wiley & Sons, New York. Digerfeldt, G., 1988. Reconstruction and regional correlation of Holocene lake-level fluctuations in Lake Bysjön, South Sweden. Boreas 17: 165-182. Ekström, G., 1961. Beskrivning till kartbladet Revinge. Sveriges Geologiska Undersökning Ad 3: 66pp. Harrison, S.P. and Digerfeldt, G., 1993. European lakes as palaeohydrological and palaeoclimatic indicators. Quaternary Science Reviews 12: 233-248. Håkansson, S. 1986. University of Lund radiocarbon dates XIX. Radiocarbon 30: 1111-1132. Radiocarbon date Lu-2383 11220±100 peat, 8.1-8.2m, core 80m Coding 10000-9800 yr B.P. high (3) 9800-8600 yr B.P. intermediate (2) 9600-8600 yr B.P. low (1) 8600-8000 yr B.P. intermediate (2) 8000-6100 yr B.P. high (3) 6100-5700 yr B.P. intermediate (2) 5700-5200 yr B.P. low (1) 5200-4800 yr B.P. intermediate (2) 4800-4400 yr B.P. low (1) 4400-2900 yr B.P. intermediate (2) 2900-1900 yr B.P. high (3) 1900-900 yr B.P. intermediate (2) 900-0 yr B.P. high (3) Final coding: June 1989. Coded by GD, SPH and GY Juokojauratj, Sweden Juokojauratj (66 36'N, 19 16'E, ca 400m above sea level) is a small (1.3ha) lake in the Luleälv River valley in northern Sweden. The water depth is 1.5m. The lake has no major inflow, and there is only one small outlet to the north. Water is supplied by wells in the mire complex situated to the west of the lake (Segerström, 1990). The lake is an oligotrophic forest lake and aquatic plants are sparse. Geologically the basin is mainly characterised by granites (Ödman, 1957) and the surfacial deposits are fluvioglacial moraines and sand (Fromm, 1965). The lake lies above the highest mid-Holocene shoreline and was probably formed as the ice retreated ca 9500-9000 yr B.P. (Segerström, 1990). No indication of prehistoric settlement or agriculture was found in this basin, and even today the human influence is minor (Segerström, 1990). A 1.75m-long core from the lake provides a sedimentary record back to ca 9000 yr B.P. (Segerström, 1990). Changes in relative water depth are based on changes in lithology, algal, Cladocera, aquatic pollen and macrofossil assemblages (Segerström, 1990; Engelmark, personal communication, 1994). Although Segerström (1990) states that the pollen record shows no major changes in lake status, we note that there are changes in aquatic pollen that seem to be consistent with other evidence for changes in lake depth. The chronology is based on pollen correlation with the regional pollen stratigraphy (Huntley and Birks, 1983; Segerström, 1990) and comparison with Kvarnmyran, a radiocarbon-dated site ca 60km to the east but also in the Luleälv valley. There are three fixed points in the pollen chronology: 2800 yr B.P. at 50cm, 4000 yr B.P. at 110cm and 8000 yr B.P. at 160cm. The first reference point is related to the expansion of Picea between 2500- 3000 yr B.P., an event dated at Kvarnmyran to 2970±215 yr B.P. The second reference point is related to the interval of abundant Betula and Alnus between 4000-5000 yr B.P., associated with a date of 5160±165 yr B.P. at Kvarnmyran. The third reference point is the expansion of Alnus, which is dated to 8000 yr B.P. in northern Fennoscandia (Huntley and Birks, 1983) The basal sediment (below 170cm) is sand, probably of fluvioglacial origin. The overlying sediment (170-150cm) is algal gyttja, with abundant algal microfossils (Desmidiaceae), suggesting shallow water. The absence of Bosmina in the Cladoceran assemblage below 140cm and sparsity of Pediastrum (<5% below 150cm) are consistent with shallow water. Below 160cm the aquatic pollen assemblage is characterised by Nuphar and Potamogeton. There is a transition to an assemblage with Menyanthes, Myriophyllum and Sphagnum above 160cm. This shift suggests decreased water depth, consistent with the other evidence of shallowing. The unit belongs to pollen zones a and the lower part b (Boreal and early Atlantic: Segerström, 1990), and is dated to ca 8800-7200 yr B.P. The overlying sediment is lacustrine gyttja (150-0cm), reflecting moderately deep water after ca 7200 yr B.P. Biological and lithological changes allow this unit to be subdivided. In the lowest part of gyttja (150-100cm), planktonic Cladocera (Bosmina) increase to 10%, consistent with increased water depth. The aquatic assemblage is characterised by Myriophyllum and Sparganium, and the disappearance of Menyanthes, consistent with increasing depth. An increase in Pediastrum (10-13%) and in Nymphaeaceae (10%) macrofossils are also consistent with this interpretation. This subunit belongs to pollen zone b, characterised by abundant Betula and Alnus (130-110cm), and is dated to ca 7200-3800 yr B.P. From 100cm to 60cm, the abundance of Potamogeton, Myriophyllum, Nymphaea and Nuphar, suggests a further increase in water depth. Pediastrum reaches its maximum abundance, consistent with deep water. The virtual absence of Desmidiaceae is consistent with this interpretation. This subunit belongs to the lower part of pollen zone c, dated to ca 3800-3000 yr B.P. Between 30-60cm, the organic content of the gyttja declines and the mineral content increases, suggesting a decrease in water depth. The aquatic assemblage is characterised by an increase in Equisetum and Sphagnum, a decline in Potamogeton and the disappearance of Nymphaea and Nuphar, consistent with decreased depth. A marked decline in Pediastrum indicates shallowing. Microfossils/macrofossils of Desmidiaceae, Rhizopoda, Cladocera and Nymphaeaceae are abundant (Engelmark, per. comm., 1994). Engelmark (personal communication cited in Segerström, 1990) suggested that changes in the micro-faunal record could indicate a shallowing ca 2500-3000 yr B.P. This is consistent with the changes noted in the aquatic pollen assemblage. Although Segerström recognized that the increase in Equisetum and Sphagnum could be a response to lake level lowering, he argues that a more likely explanation is that these changes reflect a climatically-induced expansion of the adjacent mire. However the disappearance of deeper-water aquatics (Nymphaea and Nuphar) and the decline in Potamogeton are less likely to be explained by this mechanism. We interpret the aquatic pollen record as consistent with the microfossil evidence for shallowing. This subunit belongs to the middle part of pollen zone c, characterised by expansion of Picea, and is dated to ca 3000-1700 yr B.P. Between 30-10cm, Desmidiaceae, Rhizopoda and Nymphaeaceae in microfossil/macrofossil assemblages decrease markedly (Engelmark, personal communication, 1994), suggesting increased water depth. The decline of Equisetum from 10% to 5% in aquatic pollen assemblage is consistent with the interpretation. Bosmina increases to ca 50% and Pediastrum also increases slightly (7%, ca 20cm), consistent with increasing water depth. This subunit belongs to the upper part of pollen zone c, ca 1700-560 yr B.P. The uppermost 10cm of lacustrine gyttja is characterised by decrease in Equisetum and Sphagnum (<3%), and the reappearance of Potamogeton and Nuphar, suggesting deep water. Bosmina is abundant (50%) and Nymphaeaceae macrofossils decrease to less than 5%, supporting the interpretation. In the status coding, very low (1) is indicated by algal gyttja with abundant Desmidiaceae; low (2) by gyttja with high values of minerogenic matter, presence of Menyanthes, Equisetum and Sphagnum, and abundant algal microfossils; intermediate (3) by gyttja with increasing Myriophyllum and Sparganium, moderate Bosmina and Pediastrum; high (4) by gyttja with low minerogenic matter, and abundant Bosmina and Pediastrum. References Huntley, B. and Birks, H.J.B., 1983. An Atlas of Past and Present Pollen Maps for Europe: 0-13000 years ago. Cambridge. 667pp. Engelmark, R., 1994. personal communication. Segerström, U., 1990. The long-term vegetational development of the Mid-Luleälv valley, at Vuollerim and Jokkmokk. Archaeology and Environment 7: 58-69. Fromm, E., 1965. Beskrivning till jordartskarta över Norrbottens län nedanför lappmarksgränsen. Sveriges Geologiska Undersoekning Serie (Ca) 39: 236. Ödman, O.H., 1957. Beskriving till Berggrundskarta över urberget i Norrbottens län. Sveriges Geologiska Undersoekning Serie (Ca) 41: 151 Radiocarbon dates St-10816 5160±165 yr B.P. 316-324cm, peat, Kvarnmyran. Pollen zone b, abundant Betula and Alnus. St-10817 2970±215 yr B.P. 227-235cm, peat, Kvarnmyran. Pollen zone a, Picea expansion. Coding ca 8800-7200 yr B.P. very low (1) ca 7200-3800 yr B.P. intermediate (3) ca 3800-3000 yr B.P. high (4) ca 3000-1700 yr B.P. low (2) ca 1700-560 yr B.P. intermediate (3) ca 560-0 yr B.P. high (4) Preliminary coding: 12/11/1993; Final coding: 24/4/1994 Coded by GY and SPH Krageholmssjön, Sweden Krageholmssjön (55 30'N, 13 44'E, 43m above sea level) lies ca 10km north of the southern coast of Sweden. The lake has an area of 220ha and a maximum water depth of ca 9m. There are three inflows from the north- western, south-western and western shores and an outlet from the south-eastern shore via the Svartån to the sea. The catchment area is 1500ha. The basin bedrock is Cretaceous limestone covered by clayey or stony tills and glaciofluvial sediment in a hummocky moraine landscape (Ekström, 1950). The basin was formed by melting of dead ice during the late glacial (Gaillard, 1984a). The stratigraphy of the lake deposits has been reconstructed from 18 cores from the basin (Gaillard, 1984a). Changes in the position of the sediment limit were established from a transect of 8 cores at distances of 2m, 59m, 75m, 90m, 110m, 155m, 178m and 250m from the southwestern shore (Gaillard, 1984a). Core 178m has been used for diatom analysis (Håkansson, 1984, 1989). The basal sediments are sand and gravel, grading to clay and muddy clay. The overlying sediments are detritus gyttja (clayey detritus gyttja, clayey calcareous fine detritus gyttja or calcareous fine detritus gyttja). The overlying sediments are coarse detritus gyttja with silty or sandy layers, grading upwards to calcareous fine detritus gyttja. The sediment sequences are generally similar in each core. Gaillard (1988a, b) has reconstructed lake-level changes during the Holocene on the basis of changes in geomorphology, lithology, sediment limit, diatom and aquatic assemblages following the method describedin Digerfeldt (1986). The record of changes in relative depth presented here follows this reconstruction. There are no radiocarbon dates from Krageholmssjön because of the high carbonate content of the sediments. The chronology is based on pollen correlation with a nearby radiocarbon-dated site, Ageröds mosse (Gaillard, 1984a). A lake-level curve based on the status codings has been presented in Harrison and Digerfeldt (1993). A low water level ca 9500-8900 yr B.P. is indicated by the deposition of fine detritus gyttja in the centre of the lake (core 178m). This unit lenses out towards the shore (Gaillard, 1984a). The presence of abundant Phragmites roots in the central core is consistent with shallow water. The diatom assemblage in core 178m is characterised by abundant Fragilaria and the absence of planktonic species, also consistent with shallow conditions. Gaillard (1984a) suggests the lake was ca 4m lower than present. An increase in the sediment limit to core 90m after ca 8800 yr B.P. indicates an increase in water depth. The subsequent replacement of clayey coarse detritus gyttja by calcareous clayey fine detritus gyttja in cores 90m and 178m, indicates a further increase in the sediment limit and a culmination of deepening ca 7200-5800 yr B.P. A decrease in water level after 5800 yr B.P. is indicated by deposition of silty coarse detritus in core 90m and abundant fruits and seeds of aquatics such as Chara, Potamogeton, and Najas in core 178m. The culmination of the lowering is indicated by sand deposition in core 90m and silty coarse detritus gyttja in core 178m. The lake was about 1m lower than present ca 5400-4300 yr B.P. (Gaillard, 1984a). The presence of silty coarse detritus gyttja in core 90m and silty fine detritus gyttja in core 178m, indicates an increase in water depth after 4300 yr B.P. A sandy layer in core 90m and a silty layer in core 178m indicate a decrease in water level ca 2500-2000 yr B.P. The overlying sediment is fine detritus gyttja in the nearshore cores, suggesting an increase in water depth during the last 2000 years. The diatom assemblage in core 178m is characterised by a maximum abundance of Cyclostephanos and Melosira, consistent with deep water. A discontinuous terrace and ridge of ice-pressed blocks around the lake, ca 1m above the modern water level, indicate a high water level. According to the position of the sediment limit and geomorphological evidence, Gaillard (1984a) suggests the lake was ca 2.5m higher during the interval from 2500-200 yr B.P. A decrease in water level ca 1200-700 yr B.P. is indicated by silty/sandy detritus gyttja deposition in core 90m. This unit has a high minerogenic content and contains abundant seeds and fruits from reed vegetation, consistent with shallow conditions. An increase in water level after ca 700 yr is indicated by a sediment limit above core 90m. The area of the modern lake is less than that shown on the map made in 1707 AD., probably reflecting the deepening of the outlet and the creation of a moat around the adjacent castle at Krageholmssjön (Gaillard, 1984a). In the status coding, low (1) is indicated by a sediment limit below core 178m; intermediate (2) by a sediment limit below core 90m; high (3) by a sediment limit above 90m and fine detritus gyttja with abundant planktonic diatoms in the central core, or by a terrace above modern lake level. The modern lake level has been lowered artificially and is coded accordingly. References Digerfeldt, G., 1986. Studies on past lake-level fluctuations. In Berglund, B. (ed.), Handbook of Holocene Palaeoecology and Palaeohydrology: 127-144. John Wiley & Sons, New York. Ekström, G., 1950. Skånes åkerjordsområden. Socker 6: 53. Malmö (English summary). Gaillard, M-J., 1984a. A palaeohydrological study of Krageholmssjön (Scania, South Sweden), Regional vegetation history and water-level changes. Lundqua Report 25: 1-36. Gaillard, M-J., 1984b. Water-level changes, climate and human impact: A palaeohydrological study of Krageholmssjön (Scania, South Sweden). In: Mörner, N.-A. and Karlen, W. (eds.), Climatic Changes on a Yearly to Millennial Basis, D. Reidel Piblishing Company. pp 147-154. Gaillard, M.J. 1985. Postglacial palaeoclimatic changes in Scandinavia and central Europe. A tentative correlation based on studies of lake level fluctuations. Ecologia Mediteranea Tome XI (Fascicule 1): 159-175. Harrison, S.P. and Digerfeldt, G., 1993. European lakes as palaeohydrological and palaeoclimatic indicators. Quaternary Science Reviews 12: 233-248. Håkansson, H., 1984. Diatom analysis of profile from the southwestern bay of Krageholmssjön (Scania, South Sweden). Lundqua Report 25: 37-40. Håkansson, H., 1989. Diatom succession during Middle and Late Holocene time in Lake Krageholmssjön, southern Sweden. Nova Hedwigia 48: 143-166. Coding ca 10000-9800 yr B.P. high (3) ca 9800-9500 yr B.P. intermediate (2) ca 9500-8900 yr B.P. low (1) ca 8900-7200 yr B.P. intermediate (2) ca 7200-5800 yr B.P. high (3) ca 5800-5400 yr B.P. intermediate (2) ca 5400-4300 yr B.P. low (1) ca 4300-2500 yr B.P. intermediate (2) ca 2500-2000 yr B.P. low (1) ca 2000-1800 yr B.P. intermediate (2) ca 1800-1400 yr B.P. high (3) ca 1200-700 yr B.P. intermediate (2) ca 700-0 yr B.P. high (3) Final coding: June 1989. Coded by : GD, SPH and GY Kroktjärnen, Sweden Kroktjärnen (66 14'N, 20 51'E, 58m above sea level) is a small lake in the Luleälv River valley in northern Sweden. It has an area of 5ha and a maximum water depth of 10.1m. The catchment area is about 100ha. The lake is connected to a fen associated with a small tributary of the Luleälv River. Kroktjärnen is a seepage lake. Geologically the basin is mainly characterised by granites (Ödman, 1957) and surface deposits are fluvioglacial moraines and sand (Fromm, 1965). The lake was formed as a riverside lagoon approximately 5000 years ago (Renberg and Segerström, 1981); it was isolated from the river ca 3000 yr B.P. when the river cut down below the lake threshold (Segerström, 1990). A 1.20m-long core from the lake provides a lacustrine sedimentary record back to before 3000 yr B.P. (Segerström, 1990). Changes in lake depth since the lake became isolated are reconstructed from changes in laminae thickness, sedimentation rates and minerogenic matter contents. The chronology is based on annual varve stratigraphy and comparison of the terrestrial pollen record with that from a nearby radiocarbon-dated site (Segerström, 1990). The uppermost 70cm is considered to be annually- laminated; counting yielded a date of 3023±170 years (Segerström, 1990). Irregular disturbance of the sediment has partially destroyed the laminated structure, make counting problematic but the terrestrial pollen record from this site is very similar to that from a nearby site (Strömbackatjärnen), especially above 2000 yr B.P., suggesting the sedimentation is regular and supporting the annual dating. Before 2000 yr B.P., the pollen records from the two sites differ because of local factors (river influence). We assume that the laminations in the core (0-70cm) are annual and have dated the section accordingly. The basal sediment (120-70cm) is silt and clay with irregular laminations. Segerström (1990) considers it was probably formed in a riverside lagoon when the lake received regular inputs of allochthonous matter due to overbank flooding. This unit is dated to ca 5000-3000 yr B.P. estimated from the regional shoreline displacement curve (Renberg & Segerström, 1981) for the bottom boundary and on varve-counting for the top boundary (Segerström, 1990). The overlying sediment (70-0cm) is laminated lake gyttja. Between 70-45cm, the laminae are very thin (0.1-0.3 mm/laminae), suggesting deep water conditions. The sedimentation rate is quite low (0.019 cm/yr) and the minerogenic matter content is low, consistent with deep water conditions. Between 45-35cm, the laminations are thicker (maximum thickness 0.6 mm, 38-40cm), suggesting shallowing. An increase in sedimentation rate from 0.019 cm/yr to 0.026 cm/yr is consistent with this interpretation. This unit has a relatively high value of minerogenic matter, consistent with a decrease in water depth. The unit is dated to ca 1950-1350 yr B.P. In the overlying unit (35-25cm), the laminae are thinner (0.1-0.2 mm/laminae), suggesting an increase in water depth. A marked decrease in mineral matter is consistent with deeper water. This unit is dated in ca 1350-800 yr B.P. Between 25-23cm, there is an increase in varve thickness (0.4 mm/laminae) and very high peak of minerogenic matter, reflecting a period of shallow water ca 800-650 yr B.P. The presence of Alisma in the aquatic pollen assemblage is consistent with this interpretation. The overlying laminated gyttja (23-12cm) has thin varves (0.15-0.25 mm/laminae) and a low mineral content, suggesting increased water depth. The unit is dated to 650-190 yr B.P. The uppermost gyttja (above 12cm) has indistinct laminations. Varve thickness increases to a maximum of 5mm, and then disappears, suggesting shallowing. The aquatic assemblage is characterised by the presence of Alisma and Typha, and an increase in Sphagnum, consistent with shallowing. These changes are thought to reflect increasing human activities in the basin (Segerström, 1990). The lake still has a water depth of over 10m in the centre. In the status coding, low (1) is indicated by lake gyttja, with thick laminations, high minerogenic matter and high sedimentation rate; high (2) by lake gyttja with thin laminations, low minerogenic matter and low sedimentation rate. The coding starts after the lake was isolated from riverine influence ca 3000 yr B.P. Varve dates 6-7cm ca 1930 AD (ca 20 yr B.P.) 10cm ca 1870 AD (ca 80 yr B.P.) 15cm ca 1700 AD (ca 250 yr B.P.) 17cm ca 1600 AD (ca 350 yr B.P.) 24-23cm ca 1300 AD (ca 650 yr B.P.) 30-31cm ca 800 AD (ca 1150 yr B.P.) 35cm ca 600 AD (ca 1350 yr B.P.) 45cm ca 0 AD (ca 1950 yr B.P.) 50cm 1960±72 years B.P. (ca 1960 yr B.P.) 66-64cm ca 70 BC (ca 2020 yr B.P.) 70cm 3023±170 years B.P. (ca 3000 yr B.P.) References Fromm, E., 1965. Beskrivning till jordartskarta över Norrbottens län nedanför lappmarksgränsen. Sveriges Geologiska Undersoekning (Serie Ca) 39: 236. Renberg, I. and Segerström, U., 1981. The initial points on a shoreline displacement curve for southern Västerbotten, dated by varve-counts of lake sediments. Striae 14: 174-176. Segerström, U., 1990. The history of agriculture and vegetation at Edefors as reflected in two varved lake sediments. In Segerström, U. (ed), The Post-glacial history of vegetation and agriculture in the Luleälv river valley. Archaeology and Environment 7: 39-57. Ödman, O.H., 1957. Beskriving till Berggrundskarta över urberget i Norrbottens län. Sveriges Geologiska Undersoekning (Serie Ca) 41: 151. Coding ca 3000-1950 yr B.P. high (2) ca 1950-1350 yr B.P. low (1) ca 1350-800 yr B.P. high (2) ca 800-650 yr B.P. low (1) ca 650-0 yr B.P. high (2) Preliminary coding: 6/12/1993; Final coding: 25/2/1994. Coded by GY and SHP Lilla Gloppsjön, Sweden Lilla Gloppsjön (59 48'10"N, 14 37'40"E, 198m above sea level) is a deep lake in Sikfors, south-central Sweden. It has a maximum water depth of ca 27m and an area of ca 50ha. The catchment covers ca 650ha. Most of the lakeshore is rocky with boulders. Two small streams enter the lake from the southern end. There is a man-made outlet at the northern, ca 150m east of the natural outlet which has been dammed (Almquist- Jacobson, 1994). The basin is located in a bedrock depression. The bedrock in the region includes granite, gneiss and leptite. The region was deglaciated between 9700 and 9600 yr B.P. (Björck and Digerfeldt, 1986). Seven cores (A, B, C, D, E, F, G) along a N-S transect at the northern end of the lake provide a sedimentary record back to ca 9600 yr B.P. (Almquist-Jacobson, 1994). The cores were taken from water depths of 25.80m (core A), 9.25m (core B), 4.75m (core C), 3.15m (core D), 2.55 (core E), 2.07m (core F) and 1.38m (core G). Almquist-Jacobson (1994) reconstructed changes in the water level of Lilla Gloppsjön on the basis of historical record, geomorphologic evidence, and changes in the position of the sediment limit, sediment lithology and sedimentation rate following the method described by Digerfeldt (1986). For this purpose, the individual cores were correlated on the basis of the terrestrial pollen assemblages. The chronology of lake-level changes is based on eleven radiocarbon dates from core A, which span the Holocene. Almquist-Jacobson (1994) states that changes in sediment composition are subtle because there are no significant sources of sand and the lake is very deep (maximum 27m), even during the lowest lake stand. However, the sediment limit has clearly varied through time. The description, coding and lake-level curve given here follow Almquist-Jacobson (1994). Digerfeldt (personal comm., 1994) has proposed an alternative interpretation of the changes in high sedimentation rate ca 8200, 4400 and 2600 yr B.P. He suggests that the high sedimentation rate in the shallow water cores is consistent with the presence and increase in the coarse minerogenic matter, which the occurrence of some hiatuses indicates temporary sediment erosion. The "normal" interpretation of such a combination of evidence is a lowering of lake level. Digerfeldt (personal comm., 1994) argues the pattern of lake-level change in Lilla Gloppsjön, according to this alternative interpretation, would be about the same as in southern Sweden. However, the pattern of relative lake level changes at Lilla Gloppsjön is very similar to that from the nearby lake of Ljustjärnen (Almquist-Jacobson, 1994), which is reconstructed independently from lithology, sediment limit and aquatic macrofossil assemblage data but not sedimentation rate. There does not seem to be overwhelming evidence in favour of rejecting the reconstruction proposed by Almquist-Jacobson (1994). The coding proposed here therefore follows that reconstruction. The basal sediment is silt and sand in cores A, B, E and G (below 2900cm, below 1170cm, below 820cm and below 560cm below water surface respectively). A sample from the top of this unit (2900-2950m in core A) is radiocarbon-dated to 9560±100 yr B.P. The sediment deposited after ca 9600 yr B.P. is lacustrine silty gyttja, suggesting moderately deep water. Changes in the sediment limit, sediment lithology and sedimentation rate allow the unit to be subdivided. A possible decrease in water depth ca 9100 yr B.P. is indicated by a lens of sand in the margin of the lake (core F) and medium-size sand and drift litter in cores F, D, C and B. A change to fine-grained sediment at the lake margins (cores G, F, D, C, B), suggests increased water depth after ca 8600 yr B.P. An increase in sedimentation rate in cores E and F is interpreted as a result of increasing water depth. A marked decrease in water depth after ca 7400 yr B.P. is indicated by the missing pollen zone LG3a from cores C and G. An increase in the inorganic content of cores D and E, and extraordinarily high sedimentation rates in cores D, E and F, also suggest shallow water. A return to high sedimentation rates in margin of the lake and a decrease in the inorganic content of cores D and E, suggest increased water depth after ca 5300 yr B.P. An increase in coarse organic and sand content of cores D, E and F suggests decreased water depth after ca 4100 yr B.P. The missing pollen zone LG4b (4400-3800 yr B.P.) from core G also indicates a low sediment limit and shallowing. A return to continuous sedimentation at pollen zone (core G), and a decrease in the coarse organic and sand content of cores D, E and F suggests increased water depth after ca 3800 yr B.P. A decrease in water depth after ca 2400 yr B.P. is indicated by a missing pollen zone LG4d (2600-2200 yr B.P.) from core G, increases in coarse organic and sand content in cores E and F, and abundant inorganic matter in core D. Many in situ Pinus stumps were found in the southwestern bay. One was dated to ca 500 yr B.P., implying a lake level ca 1m lower than today. A low sedimentation rate at the lake margin (cores C and D) is consistent with a shallowed lake margin condition. The southwestern bay was inundated after ca 500 yr B.P. (a correction of 340 yr B.P. was subtracted from the following reported ages). Decreases in the coarse organic and sand content of cores E and F, and a decrease in the inorganic content of core D are consistent with a rise in water level. An increase in sedimentation rate in near lake margin (cores C, D and G) is consistent with deeper conditions. In the status coding, low (1) is indicated by a sediment limit below core C, and increase in inorganic content in cores D and E; moderately low (2) by a sediment limit below core G, and increases in coarse organic and sand content of cores D, E and F; intermediate (3) by a sediment limit below core G, sand in core F, and medium-size sand and drift litter in cores F, D, C; moderately high (4) by a high sediment limit and fine-grained sediments in the marginal lake; high (5) by the highest sediment limit and the inundation of the southwest bay. Radiocarbon dates Lu-3027 1840±60 yr B.P. 26.13-26.17m below water surface, silty gyttja, core A Lu-2965 2230±60 yr B.P. 26.30-26.34m below water surface, silty gyttja, core A Lu-2964 2690±60 yr B.P. 26.60-26.63m below water surface, silty gyttja, core A Lu-2963 3180±60 yr B.P. 26.90-26.93m below water surface, silty gyttja, core A Lu-2962 3880±70 yr B.P. 27.20-27.23m below water surface, silty gyttja, core A Lu-2961 4240±70 yr B.P. 27.46-27.49m below water surface, silty gyttja, core A Lu-2960 5060±70 yr B.P. 27.80-27.83m below water surface, silty gyttja, core A Lu-2959 5910±70 yr B.P. 28.10-28.13m below water surface, silty gyttja, core A Lu-2958 7150±80 yr B.P. 28.40-28.43m below water surface, silty gyttja, core A Lu-2957 8490±100 yr B.P. 28.70-28.73m below water surface, silty gyttja, core A Lu-2955 9560±100 yr B.P. 29.00-29.05m below water surface, organic silt, core A References Almquist-Jacobson, H., 1994. Interaction of Holocene climate, water balance, vegetation, fire, and cultural land- use in the Swedish Borderland. Lundqua Thesis 30: 82 pp. Björck, S. and Digerfeldt, G., 1986. Late Weichselian-Early Holocene shore displacement west of Mt. Billingen, within the Middle Swedish end-moraine zone. Boreas 15: 1-18. Digerfeldt, G., 1986. Studies on past lake-level fluctuations. In Berglund, B. (ed.), Handbook of Holocene Palaeoecology and Palaeohydrology: 127-144. John Wiley & Sons, New York. Digerfeldt, G., 1994. personal communication. Coding ca 9600-8900 yr B.P. moderately high (4) ca 8900-8600 yr B.P. intermediate (3) ca 8600-7400 yr B.P. moderately high (4) ca 7400-5300 yr B.P. low (1) ca 5300-4100 yr B.P. intermediate (3) ca 4100-3500 yr B.P. moderately low (2) ca 3500-2400 yr B.P. moderately high (4) ca 2400-500 yr B.P. intermediate (3) ca 500-0 yr B.P. high (5) Preliminary coding: 27/5/1994; Final coding: 7/7/1994 Coded by GY, SPH and HA-J Ljustjärnen, Sweden Ljustjärnen (59 45'40"N, 14 29'25"E, 183 above sea level) is a small lake in Hällefors, south-central Sweden (Almquist-Jacobson, 1994). It has a maximum water depth of ca 10.3m and an area of ca 10ha. The catchment covers ca 50ha. Two small man-made channels enter the lake from the west and the east respectively. There is a man-made outlet, constructed in the last century, from the southern end (Almquist-Jacobson, 1994). The basin is a ice-block depression located in a glaciofluvial sandplain. The region was deglaciated between 9700 and 9600 yr B.P. (Björck and Digerfeldt, 1986). Six cores (A', A, B, C, D, E) along an E-W transect across the lake provide a sedimentary record back to ca 9200 yr B.P. (Almquist-Jacobson, 1994). The cores were taken from water depths of 10.30m (core A'), 8.10m (core B), 6.55m (core C), 4.75m (core D), 3.70m (core D) and 2.15m (core E). There are three additional cores: cores O and R were taken from the peaty southwestern edge and core S from a water depth of 6.17m in the southern part of the lake. Almquist-Jacobson (1994) reconstructed changes in the water level of Ljustjärnen on the basis of geomorphologic evidence and changes in the position of the sediment limit, sediment lithology and aquatic macrofossil assemblages following the method described by Digerfeldt (1986). For this purpose, the individual cores were correlated on the basis of the terrestrial pollen assemblages. The chronology of lake-level changes is based on six radiocarbon dates, 5 from core A and one from core A', which span the Holocene. The description, coding and lake-level curve given here follow Almquist-Jacobson (1994). Digerfeldt (personal comm., 1994) has proposed that the lake-level changes in Ljustjärnen in the early Holocene is not suitable for paleoclimatic reconstruction. He argued that the lake is located in a glaciofluvial sandplain so that the water balance must be dominated by groundwater, and the lake level can be assumed to be related to the regional groundwork table. After deglaciation in the early Holocene the irregular isostatic uplift (northwards increasing uplift) probably resulted in a progressive tilting of the regional groundwork table, which also affected lake level in Ljustjärnen. This means that the record lake level changes in the early Holocene - perhaps until about 6000 yr B.P. - are "untypical" and cannot be uses for paleoclimatic reconstruction (Digerfeldt, personal comm., 1994). The rapid lowering of the Ancylus Lake between 9200-9000 yr B.P. may also have affected the lake level in Ljustjärnen - viz. through a lowering of the hydrologic threshold (Digerfeldt, personal comm., 1994). However, the pattern of water-level changes during the early Holocene does not appear to reflect a simple, albeit irregular, lowering of base-level. Thus, although changes in the regional ground-water may have influenced the lake they are insufficient to completely explain the observed record. The coding proposed here therefore follows that proposed by Almquist-Jacobson (1994). The basal sediment is silt and sand in cores A' and A (below 1213cm and below 1056cm below water surface), deposited before ca 9200 yr B.P. The overlying sediment is silty gyttja in both the centre of the lake (1056-1010cm below water surface in core A and 1213-1120cm below water surface in core A') and the margin of the lake (core R, 254-270cm). The occurrence of lacustrine deposits over the entire lake indicates the lake level was high. A wave-cut scarp ca 0.5m above the modern lake surface occurring along the northern and eastern lake shore, probably corresponds to this high lake level (Almquist-Jacobson, 1994). There is a layer of fine silt in the margin of the lake (ca 820cm in core S), with continued silty gyttja in the centre, suggesting slightly decreased water depth ca 8800-8200 yr B.P. Discontinuous sediments in cores R and O are consistent with shallowing. Macrofossils of Potamogeton friesii and P. berchtoldii occur in core R, suggesting that the lake level did not fall more than ca 2m below the modern level (Almquist-Jacobson, 1994). An extension of silty gyttja deposition into the marginal areas of the lake (475-478cm below water surface in core B), indicates an increase in water depth ca 8200-7800 yr B.P. The aquatic macrofossils assemblage in cores R and O is characterised by Potamogeton friesii, P. natans and P. berchtoldii, which constrain water level to ca 1m below modern lake level (Almquist-Jacobson, 1994). The overlying sediments are sand and silt in cores O and R, with continued silty gyttja deposition in the lake centre. This unit extends from the lake margin to core C, indicating a lowered sediment limit below core C, and hence moderately shallow water after ca 7800 yr B.P. Fen peat began to form at the margin after ca 6500 yr B.P. (above 307cm in core O and above 254cm in core R). The aquatic macrofossils assemblage is characterised by Isoetes setacea in core B, which grows in water depths of less than 2m, and constrains the lowest lake-level to ca 5m below the modern water level, which culminated between 6500-6100 yr B.P. (Almquist-Jacobson, 1994). The overlying sediment is gyttja with bryophyte remains (above 1120cm below water surface in core A', above 1010cm below water surface in core A, 746-715cm below water surface in core B, 540-536cm below water surface in core C), suggesting an increase in water depth. Isoetes setacea is absent in core B but occurs at the lake margin (core D), consistent with rising water level. The fen peat at coring site R was not inundated, suggesting that the lake level probably did not rise to more than ca 2.5m below the modern water level (Almquist-Jacobson, 1994). A change to sand with coarse organic material in cores D (475-474cm below water surface) and C (534-536cm below water surface), and an influx of magnetic materials at cores B and D after ca 4100 yr B.P., with continued gyttja in the centre, suggests a lowering of sediment limit and moderately low lake level. A return to gyttja with moss in core C (534-480cm below water surface), suggests a higher sediment limit and a rise in water level after ca 3900 yr B.P. Isoetes setacea decreases in core B but became established in the lake margin (core E), consistent with increased depth. The fen peat at core R was not inundated, suggesting that the water level rose to a maximum of ca 2m below the modern water level (Almquist-Jacobson, 1994). A lower sediment limit and decrease in water depth between ca 2200-1900 yr B.P. is indicated by magnetic materials in cores B, C and E, and by coarse inorganic matter in cores D and E. The sediment deposited in core C after 1900 yr B.P. is reworked and sedimentation ceased at core E, consistent with shallowing. Almquist- Jacobson (1994) suggests that the water level fell to ca 2.75m below the modern water level. The uppermost sediments are gyttja in cores A and E (above 865cm and above 290cm below water surface respectively), and gyttja with moss in core B (above 713cm below water surface), suggesting increased water depth after ca 500 yr B.P. At the lake margins, gyttja overlies peat in core O, consistent with lake expansion and rising water level in last 300 yr B.P. In the status coding, (1) low (ca 5m lower than the modern water level) is indicated by Isoetes at ca 8m below present and sediment limit below 5.5m; (2) moderately low (ca 2.5-3m lower than the modern water level) by sand near the lake margin; (3) intermediate (ca 2m lower than the modern water level) by gyttja in the centre and fen peat at the margin, or discontinuous sediments in the margin and silt in near margin with continued silty gyttja in the centre; (4) moderately high (ca 1m lower than the modern water level) by gyttja or silty gyttja extended to near lake margins, with increased Potamogeton and absent Isoetes; (5) high (ca 0-0.5m higher than the modern water level) by high shoreline (a wave-cut scarp lying 0.5m above the modern lake surface); or by gyttja over the fen peat at the margin of the lake. Radiocarbon dates Lu-3244 1630±60 yr B.P. 850-857cm below water surface, gyttja core A Lu-3243 3400±70 yr B.P. 887-892cm below water surface, gyttja with moss core A Lu-3242 4050±70 yr B.P. 922-927cm below water surface, gyttja with moss core A Lu-3241 4970±80 yr B.P. 952-957cm below water surface, gyttja with moss core A Lu-3240 6650±90 yr B.P. 982-987cm below water surface, silty gyttja core A Lu-3352 9120±110 yr B.P. 1031-1037cm below water surface, silty gyttja core A' References Almquist-Jacobson, H., 1994. Interaction of Holocene climate, water balance, vegetation, fire, and cultural land- use in the Swedish Borderland. Lundqua Thesis 30: 82 pp. Björck, S. and Digerfeldt, G., 1986. Late Weichselian-Early Holocene shore displacement west of Mt. Billingen, within the Middle Swedish end-moraine zone. Boreas 15: 1-18. Digerfeldt, G., 1986. Studies on past lake-level fluctuations. In Berglund, B. (ed.), Handbook of Holocene Palaeoecology and Palaeohydrology: 127-144. John Wiley & Sons, New York. Digerfeldt, G., 1994. Personal communicatin. Coding ca 9200-8800 yr B.P. high (5) ca 8800-8200 yr B.P. intermediate (3) ca 8200-7800 yr B.P. moderately high (4) ca 7800-6600 yr B.P. moderately low (2) ca 6600-6100 yr B.P. low (1) ca 6100-5400 yr B.P. moderately low (2) ca 5400-4100 yr B.P. intermediate (3) ca 4100-3900 yr B.P. moderately low (2) ca 3900-2200 yr B.P. intermediate (3) ca 2200-1900 yr B.P. moderately low (2) ca 1900-300 yr B.P. moderately high (4) ca 300-0 yr B.P. high (5) Preliminary coding: 19/4/1994; Final coding: 6/7/1994. Coded by GY, SPH and HA-J Lyngsjö, Sweden Lake Lyngsjö (56 59'N, 12 33'E, ca 55m above sea level) is a small lake in central Halland, Sweden. The lake has an area of about 35ha and a maximum depth of 3.2m. There is an outlet from the south of the lake to the river Törlan. The catchment area is ca 180ha. The catchment bedrock is Precambrian gneiss. The stratigraphy of the lake deposits has been reconstructed from a transect of six cores taken at distances between 28m and 118m from the shore (cores 28m, 38m, 43m, 53m, 95m and 118m) (Digerfeldt, 1976). The basal sediment is sand and silty clay gyttja. The overlying sediments are clayey algal gyttja in the centre (core 118m) and silty sand near the margin (core 38m). After that a layer of Phragmites peat occurs. This is overlain by algal gyttja in cores 95m and 118m. The uppermost sediments are detritus gyttja, but most of this unit has been disturbed (Digerfeldt, 1976). The sediment sequences are generally similar in each core. Digerfeldt (1976) has reconstructed lake-level changes during the early Holocene on the basis of changes in lithology, sediment limit and aquatic assemblages following the method described in Digerfeldt (1986). The record of changes in relative depth presented here follows this reconstruction. The chronology is based on pollen correlation with a nearby radiocarbon-dated site, Ageröds mosse (Digerfeldt, 1976). A lake-level curve based on the status codings has been presented in Harrison and Digerfeldt (1993). A higher water level during the early pre-Boreal (ca 10400-9500 yr B.P.) is indicated by a high sediment limit up to core 38m (5.09-5.18m). The aquatic assemblage in cores 38m and 95m contains abundant Myriophyllum and Nymphaea, consistent with deep water. The overlying sediment consists of silty clayey gyttja in core 95m (6.05-6.11m) and silty sand in core 38m (5.05-5.09m), but clayey algal gyttja in core 118m (6.15-6.25m). This indicates a decrease in sediment limit below core 95m and shallow conditions ca 9500-9300 yr B.P. A continuous decrease in water level during the late pre-Boreal (ca 9300-8400 yr B.P) is indicated by a low sediment limit and deposition of Phragmites peat from the margin to the centre of the lake (4.57-5.05m in core 38m, 5.80-6.05m in core 95m and 5.98-6.15m in core 118m). Digerfeldt (1988) suggests that the lake was 4-5m lower than present at the culmination of the lowering ca 9000 yr B.P. An increase in water level during the early Boreal is indicated by an increased sediment limit to core 95m. Algal gyttja is found in core 95m (3.45-3.60m) and core 118m (3.45-3.3.58m). A continuous increase in water level after ca 7900 yr B.P. is indicated by a sediment limit up to core 38m (above 3.47m), and replacement of detritus gyttja by algal gyttja in cores 95m (above 3.45m) and 118m (above 3.45m)(Digerfeldt, 1988). The record of lake-level changes after 7500 yr B.P. has not been reconstructed because the sediments have been considerably disturbed (Digerfeldt, 1976). In the status coding, low (1) is indicated by a sediment limit below core 118m and Phragmites peat in the centre of the lake; intermediate (2) by a sediment limit below core 95m; high (3) by a sediment limit above core 38m. References Digerfeldt, G., 1976. A Pre-Boreal water-level change in Lake Lyngsjö, central Halland. Geologiska Föreningens i Stockholm Förhandlingar 98: 329-336. Digerfeldt, G., 1986. Studies on past lake-level fluctuations. In Berglund, B. (ed.), Handbook of Holocene Palaeoecology and Palaeohydrology: 127-144. John Wiley & Sons, New York. Harrison, S.P. and Digerfeldt, G., 1993. European lakes as palaeohydrological and palaeoclimatic indicators. Quaternary Science Reviews 12: 233-248. Coding ca 10000-9500 yr B.P. high (3) ca 9500-9300 yr B.P. intermediate (2) ca 9300-8400 yr B.P. low (1) ca 8400-7900 yr B.P. intermediate (2) ca 7900-7500 yr B.P. high (3) ca 7500-0 yr B.P. not coded Final coding: June 1989. Coded by GD, SPH and GY Ranviken (Lake Immeln), Sweden Lake Immeln (56 16'N, 14 18'E, 81m above sea level) is a large lake (ca 28000ha) in the southern Swedish Uplands. Ranviken is the western bay of the lake and is linked to the main basin by a narrow channel (ca 20m wide). Ranviken has an area of ca 8.3ha and a maximum water depth of 1.7m. A small stream enters the bay in the west. The water is poor in electrolytes (µ S20 ca 80) and has a slightly acid reaction (pH 5.8-6.7). The basin was deglaciated towards the end of the Oldest Dryas (ca 12400-12000 yr B.P.) (Digerfeldt, 1974). The bedrock is Archaean gneiss, covered by a sand and gravel till. The stratigraphy of the lake deposits has been reconstructed from five cores from the bay (Digerfeldt, 1974, 1975). A 8.7m-long Livingstone core (main core) taken in a water depth of 1.6m in the centre of the lake, a complementary core taken from the shallow water in the southwestern part of the lake, and a transect of 3 cores taken at distances at 10m, 25m and 55m from the northwestern shore (cores MBP1, MBP2 and MBP3) provide a sedimentary record through the Holocene. The basal sediments are clayey silt and silty clay. The overlying sediments are clay gyttja. The uppermost sediments are detritus gyttja. The sediment sequences are generally similar in each core. Digerfeldt (1974) has reconstructed lake-level changes during the Holocene on the basis of changes in lithology, sediment limit, diatom and aquatic assemblages following the method described in Digerfeldt (1986). The record of changes in relative depth presented here follows this reconstruction (Digerfeldt, 1974). The chronology is based on 20 radiocarbon dates from the main core and 5 from complementary core (Håkansson, 1969 and 1972). A lake-level curve based on the status codings has been presented in Harrison and Digerfeldt (1993). A lowered water level during the Pre-Boreal and early Boreal is indicated by a sediment limit below core MBP3 and coarse minerogenic matter in the central core. Digerfeldt (1974) suggests the lake was ca 2.5m lower than present at the culmination of this lowering, ca 9400-8700 yr B.P. An increase in water level during the late Boreal and Atlantic (ca 7600-5700 yr B.P.) is indicated by a sediment limit at core MBP1 and a decrease in the coarse mineral content of cores MBP2 and MBP3. A decrease in water level during the sub-Boreal is indicated by a sediment limit below core MBP3 and an increase in the coarse matter content of the central core. The abundance of Potamogeton, Typha and Rhamnus frangula fruits in the nearshore cores is consistent with shallow water. The lake was 2.0m lower than the present (Digerfeldt, 1974) ca 4400-2200 yr B.P. A higher water level during the sub-Atlantic is indicated by an increase in the sediment limit to core MBP1 and a decrease in the coarse matter content of the central cores. A minimum in the coarse matter content, and the abundance of Potamogeton and Equisetum, in cores MBP1 and MBP 3 marks the culmination of deep water conditions after ca 1100 yr B.P. The uppermost sediment in cores MBP1 and MBP3 is characterised by an increase in coarse matter. This is probably due to infilling of Ranviken Bay (Digerfeldt, 1974) and is coded accordingly. In the status coding: low (1) is indicated by a sediment limit in core MBP3 and an increase in coarse minerogenic content in the central cores; intermediate (2) by an increase in sediment limit close to core MBP1; high (3) by a sediment limit above core MBP1 and clay gyttja or detritus gyttja deposition in all the cores. Radiocarbon dates Lu-133 750±100 112.5-117.5cm detritus gyttja, complementary core Lu-132 910±100 137.5-142.5cm detritus gyttja, complementary core Lu-198 1260±100 185.0-190.0cm detritus gyttja, main core Lu-131 1500±100 160.0-165.0cm detritus gyttja, complementary core Lu-197 1880±100 200.0-205.0cm detritus gyttja, main core Lu-130 1920±100 182.5-187.5cm detritus gyttja, complementary core Lu-129 2300±100 192.5-197.5cm detritus gyttja, complementary core Lu-215 2310±100 227.0-232.5cm detritus gyttja, main core Lu-128 2950±100 312.5-317.5cm detritus gyttja, main core Lu-127 3450±100 345.0-350.0cm detritus gyttja, main core Lu-196 4130±100 227.0-232.5cm detritus gyttja, main core Lu-195 4900±100 470.0-475.0cm detritus gyttja, main core Lu-126 5420±100 517.5-522.5cm detritus gyttja, main core Lu-125 5840±100 537.5-542.5cm detritus gyttja, main core Lu-194 6140±100 595.0-600.0cm detritus gyttja, main core Lu-595 6820±60 637.5-642.5cm detritus gyttja, main core Lu-124 6980±100 652.5-657.5cm detritus gyttja, main core Lu-193 7390±100 690.0-695.0cm detritus gyttja, main core Lu-120 7790±100 722.5-727.5cm detritus gyttja, main core Lu-119 8010±100 730.0-735.0cm detritus gyttja, main core Lu-118 8570±100 760.0-765.0cm detritus gyttja, main core Lu-117 8750±100 765.0-770.0cm detritus gyttja, main core Lu-123 9310±100 792.5-797.5cm detritus gyttja, main core Lu-122 9450±100 797.5-802.5cm detritus gyttja, main core Lu-121 9850±100 815.0-820.5cm detritus gyttja, main core References Digerfeldt, G. 1974. The Post-glacial development of the Ranviken bay in Lake Immeln. I. The history of the regional vegetation, and II. The water-level changes. Geologiska Föreningens i Stockholm Förhandlingar 96: 3-32. Digerfeldt, G. 1975. The Post-glacial development of the Ranviken bay in Lake Immeln. III. Palaeolimnology. Geologiska Föreningens i Stockholm Förhandlingar 97: 13-28. Digerfeldt, G., 1986. Studies on past lake-level fluctuations. In Berglund, B. (ed.), Handbook of Holocene Palaeoecology and Palaeohydrology: 127-144. John Wiley & Sons, New York. Harrison, S.P. and Digerfeldt, G., 1993. European lakes as palaeohydrological and palaeoclimatic indicators. Quaternary Science Reviews 12: 233-248. Håkansson, S., 1969. University of Lund radiocarbon dates II. Radiocarbon 11: 430-450. Håkansson, S., 1972. University of Lund radiocarbon dates V. Radiocarbon 14: 340-357. Coding 10000-9700 yr B.P. high (3) 9700-9400 yr B.P. intermediate (2) 9400-8400 yr B.P. low (1) 8400-7600 yr B.P. intermediate (2) 7600-5700 yr B.P. high (3) 5700-4400 yr B.P. intermediate (2) 4400-2200 yr B.P. low (1) 2200-1100 yr B.P. intermediate (2) 1100-0 yr B.P. high (3) Final coding: June 1989 Coded by GD, SPH and G Sandsjön, Sweden Sandsjön (56 45'N, 13 25'E, 157.8m above sea level) is a small lake in southwestern Småland, about 30km from the west coast of Sweden. The lake has an area of 65ha and a maximum depth of 2.2m. There are three inlets through canalized brooks, and an outflow from the northern part of the lake to the river Lagan. The lake is oligotrophic with a low productivity and a mean pH of 5.4 (Thelaus, 1988). The basin was deglaciated during the Bölling between 12,700 and 12,400 yr B.P. (Mangerud et al., 1974). The southern bay of the lake, where the cores were taken, is probably a kettle hole. The catchment area is 600ha. The catchment bedrock is Precambrian veined gneiss (Kornfält et al., 1986). A transect of three cores (cores A, B and C) taken at distances of 25m, 47m and 72m from the shore in the southern bay, and a main core (core MP) taken from the centre of the bay, provide a sedimentary record back to ca 12,000 yr B.P. (Thelaus, 1988). The basal sediments are silts, grading upwards from sandy silt to sandy gyttja silt and clay gyttja silt. Holocene lacustrine sedimentation began with algal silty gyttja, grading upwards to silty fine detritus gyttja. Note that the core depths used here are depths below the water surface (Thelaus, 1988). Thelaus (1988) has reconstructed lake-level changes during the Holocene on the basis of changes in lithology, sediment limit and aquatic assemblages following the method described in Digerfeldt (1986). The record of changes in relative depth presented here follows this reconstruction. The chronology is based on 15 radiocarbon dates from core MP (Thelaus, 1988; Håkansson, 1988). A lowered water level ca 10000-9300 yr B.P is indicated by a low sediment limit, an hiatus in sedimentation in core A and the presence of coarse algal gyttja in cores MP and C (Thelaus, 1988). An increase in water level after 9300 yr B.P. is indicated by an increase in sediment limit to core B. Sediment in cores C and B have a low content of coarse matter, consistent with deep water. A continuous increase in water level after ca 7600 yr B.P. is indicated by a sediment limit up to core A. A decrease in coarse mineral content and the absence of Nymphaea seeds in the centre of the lake (core C) is consistent with deep water. A decrease in the sediment limit to core B and the presence of coarse minerogenic matter in cores MP and C suggest a decrease in water depth ca 4700-2700 yr B.P. Abundant tree rootlets and Nymphaea seeds in cores C and MP are consistent with shallowing. There is a sedimentary hiatus in core A (ca 2.8m) around 3900 yr B.P., suggesting very shallow or even dry conditions at this time (Thelaus, 1988). An increase in water level after 2700 yr B.P. is indicated by an increase in the sediment limit to core A and a decrease in coarse minerogenic matter in cores MP and C. A decrease in the sediment limit to core B and an increase in coarse minerogenic matter in cores C and MP, suggest decreased water depth ca 2100-1600 yr B.P. The macrofossil assemblage in core MP is characterised by an increase in tree and shrub rootlets and Nymphaea seeds and leaf scars, consistent with shallower water. A high sediment limit to core A after ca 1600 yr B.P. indicates an increase in water level (Thelaus, 1988). Fine detritus gyttja with relatively little coarse matter is present in cores MP, C and B, consistent with deep water. In the status coding, low (1) is indicated by a sediment limit to core C, and high coarse minerogenic content and abundant macrofossils in the central core; intermediate (2) by a sediment limit below core B; high (3) by a sediment limit to core A and low coarse minerogenic content in the central core. References Digerfeldt, G., 1986. Studies on past lake-level fluctuations. In Berglund, B. (ed.), Handbook of Holocene Palaeoecology and Palaeohydrology: 127-144. John Wiley & Sons, New York. Harrison, S.P. and Digerfeldt, G., 1993. European lakes as palaeohydrological and palaeoclimatic indicators. Quaternary Science Reviews 12: 233-248. Håkansson, S. 1988. University of Lund radiocarbon dates XXI. Radiocarbon 30: 179-196. Kornfält, K-A., Wikman, H. and Samuelsson, L., 1986. Berggrundskarta över Kronobergs län. In: Söderholm, H., Fogdestam, B. and Equgqvist, P., Beskrivning till kartan över grundvattnet i Kronobergs län. Sveriges Geologiska Undersökning Ah 10: 88 pp. Mangerud, J., Andersen, S.T., Berglund, B.E. and Donner, J.J., 1974. Quaternary stratigraphy of Norden, a proposal for terminology and classification. Boreas 3: 109-126. Thelaus, M., 1989. Late Quaternary vegetation history and palaeohydrology of the Sandsjön-Arshult area, southwestern Sweden. Lundqua Thesis 26: 77 pp. Radiocarbon dates Lu-2976 2180±50 yr B.P. 2.60-2.65m below water surface, core MP Lu-2760 1900±50 yr B.P. 3.05-3.10m below water surface, core MP Lu-2759 2400±50 yr B.P. 3.80-3.85m below water surface, core MP Lu-2758 2470±50 yr B.P. 4.20-4.25m below water surface, core MP Lu-2757 2640±50 yr B.P. 5.25-5.30m below water surface, core MP Lu-2756 3880±50 yr B.P. 6.25-6.30m below water surface, core MP Lu-2755 4230±60 yr B.P. 7.35-7.40m below water surface, core MP Lu-2754 5570±60 yr B.P. 8.30-8.35m below water surface, core MP Lu-2753 6370±70 yr B.P. 8.90-8.95m below water surface, core MP Lu-2752 7370±60 yr B.P. 9.55-9.60m below water surface, core MP Lu-2751 8000±80 yr B.P. 9.85-9.90m below water surface, core MP Lu-2700 8850±80 yr B.P. 10.15-10.20m below water surface, core MP Lu-2699 9440±80 yr B.P. 10.30-10.35m below water surface, core MP Lu-2698 10140±90 yr B.P. 10.70-10.75m below water surface, core MP Lu-2697 10200±90 yr B.P. 10.85-10.90m below water surface, core MP Coding 10000-9300 yr B.P. low (1) 9300-7600 yr B.P. intermediate (2) 7600-4700 yr B.P. high (3) 4700-3800 yr B.P. low (1) 3800-2700 yr B.P. intermediate (2) 2700-2100 yr B.P. high (3) 2100-1600 yr B.P. intermediate (2) 1600-0 yr B.P. high (3) Final coding: June 1989. Coded by GD, SPH and GY Torreberga, Sweden Torreberga (55.37 N, 13.14 E, 6.8m above sea level) is a former lake in the Torreberga valley, 15km south of Lund in southern Sweden (Berglund and Digerfeldt, 1970). The lake was drained by an affluent of the Segeå river recently (Digerfeldt, 1971). The Torreberga valley consists mainly of glaciofluvial sand and gravel. This region was isolated from the Baltic Ice Lake ca 13,000 yr B.P. (Berglund and Digerfeldt, 1970). The stratigraphy of the lake deposits has been reconstructed from a transect of ten cores taken across the ancient lake basin at elevations between 6.8m and 9.35m above sea level (cores MBP1, 2, and 3 at 6.8m, MBP4 at 6.7m, MBP5 at 6.85m, MBP6 at 6.87m, MBP7 at 7.75m, MBP8 at 8.2m, MBP9 at 9.05m, and MBP10 at 9.35m above sea level respectively) (Digerfeldt, 1971). Core MBP1 is closest to the deepest part of the basin, and cores MBP7-MBP10 are located in the margin of the basin (Digerfeldt, 1971). The basal sediments in cores MBP1- MBP6 are silt/sand with gravel and clay. The overlying sediments are calcareous gyttja and coarse detritus gyttja. The uppermost sediments are peat and swamp dy. In the central part of the basin (core MBP1), there is clay gyttja overlying the swamp dy. Digerfeldt (1971) has reconstructed lake-level changes during the Holocene on the basis of changes in lithology, sediment limit and aquatic assemblages following the method described in Digerfeldt (1986). The record of changes in relative depth presented here follows this reconstruction. The chronology is based on pollen correlation with a nearby radiocarbon-dated site, Ageröds mosse (Berglund and Digerfeldt, 1970; Digerfeldt, 1971). A lake-level curve based on the status codings has been presented in Harrison and Digerfeldt (1993). An interval of high water levels before ca 9500 yr B.P. is indicated by a high sediment limit in cores MBP4 and the relatively low content of coarse detritus in the central cores. The presence of humic sand in core MBP9 and MBP10, representing marshy ground often found along lake shores immediately above the high water level (Digerfeldt, 1971), indicates the position of the lake shoreline. A decrease in water level during the late PB and SB1 (around 8500 yr B.P.) is indicated by a sediment limit in core MBP1 and peat deposition in cores MBP2, MBP3 and MBP4 (Digerfeldt, 1971). An increase in the sediment limit to core MBP4 and a decrease in coarse detritus in core MBP1, indicate an increase in water level during pollen zone AT1, ca 6700-5000 yr B.P. A decrease in water level during AT2 and SB1 is indicated by peat deposition in core MBP1. An hiatus in sedimentation in cores MBP2, MBP3 and MBP4 marks the culmination of lowering, ca 4100-2200 yr B.P. A slight increase in water depth during SB2 is indicated by the presence of swamp dy in cores MBP1, MBP2, MBP3 and MBP4. The deposition of clay gyttja overlying the swamp dy in core MBP1, indicates a continuous increase in water level after ca 1100 yr B.P. In the status coding, low (1) is indicated by peat deposition in core MBP1; intermediate (2) by lacustrine sediment in core MBP1 and peat in cores MBP2-MBP4; high (3) by lacustrine sediments above core MBP4 and low content of coarse detritus in the central cores. References Berglund, B.E. and Digerfeldt, G., 1970. A palaeoecological study of the Late-Glacial lake at Torreberga, Scania, south Sweden. Oikos 21: 98-128. Digerfeldt, G., 1971. The post-glacial development of the ancient lake at Torreberga, Scania, south Sweden. Geologiska Föreningens i Stockholm Förhandlingar 93: 601-624. Digerfeldt, G., 1986. Studies on past lake-level fluctuations. In Berglund, B. (ed.), Handbook of Holocene Palaeoecology and Palaeohydrology: 127-144. John Wiley & Sons, New York. Harrison, S.P. and Digerfeldt, G., 1993. European lakes as palaeohydrological and palaeoclimatic indicators. Quaternary Science Reviews 12: 233-248. Coding 10000-9500 yr B.P. high (3) 9500-9100 yr B.P. intermediate (2) 9100-8100 yr B.P. low (1) 8100-6700 yr B.P. intermediate (2) 6700-4800 yr B.P. high (3) 4800-4100 yr B.P. intermediate (2) 4100-2200 yr B.P. low (1) 2200-1100 yr B.P. intermediate (2) 1100-0 yr B.P. high (3) Final coding: June 1989. Coded by GD, SPH and GY Trummen, Sweden Lake Trummen (56 52'N, 14 45'E, 161m above sea level) is a small lake in the central part of the Southern Swedish Upland. The lake has an area of ca 100ha and a maximum depth of 2.1m. There are at least three inflows to the lake and an outlet northwestwards to Lake Växjösjön. The lake level was artificially lowered by ca 0.9m in the 19th century. The annual fluctuation in the water level is ca 0.8-0.9m (Digerfeldt, 1972). The catchment area is ca 1300ha. The bedrock in the catchment is Archaean granites and porphyrites. Two cores from the centre of the lake taken in water depth of 1.70m (main core and complementary core) and a transect of seven cores taken near the western shore in water depths between 0.2m and 1.4m (cores MBP1, MBP2, ... MBP7), provide a sedimentary record back to ca 10000 yr B.P. (Digerfeldt, 1972). The basal sediments are sandy silt and silty clay, grading to clay gyttja and clayey silty gyttja. The overlying sediments are detritus gyttja. The sediment sequences are generally similar in each core. Digerfeldt (1972) has reconstructed lake-level changes during the Holocene on the basis of changes in lithology, sediment limit, aquatic macrofossil and pollen assemblages following the method described in Digerfeldt (1986). The record of changes in relative depth presented here follows this reconstruction (Digerfeldt, 1972). The chronology is base on 30 radiocarbon dates (Digerfeldt, 1972; Håkansson, 1975). A lake-level curve based on the status codings has been presented in Harrison and Digerfeldt (1993). An interval of lowered water level during the late Pre-Boreal period (ca 9400 yr B.P.) is indicated by abundance of reworked minerogenic matter in cores MBP5, MBP6 and MBP7, and an hiatus in sedimentation in cores MBP1, MBP2, MBP3 and MBP4 (Digerfeldt, 1972). An increase in water depth during the Boreal period (ca 8600-7800 yr B.P.) is indicated by a decrease in minerogenic matter in cores MBP5, MBP6 and MBP7, and gyttja deposition in cores MBP1, MBP2, MBP3 and MBP4. The increased sediment limit suggests the lake was ca 1.6-1.7m higher than during Pre-Boreal period (Digerfeldt, 1972). The further decrease in the coarse detrital content of the gyttja in cores MBP1, MBP2 and MBP3 suggests the increase in water depth continued during the early Atlantic. The presence of Trapa natans and Potamogeton with Nuphar and Nymphaea in cores MBP2 and MBP3 is consistent with relatively deep water. An increase in coarse gyttja in cores MBP2 and MBP3 indicates a decrease in water depth during the Late Atlantic. An increase in Schoenoplectus and Equisetum, and a decrease in Trapa natans and Potamogeton is consistent with this interpretation. A continued decrease in water depth during the early Sub-Boreal is indicated by the presence of coarse detritus gyttja in cores MBP4, MBP5 and MBP6, and an hiatus in sedimentation in cores MBP1, MBP2 and MBP3. The decrease in the coarse detritus content of sediments in cores MBP4, MBP5 and MBP6, and lacustrine sedimentation in cores MBP1, MBP2 and MBP3, indicate an increase in water depth during the Sub-Atlantic. The presence of Isoetes in cores MBP4, MBP5, MBP6 and MBP7 is consistent with increased water depth. In the status coding, low (1) is indicated by a sediment limit below core MBP4 and reworked minerogenic matter in the central core; intermediate (2) by a sediment limit up to core MBP3; high (3) by a sediment limit above core MBP1 and low coarse detritus content of the central core. References Digerfeldt, G., 1972. Post-Glacial development of Lake Trummen. Regional vegetation history, water-level changes and palaeoliminology. Folia Limnlogica Scandinavica 16: 96 pp. Digerfeldt, G., 1986. Studies on past lake-level fluctuations. In Berglund, B. (ed.), Handbook of Holocene Palaeoecology and Palaeohydrology: 127-144. John Wiley & Sons, New York. Harrison, S.P. and Digerfeldt, G., 1993. European lakes as palaeohydrological and palaeoclimatic indicators. Quaternary Science Reviews 12: 233-248. Håkansson, S., 1975. University of Lund radiocarbon dates VIII. Radiocarbon 17: 174-195. Radiocarbon dates Lu-224 1000±50 1.250-1.300m detritus gyttja, complementary core Lu-225 1010±50 1.650-1.700m detritus gyttja, complementary core Lu-55 1130±100 2.125-2.175m detritus gyttja, main core Lu-56 1150±100 2.075-2.125m detritus gyttja, main core Lu-226 1340±50 2.050-2.100m detritus gyttja, complementary core Lu-54 2080±100 2.275-2.325m detritus gyttja, main core Lu-227 2480±55 2.300-2.350m detritus gyttja, complementary core Lu-84 2600±100 2.475-2.525m detritus gyttja, main core Lu-192 3120±100 2.750-2.800m detritus gyttja, main core Lu-101 3800±100 3.075-3.125m detritus gyttja, main core Lu-83 4100±100 3.225-3.275m detritus gyttja, main core Lu-59 4210±100 3.325-3.375m detritus gyttja, main core Lu-58 4530±100 3.475-3.525m detritus gyttja, main core Lu-89 5320±100 3.750-3.800m detritus gyttja, main core Lu-57 5450±100 3.875-3.925m detritus gyttja, main core Lu-191 6180±100 4.150-4.200m detritus gyttja, main core Lu-53 7190±100 4.400-4.450m detritus gyttja, main core Lu-52 7480±100 4.500-4.550m detritus gyttja, main core Lu-190 8060±100 4.800-4.850m detritus gyttja, main core Lu-50 8490±100 5.175-5.225m detritus gyttja, main core Lu-51 8530±100 5.125-5.175m detritus gyttja, main core Lu-189 8940±100 5.500-5.550m detritus gyttja, main core Lu-46 9310±110 6.175-6.225m detritus gyttja, main core Lu-47 9320±130 6.125-6.175m detritus gyttja, main core Lu-49 9360±100 5.800-5.850m detritus gyttja, main core Lu-48 9360±100 5.900-5.950m detritus gyttja, main core Lu-45 9650±105 6.550-6.600m detritus gyttja, main core Lu-87 9690±105 6.890-6.940m detritus gyttja, main core Lu-88 9690±110 6.890-6.940m detritus gyttja, main core Lu-207 10230±105 6.940-6.990m clayey gyttja, main core Coding 10000-9700 yr B.P. high (3) 9700-9400 yr B.P. intermediate (2) 9400-8600 yr B.P. low (1) 8600-7800 yr B.P. intermediate (2) 7800-4900 yr B.P. high (3) 4900-4100 yr B.P. intermediate (2) 4100-2600 yr B.P. low (1) 2600-1800 yr B.P. intermediate (2) 1800-1000 yr B.P. low (1) 1000-500 yr B.P. intermediate (2) 500-0 yr B.P. high (3) Final coding: June 1989. Coded by GD, SPH and GY Växjösjön, Sweden Växjösjön (56 52'N, 14 45'E, 161m above sea level) is a small, oligotrophic lake in the central part of the Southern Swedish Upland. The lake has an area of ca 100ha (600m x 1700m) and a maximum water depth of ca 6.5m (Battarbee et al., 1976). The lake receives inputs from Lake Trummen via an inlet on the southwest shore, and an outlet southwards. The bedrock in the catchment is Archaean granites and porphyrites. The lake has been severely polluted by sewage and waste water discharge since the later half of the nineteenth century. This has affected a 30cm thick layer of the bottom sediments (Digerfeldt, 1975). The stratigraphy of the lake deposits has been reconstructed from a transect of 10 cores taken at distances between 125m and 200m from the western shore (cores 125m, 130m, 135m, 150m, 160m, 170m, 175m, 182m, 190m and 200m) (Digerfeldt, 1975). The basal sediments in each core are clay gyttja. The overlying sediments are gyttja. There are four sandy layers (Layers 1, 2, 3 and 4) within the gyttja (Digerfeldt, 1975). The sediment sequences are generally similar in each core. A second transect of six cores (cores BP1, BP2, ... BP6) across the lake centre has been used to study the recent development of the lake (Battarbee et al., 1976). Digerfeldt (1975) has reconstructed lake-level changes during the Holocene on the basis of changes in lithology, sediment limit and aquatic assemblages following the method described in Digerfeldt (1986). The record of changes in relative depth presented here follows this reconstruction. There are 18 radiocarbon dates from core BP1 (Battarbee et al., 1976). However, the dates are either younger than expected or stratigraphically inconsistent as a result of reworking. The chronology is therefore based on pollen correlation with Ageröds mosse (Digerfeldt, 1975). A lake-level curve based on the status codings has been presented in Harrison and Digerfeldt (1993). An interval of lowered water level at the boundary of pollen zone PO/BO1 is indicated by a low sediment limit (Digerfeldt, 1975). A layer of coarse material (Layer 1) with high loss-on-ignition is found in cores 175m, 182m and 190m but disappears in core 200m, indicating a sediment limit below core 190m. The aquatic assemblage is characterised by the absence of Isoetes in core 182m, consistent with shallowing ca 9400-8300 yr B.P. An increase in sediment limit during pollen zone BO2 and the early AT1 is indicated by lacustrine sediment in core 150m and deeper-water cores. A decrease in water level at the boundary of pollen zone AT1/AT2 is indicated by decreased sediment limit (Digerfeldt, 1975). A layer of coarse sandy gyttja with an increased loss-on-ignition (Layer 2) occurs in cores 160m and 175m but is absent from core 182m, indicating a sediment limit below core 175m. A decrease in Isoetes in the central cores is consistent with decreased water depth, ca 6100-5200 yr B.P. An increase in the sediment limit, suggesting an increase in water depth during the late AT2 and SB1, is indicated by the presence of lacustrine sediment in core 150m. A lowered water level around the SB1/SB2 boundary (ca 4100-3300 yr B.P.) is indicated by a lowered sediment limit (Digerfeldt, 1975). A third layer of coarse material, consisting of muddy sand with a high loss-on-ignition, is found in cores 160m and 170m but is absent in core 175m. In cores 175m and 182m Isoetes gradually decreases in abundance and disappears, consistent with shallowing. An increase in water level during pollen zone SB2 is indicated by an increased sediment limit up to core 150m and 135m. A fourth sandy layer, dated to pollen zone SA1, after ca 1800 yr B.P. is present in cores 160m and 170m but absent in core 175m and 182m, indicating that the sediment limit was below core 170m. However the unit does not thin out nearshore between cores 125m and 130m, indicating only moderate shallowing (Digerfeldt, 1975). Lacustrine sediment is well represented at all sites in the transect after ca 700 yr B.P., indicating an increase in water depth. In the status coding, low (1) is indicated by a sediment limit below core 175m, with sandy deposits and low abundance of Isoetes in the central cores; intermediate (2) by moderately low sediment limit in core 160m; (3) by a sediment limit above core 150m, with low loss-on-ignition and moderate abundance of Isoetes in the central cores. References Battarbee, R.W., Coleraine (no initials), and Digerfeldt, G., 1976. Palaeoecological studies of the recent development of Lake Växjösjön. Archiv für Hydrobiologie 77: 330-346. Digerfeldt, G., 1975. Post-Glacial water-level changes in lake Växjösjön, central southern Sweden. Geologiska Föreningens i Stockholm Förhandlingar 97: 167-173. Digerfeldt, G., 1986. Studies on past lake-level fluctuations. In Berglund, B. (ed.), Handbook of Holocene Palaeoecology and Palaeohydrology: 127-144. John Wiley & Sons, New York. Harrison, S.P. and Digerfeldt, G., 1993. European lakes as palaeohydrological and palaeoclimatic indicators. Quaternary Science Reviews 12: 233-248. Radiocarbon dates Lu-734 760±50 15-20cm, core BP 1, RWKD, REJECT Lu-735 1120±55 40-45cm, core BP 1, RWKD, REJECT Lu-736 920±50 65-70cm, core BP 1, RWKD, REJECT Lu-737 630±55 90-95cm, core BP 1, RWKD, REJECT Lu-675 640±55 105-110cm, core BP 1, RWKD, REJECT Lu-676 500±55 125-130cm, core BP 1, RWKD, REJECT Lu-677 450±55 145-150cm, core BP 1, RWKD, REJECT Lu-678 480±55 165-170cm, core BP 1, RWKD, REJECT Lu-679 440±55 185-190cm, core BP 1, RWKD, REJECT Lu-680 610±55 205-210cm, core BP 1, ATY, REJECT Lu-681 770±50 225-230cm, core BP 1, ATY, REJECT Lu-682 970±50 245-250cm, core BP 1, ATY, REJECT Lu-683 980±55 265-270cm, core BP 1, ATY, REJECT Lu-850 1220±60 285-290cm, core BP 1, ATY, REJECT Lu-857 1340±60 305-310cm, core BP 1, ATY, REJECT Lu-858 1400±60 325-330cm, core BP 1, ATY, REJECT Lu-859 1370±75 345-350cm, core BP 1, ATY, REJECT Coding ca 10000-9700 yr B.P. high (3) ca 9700-9400 yr B.P. intermediate (2) ca 9400-8300 yr B.P. low (1) ca 8300-7300 yr B.P. intermediate (2) ca 7300-6300 yr B.P. high (3) ca 6300-6100 yr B.P. intermediate (2) ca 6100-5200 yr B.P. low (1) ca 5200-4100 yr B.P. intermediate (2) ca 4100-3300 yr B.P. low (1) ca 3300-2800 yr B.P. intermediate (2) ca 2800-1800 yr B.P. high (3) ca 1800-700 yr B.P. intermediate (2) ca 700-0 yr B.P. high (3) Final coding: June 1989. Coded by GD, SPH and GY Vielången, Sweden Vielången (56 11'N, 13 10'E, 93m above sea level) is one of a series of inter-connected lakes in hummocky terrain in northeast Skåne (Digerfeldt, 1965). It lies in the same basin as the lake of Farlången. Farlången and Vielången would have formed a single, united lake during former intervals of high water level. The lakes are separated by a distance of only ca 200m. During intervals of lower water level, a small stream flowed between Farlången and Vielången. This natural connection has now been canalised to assist drainage. Vielången is also fed by an inflow from Tuvesjön, to the north, but there is no indication that these lakes were formerly part of the same system. The level of Vielången has been affected by drainage works since the beginning of the 20th century. The lake now has a depth of ca 1-2m (Digerfeldt, 1965). The stratigraphy of the lake bottom sediments has been reconstructed from 17 cores along three transects (Digerfeldt, 1965). One transect crosses the upstream end of Vielången, a second transect runs parallel to the first across the carr that separates Farlången and Vielångan. A third transect runs transversally from the northern shore of Farlängen and out into Vielången. All the cores show a similar stratigraphy, with clay gyttja overlain by gyttja. The uppermost sediments in the cores from the carr are peat. Digerfeldt (1965) has reconstructed lake-level changes during the Holocene on the basis changes in sediment lithology and aquatic macrofossil assemblages. The record of changes in relative depth presented here follows the reconstruction as summarised in Harrison and Digerfeldt (1993). The chronology is based on pollen correlation with the radiocarbon-dated site of Ageröds mosse. The absence of sediments dating to the Preboreal and the first part of the Boreal (BO1) indicates the lake was low during this interval. An increase in water depth in the second half of the Boreal is marked by gyttja sedimentation across the whole basin. At this stage, Vielången and Farlången would have been united to form a single lake. The later Subboreal (SB-2) is represented by a relatively small amount of sediment in the shallow water cores (e.g. core BP6) compared to the deeper-water cores (e.g. core BP8), suggesting a lowering in lake level. This is consistent with a major increase in the importance of Equisetum. A decline in the abundance of Equisetum, and an increase in deeper-water aquatics such as Nymphaea, Nuphar and Potamogeton, suggests a gradual increase in water depth during the Subatlantic. In the status coding, low (1) is indicated by hiatuses in sedimentation; intermediate (2) by gyttja sedimentation; high (3) by lake levels similar to present. References Digerfeldt, G., 1965. Vielången och Farlången. En utvecklingshistorisk insjö-undersökning. Skånes Natur 52: 162-183. Harrison, S.P. and Digerfeldt, G., 1993. European lakes as palaeohydrological and palaeoclimatic indicators. Quaternary Science Reviews 12: 233-248. Coding 9300-8600 yr B.P. low (1) 8600-7900 yr B.P. intermediate (2) 7900-5900 yr B.P. high (3) 5900-4400 yr B.P. intermediate (2) 4400-2000 yr B.P. low (1) 2000-1100 yr B.P. intermediate (2) 1100-0 yr B.P. high (3) Final coding: June 1989. Coded by: GD and SPH Goplo Lake, Poland Goplo Lake, Poland 232 167 Kepa, Poland Kepa, Poland Kolno Lake, Poland Kolno Lake, Poland Kruklin Lake, Poland Kruklin Lake, Poland Lukcze, Poland Lukcze, Poland Steklin, Poland Steklin, Poland Wielke Gacno, Poland Wielke Gacno, Poland Comprida, Portugal Comprida, Portugal Madres, Spain Madres, Spain Padul, Spain Padul, Spain Sanguijuelas, Spain Sanguijuelas, Spain Ageröds mosse, Sweden Ageröds mosse, Sweden Bjäresjö, Sweden Bjäresjö, Sweden Bysjön, Sweden Bysjön, Sweden Juokojauratj, Sweden Juokojauratj, Sweden Krageholmssjön, Sweden Krageholmssjön, Sweden Kroktjärnen, Sweden Kroktjärnen, Sweden Lilla Gloppsjön, Sweden Lilla Gloppsjön, Sweden Ljustjärnen, Sweden Ljustjärnen, Sweden Lyngsjö, Sweden Lyngsjö, Sweden Ranviken, Sweden Ranviken, Sweden Sandsjön, Sweden Sandsjön, Sweden Torreberga, Sweden Torreberga, Sweden Trummen, Sweden Trummen, Sweden Växjösjön, Sweden Växjösjön, Sweden Vielången, Sweden Vielången, Sweden