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Differentiation of MIS 9 and MIS 11 in the continental record: vegetational, faunal, aminostratigraphic and sea-level evidence from coastal sites in Essex, UK.

Roe HM, Coope GR, Devoy RJ, Harrison CJ, Penkman KE, Preece RC, Schreve DC - Quat Sci Rev (2009)

Bottom Line: However, the sites can be differentiated on the basis of mammalian biostratigraphy, new aminostratigraphic data, as well as the differences in the sea-level history.The infill of a much later channel, yielding non-marine molluscs and vertebrates including Hippopotamus, appears to have formed during the Ipswichian (MIS 5e).This evidence is compared with other important sites of late Middle Pleistocene age in Britain and elsewhere on the continent and the importance of a multidisciplinary approach is stressed.

View Article: PubMed Central - PubMed

Affiliation: School of Geography, Archaeology and Palaeoecology, Queen's University of Belfast, Belfast BT7 1NN, UK.

ABSTRACT
Multidisciplinary investigations of the vegetational, faunal and sea-level history inferred from the infills of buried channels on the coast of eastern Essex have a direct bearing on the differentiation of MIS 11 and MIS 9 in continental records. New data are presented from Cudmore Grove, an important site on Mersea Island that can be linked to the terrace sequence of the River Thames. The vegetational history has been reconstructed from a pollen sequence covering much of the interglacial represented. The temperate nature of the climate is apparent from a range of fossil groups, including plant remains, vertebrates (especially the rich herpetofauna), molluscs and beetles, which all have strong thermophilous components. The beetle data have been used to derive a Mutual Climatic Range reconstruction, suggesting that mean July temperatures were about 2 degrees C warmer than modern values for southeast England, whereas mean January temperatures may have been slightly colder. The sea-level history has been reconstructed from the molluscs, ostracods and especially the diatoms, which indicate that the marine transgression occurred considerably earlier in the interglacial cycle than at the neighbouring Hoxnian site at Clacton. There are a number of palynological similarities between the sequence at Cudmore Grove and Clacton, especially the presence of Abies and the occurrence of Azolla filiculoides megaspores. Moreover, both sites have yielded Palaeolithic archaeology, indeed the latter is the type site of the Clactonian (flake-and-core) industry. However, the sites can be differentiated on the basis of mammalian biostratigraphy, new aminostratigraphic data, as well as the differences in the sea-level history. The combined evidence suggests that the infill of the channel at Cudmore Grove accumulated during MIS 9, whereas the deposits at Clacton formed during MIS 11. The infill of a much later channel, yielding non-marine molluscs and vertebrates including Hippopotamus, appears to have formed during the Ipswichian (MIS 5e). This evidence is compared with other important sites of late Middle Pleistocene age in Britain and elsewhere on the continent and the importance of a multidisciplinary approach is stressed.

No MeSH data available.


Related in: MedlinePlus

Section A–C showing the lithostratigraphy of the Cudmore Grove channel-fill sequence and overlying sands and gravels (Unit 6). The location of the boreholes is shown in Fig. 3. The position of Unit 3, only a few centimetres thick, at the base of the organic sequence (depicted in black) is indicated. The stratigraphical position of this unit is shown more clearly in Fig. 5. The lateral continuity of sub-units 2c and 2d near boreholes MM6–MM7 is unclear; here the Pleistocene beds are replaced by Holocene estuarine deposits (Fig. 3) which are compositionally similar to the upper part of the Pleistocene channel-fill sequence and locally indistinguishable. Samples for clast lithological analysis (Table 1) were collected from the cliff sections near borehole CG1 (sampling points a, b, c).
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fig4: Section A–C showing the lithostratigraphy of the Cudmore Grove channel-fill sequence and overlying sands and gravels (Unit 6). The location of the boreholes is shown in Fig. 3. The position of Unit 3, only a few centimetres thick, at the base of the organic sequence (depicted in black) is indicated. The stratigraphical position of this unit is shown more clearly in Fig. 5. The lateral continuity of sub-units 2c and 2d near boreholes MM6–MM7 is unclear; here the Pleistocene beds are replaced by Holocene estuarine deposits (Fig. 3) which are compositionally similar to the upper part of the Pleistocene channel-fill sequence and locally indistinguishable. Samples for clast lithological analysis (Table 1) were collected from the cliff sections near borehole CG1 (sampling points a, b, c).

Mentions: With the exception of the sands and gravels exposed in the cliffs, which extend for several kilometres along the coast of Mersea Island (Fig. 3), the entire Pleistocene sequence at Cudmore Grove fills a steep-walled, channel-like depression cut into the London Clay, the ‘Cudmore Grove Channel’ (Roe, 1994) (Figs. 3–5). This feature is at least 0.28 km wide and 0.25 km long and is aligned in a northwest–southeast direction. The southern edge of the channel is well exposed at the base of the cliffs near Cudmore Grove wood and on the foreshore (Fig. 3). Its maximum observed depth was recorded in borehole CG1 at −10.40 m O.D. (Fig. 4). The depth further to the east is unknown, where the Pleistocene beds are truncated by Holocene sediment.


Differentiation of MIS 9 and MIS 11 in the continental record: vegetational, faunal, aminostratigraphic and sea-level evidence from coastal sites in Essex, UK.

Roe HM, Coope GR, Devoy RJ, Harrison CJ, Penkman KE, Preece RC, Schreve DC - Quat Sci Rev (2009)

Section A–C showing the lithostratigraphy of the Cudmore Grove channel-fill sequence and overlying sands and gravels (Unit 6). The location of the boreholes is shown in Fig. 3. The position of Unit 3, only a few centimetres thick, at the base of the organic sequence (depicted in black) is indicated. The stratigraphical position of this unit is shown more clearly in Fig. 5. The lateral continuity of sub-units 2c and 2d near boreholes MM6–MM7 is unclear; here the Pleistocene beds are replaced by Holocene estuarine deposits (Fig. 3) which are compositionally similar to the upper part of the Pleistocene channel-fill sequence and locally indistinguishable. Samples for clast lithological analysis (Table 1) were collected from the cliff sections near borehole CG1 (sampling points a, b, c).
© Copyright Policy
Related In: Results  -  Collection

License
Show All Figures
getmorefigures.php?uid=PMC2806946&req=5

fig4: Section A–C showing the lithostratigraphy of the Cudmore Grove channel-fill sequence and overlying sands and gravels (Unit 6). The location of the boreholes is shown in Fig. 3. The position of Unit 3, only a few centimetres thick, at the base of the organic sequence (depicted in black) is indicated. The stratigraphical position of this unit is shown more clearly in Fig. 5. The lateral continuity of sub-units 2c and 2d near boreholes MM6–MM7 is unclear; here the Pleistocene beds are replaced by Holocene estuarine deposits (Fig. 3) which are compositionally similar to the upper part of the Pleistocene channel-fill sequence and locally indistinguishable. Samples for clast lithological analysis (Table 1) were collected from the cliff sections near borehole CG1 (sampling points a, b, c).
Mentions: With the exception of the sands and gravels exposed in the cliffs, which extend for several kilometres along the coast of Mersea Island (Fig. 3), the entire Pleistocene sequence at Cudmore Grove fills a steep-walled, channel-like depression cut into the London Clay, the ‘Cudmore Grove Channel’ (Roe, 1994) (Figs. 3–5). This feature is at least 0.28 km wide and 0.25 km long and is aligned in a northwest–southeast direction. The southern edge of the channel is well exposed at the base of the cliffs near Cudmore Grove wood and on the foreshore (Fig. 3). Its maximum observed depth was recorded in borehole CG1 at −10.40 m O.D. (Fig. 4). The depth further to the east is unknown, where the Pleistocene beds are truncated by Holocene sediment.

Bottom Line: However, the sites can be differentiated on the basis of mammalian biostratigraphy, new aminostratigraphic data, as well as the differences in the sea-level history.The infill of a much later channel, yielding non-marine molluscs and vertebrates including Hippopotamus, appears to have formed during the Ipswichian (MIS 5e).This evidence is compared with other important sites of late Middle Pleistocene age in Britain and elsewhere on the continent and the importance of a multidisciplinary approach is stressed.

View Article: PubMed Central - PubMed

Affiliation: School of Geography, Archaeology and Palaeoecology, Queen's University of Belfast, Belfast BT7 1NN, UK.

ABSTRACT
Multidisciplinary investigations of the vegetational, faunal and sea-level history inferred from the infills of buried channels on the coast of eastern Essex have a direct bearing on the differentiation of MIS 11 and MIS 9 in continental records. New data are presented from Cudmore Grove, an important site on Mersea Island that can be linked to the terrace sequence of the River Thames. The vegetational history has been reconstructed from a pollen sequence covering much of the interglacial represented. The temperate nature of the climate is apparent from a range of fossil groups, including plant remains, vertebrates (especially the rich herpetofauna), molluscs and beetles, which all have strong thermophilous components. The beetle data have been used to derive a Mutual Climatic Range reconstruction, suggesting that mean July temperatures were about 2 degrees C warmer than modern values for southeast England, whereas mean January temperatures may have been slightly colder. The sea-level history has been reconstructed from the molluscs, ostracods and especially the diatoms, which indicate that the marine transgression occurred considerably earlier in the interglacial cycle than at the neighbouring Hoxnian site at Clacton. There are a number of palynological similarities between the sequence at Cudmore Grove and Clacton, especially the presence of Abies and the occurrence of Azolla filiculoides megaspores. Moreover, both sites have yielded Palaeolithic archaeology, indeed the latter is the type site of the Clactonian (flake-and-core) industry. However, the sites can be differentiated on the basis of mammalian biostratigraphy, new aminostratigraphic data, as well as the differences in the sea-level history. The combined evidence suggests that the infill of the channel at Cudmore Grove accumulated during MIS 9, whereas the deposits at Clacton formed during MIS 11. The infill of a much later channel, yielding non-marine molluscs and vertebrates including Hippopotamus, appears to have formed during the Ipswichian (MIS 5e). This evidence is compared with other important sites of late Middle Pleistocene age in Britain and elsewhere on the continent and the importance of a multidisciplinary approach is stressed.

No MeSH data available.


Related in: MedlinePlus