related to fundamental geophysical- astronomical problems. Late Quaternary 

 data suggest a cyclic pattern of the geoid changes that resembles the 

 precession cycle. Holocene geoid changes- -like correlated magnetic, climate, 

 and volcanic fluctuations- -seem to be caused by changes at the core/mantle 

 interface (bumps and eddies) and coupling. Because of geoid changes, eustasy 

 is not globally valid. (Authors) . 



223 MORNER, N.-A. 1978. "Palaeogeoid Changes and Palaeoecological Changes 

 in Africa With Respect to Real and Apparent Palaeoclimatic Changes , " 

 Palaeoecology of Africa and the Surrounding Islands . Vol 10, Bakker and 

 Coetzee Eds., A. A. Balkema/Rotterdam. 



Paleogeoid changes affect the ocean level configuration and the geoid 

 under the continents which may affect the ground water level. The correlation 

 between pre -Pliocene drought and mammalian extinction levels and general sea- 

 level regressions is explained by palaeogeoid changes instead of a palaeo- 

 temperature changes. The ice age aridity and early Holocene humidity in 

 Africa seem mainly or partly to be the effect of palaeogeoid changes. The 

 late Holocene increasing aridity may be explained in terms of cyclic geoid 

 changes. The aridity at around 115,000 BP (isotope stage 5d) may not at all 

 correspond to a major glaciation period, which would drastically change our 

 base for prediction of future climate. Palaeoecological variations should be 

 analyzed with respect to the possible effect of a palaeogeoid changes in order 

 to separate real and apparent palaeoclimatic changes. (Author). 



224 MORNER, N.-A. 1980. "The Northwest European 'Sea-Level Laboratory' and 

 Regional Holocene Eustasy," Palaeogeographv. Palaeoclimatology . Palaeocology . 

 Vol 29, pp 281-300. 



The northwest European coasts and shelf, including rising, subsiding and 

 semi-stable areas, can be regarded as an immense "sea-level laboratory" where 

 the interaction between eustasy, crustal movements and local paleoenvironmen- 

 tal effects can be analyzed, separated and checked. Central Fennoscandia has 

 risen by 830 m and the North Sea basin has subsided by 170 m in response to 

 the Late Weichselian glaciation. This implies rapid horizontal motions of a 

 low-viscosity asthenosphere . Sea-level oscillations are recorded both in 

 uplifted and subsided areas. The Fennoscandian shorelines are uplifted and 

 tilted, and hence separated so that they can be clearly identified and dated. 

 Each little Postglacial transgression maximum (PTM) is represented by a mor- 

 phologically identified shoreline that has been followed from some 250 km in 

 the direction of tilting in the Kattegat region. The amplitudes of the 

 interjacent regressions are will expressed in the stratigraphy and can be 

 determined with great accuracy. The Kattegat sea- level spectrum offers a 

 "eustatic test area." The eustatic curve calculated from the Kattegat data 

 agrees in such detail with the records from other parts of northwestern Europe 

 (e.g., northwest England, The Netherlands, northern Norway) that it must be 

 concluded that reflects the regional eustatic changes. It is a low amplitude 

 oscillating curve. Local paleoenvironmental effects are sometimes recorded, 

 e.g., in relation to the climatic deterioration at the Subboreal/ Subatlantic 



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