whereas Heceta Island underwent processes and magnitudes of glaciation and 

 isostatic rebound similar to the Queen Charlotte Islands, Prince of Wales 

 Island was subjected to a pattern of glaciation and isostatic rebound 

 different from that of the Queen Charlotte Islands and mainland of British 

 Coliambia. (Author). 



220 MOORE, S. 1946. "Crustal Movement in the Great Lakes Area," Geological 

 Society of America . Bulletin 59, pp 697-710. 



The crustal movement in progress at the present time has been determined 

 at 106 points in the Great Lakes area. The entire area, except for the 

 extreme northerly part of Lake Superior, is subsiding with respect to sea- 

 level. The methods employed and the results obtained are discussed, but no 

 conclusion as to the cause of the movement is reached. (Author) . 



221 MORNER, N.-A. 1973. "Eustatic Changes During the Last 300 Years," 

 Palaeogeographv. Palaeoclimatology . Palaeoecology . Vol 12, No. 1, pp 1-14. 



Tide gages in rising and subsiding areas show a major change in the 

 shore -level displacement at about A.D. 1840, caused by the onset of a rapid 

 eustatic rise. Comparisons between information from Amsterdam, Stockholm and 

 Warnemunde provide material for the reconstruction of the eustatic changes 

 during the last 290 years. Relative uplift data from the Swedish west coast, 

 corrected according to the eustatic curve established here, give the same 

 location of the isostatic zero isobase as does the geological material for the 

 last 7,000 years. The eustatic changes closely follow climatic changes. A 

 rapid eustatic rise started about 1840, showed down about 1930 and ended about 

 1950. Knowing the eustatic factor, the isostatic (or tectonic) factor is cal- 

 culated for different areas of importance in the discussion of Holocene eus- 

 tatic sea- level changes. (Author). 



222 MORNER, N.-A. 1976. "Eustasy and Geoid Changes," Journal of Geology . 

 Vol 84, No. 2, pp 123-151. 



The real ocean surface -the equipotential surface of the geoid or the 

 geodetic sea- level -is rough and uneven and characterized by humps and 

 depressions of several ms . The present geoid configuration cannot have 

 remained stationary back in time. The main question is over what time units 

 geoid changes may have played a significant role. The instability of the 

 geoid configuration has not been considered previously. The geoid may change 

 both horizontally (geographical dislocation of the geoid relief) and verti- 

 cally (magnitudinal changes in relief) . There are numerous variables (during 

 different geological time units) that must have affected the geoid. Geoid 

 changes must certainly have occurred during the Phanerozoic and the Late Qua- 

 ternary. Holocene "eustatic" data also yield indication of geoid changes. 

 Tide gage data and Holocene eustatic short-period fluctuations seem to indi- 

 cate geoid changes even during short-period time units. Geoid changes are 



101 



