302 !• RID I JOK NANSKN. M.-.\. Kl. 



ice masses is in excess of llie lo.-ul correspoiulinj^' lo llie amount of depres- 

 sion. After llial lin. c an upluaxal of ilic criisl will {gradually bej^'^in. 



Me.anwlnlc- an n|)li(a\al of llic land will slarl in tlie outer zone of 

 the previously ice-coxcred rej.;ion, soon aflcr il has hecn left free 1)V the 

 retreatinj,*- ice. This n])hca\al may he facilitated h\ a double "unrlertow" 

 of mailer coniinj; from tin- still suhsidinj^ area inside, imder the ice-cap, 

 as well as from tlie iipliea\'ed peripheral /.one (the npheaved wave) outside, 

 as is indicated in h'i^'. 170, III. This ma\ possihh' hast- been wliat hap- 

 pened during the periofl before the Tapes-Litlorina period in tlie regions 

 of Skagen and Kalmar, &c. (cf. above p. 284). 



When tlie upln'a\al of the more central area began, an undertow of 

 matter leewards this rising area from the surrounding previously upheaved 

 zone would arise, and this wcaild cause a sinking of tlie lanrl in that zone 

 (Fig. 170, 1\'), C(>rresi)()nding to the previously mentioned sinking of the 

 land in the region of Skagen and Kalmar, Arc. (cf. \). 284), before or at 

 the beginning of the Tapes-Littorina period. 



As, however, the uphea\al of the depresserl area advanced, the under- 

 tow of matter from the ])erii)heral, formerly Uj)h'-aved regions (outside 

 the ice-cap at its widest extent) would be increased, and a general upheaval 

 of the whole depressed region would be developed, and this woulrl now 

 continue, till the upheaval was coiupleted. At the same time, the lanrl in 

 the peripheral, formerly upheaved zone, surrounding the ice-covered region, 

 woulrl gradually sink. 



Where the retreating ice-cap was to some extent replaced by a trans- 

 gressing sea, the upheaval of the crust would be retarded, as was previously 

 pointed out (cf. p. 280). 



It seems to me. that a development as here inrlicated agrees well with 

 what we now know about the late-glacial and postglacial crustal move- 

 ments wdiich prol)al)ly have taken place in Fenno-Scandia and the sur- 

 rounding regions. 



Along the coast of Norway, where the retreat of the margin of the 

 ice-cap was verv much slower c. g. than in Southern .Sweden and in Den- 

 mark, and where the ice remained near the coast till late-glacial times, 

 the crustal movements have probably been less complicated, and the up- 

 heaval may have been fairly continuous froiu its beginning. 



In regions where the ice-cap left great quantities of moraine material, 

 as for instance in Denmark and in Northern Germany, the crust was 

 naturallv depressed by the weight of these deposits, and this fact would 

 also cause a sinking of the land which may have continued long after the 

 ice retreated. The quantity of moraine material, however, carried by the 

 last ice-cap, may probably not have been very great, and the sinking of 

 the land thus caused after the last glacial period may, therefore, have 

 been less considerable than after the previous glacial periods. 



