86 
REPORT-1847* 
diagram (fig. 15.). CH represents the surface of the sea; BjH the sa 
bottom to the coast line through H; DK the lower surface of the soW 
Fig. IS. 
I 
I 
crust. 
wave 
at ^ QP9^> are the directions of propagation of the 
refracted in of those lines respectively, and show how the ware iJ 
fronts of the^wlT® meilium into another. The conaeculire 
directions nrovi J^preai-nted by tile curved lines, which meet all tli« 
these three^medi'r^n^ «»entioned «t right .'ingles. It is supposed tlifth ‘® 
in the solid crus? a Ifi propagation is least in the water, great^ 
served that »o the subjacent fluid, it will be obj 
reach the shore IT *1^ (the reflected waves are not here noticed)*'^ 
instant. ' tlirough the solid crust and through the sea, at the same 
sphere is not m!a1^ from J^isiKtrltanoes of lehich the 
restricted to a smiiil considered the original ilisWrbaiict 
suppose the dUturbanrn^e vi'too great intensity. let us wu 
the earth s cruet of^ simultaneously beneath a portion rf 
®o>all, we shall hrve th "*^ i" 
permanent elevatiio. u considerwl (Sect. I. Part II.),« 
tensity be so sniall that superincumbent crust If th*®: 
lie produced, the fi^nt of It, a wave 
area of dislurbauco will i ^**^-**’ situated Teiiically ^ 
the crust situated bevond^i^!^** hori2outal; while in the j»ortioDS<n 
surface of which, after w haJ‘h T®' 
a general concepUon Imn. *^**'‘^' will not be difficult to 
manifestly reach all points^,disturbed area the wavcinw^ 
)vhat I have called same instant* 
mfinitely great. Content immontal velocity of propagadon wooM be 
'vould afftrd the stronS observed over ^ extensive f* 
flisturbaticc, though it woutrh^ •'«*^i'-oijtal extent of the on^ 
mice of greater infen^tv r ^ he necessary to bear in mind tbata disturt' 
^upth, might produce m Ul “ smg>e centre at a much gteaf*^ 
vvhich a verbal \tuc ihfl the region around the 
It is i„ those disturblnce should 
ases in which the area of original disturbance is 
