526 
THE  ADMIEALTT  ASTEOXOZ^nCAL  EXPEEEMEXT 
And  thus  for  August  30 : — 
Temperature 
Dew-point 
Height  in 
reduced  to 
mean  of 
depression 
reduced  to 
Humidity, 
saturation 
Wind. 
Clouds. 
feet. 
twenty-four 
mean  of 
= 100. 
hours. 
twenty-four 
Velocity. 
hours. 
Direction. 
Upper. 
Lower. 
miles  per  hour. 
13 
7&-8 
6-8 
80 
0 
10  r> 
304 
75-6 
6-6 
81 
— 
— 
839 
74-1 
6-6 
81 
1,435 
73-2 
6-1 
82 
1,837 
72-7 
5-8 
83 
— 
r 
Xear  level  of 
2,292 
73-0 
5*6 
83 
0 
50  <i 
L 
> 
cloud,  but  it 
is  dispersing. 
3,460 
74-1 
6-9 
80 
0 
cl 
ot  O 
Dense  to  sea- 
ward. 
3,696 
75-4 
6-3 
82 
30 
4,157 
76-7 
14-4 
62 
0 
5 O 
Dense. 
4,769 
75-7 
10-5 
71 
1 
N.w. 
7 O 
— 
5,160 
73-9 
20-5 
51 
1 
N.W. 
70 
— 
5,904 
71-9 
26-4 
41 
0 
70 
— 
6,521 
70-2 
24-4 
44 
1 
N. 
70 
— 
6,875 
69-0 
25-3 
43 
1 
N, 
5 n 
— 
7,234 
64-9 
23-3 
46 
3 
N. 
5 o 
— 
7,792 
67-9 
25-3 
43 
3 
S.W. 
5 o 
— 
8,260 
65-2 
21-8 
48 
4 
s. 
0 O 
— 
8,976 
60-5 
19-7 
51 
3 
S.W. 
5 O 
— 
9,662 
52-8 
13-0 
64 
1 
S.W. 
3 0\_\ 
— 
10,710 
47*4 
7-2 
78 
2 
S.W. 
3 \and  O 
— 
Cloud  on  Peak 
or  close  above 
station. 
These  quantities  are  likewise  exhibited  in  the  Plates  XXXVIII.  and  XXXIX. 
The  first  result  deducible  from  the  two  preceding  Tables,  is  the  remarkable  confiinia- 
tion  which  they  give,  of  Mr.  Welsh’s  discovery  in  his  balloon  ascents,  of  a break  m,  or  a 
very  great  anomalous  deviation  from,  the  law  of  decrease  of  heat  ndth  the  elevation,  at  a 
height  of  a few  thousand  feet  above  the  sea.  The  reason  of  this  anomaly  seems  to  be  indi- 
cated at  the  same  time ; for  it  occurs  not  at  any  passage  from  one  wind  to  another,  not 
at  any  break  in  the  slope  of  the  mountain,  but  at  the  level  of  the  cloud  stratum.  This 
is  the  only  noteworthy  circumstance  that  can  be  found  accompamdng  the  de'^iation  from 
the  law,  and  may  arise  partly  from  the  reflexion  of  heat  by  the  brilliant  upper  sm-face 
of  the  cloud,  and  partly,  as  suggested  by  Mr.  Welsh,  in  connexion  with  the  coiiA  ersion 
of  latent  into  sensible  heat,  dependent  on  the  condensation  of  vapom  into  cloud.  In 
either  case,  the  practical  result  is  the  same ; viz.  that  at  any  moderate  height  above  the 
clouds,  the  temperature  of  the  air  is  by  no  means  so  low  as  might  have  been  computed 
from  the  usual  hypsometric  idea  of  gradation. 
The  second  result  is,  further  confu-mation  to  Gkeen’s  and  Sabine’s,  of  Daniell’s  con- 
clusion of  dryness  above  the  cloud  stratum.  From  the  sea-level  to  the  clouds,  3000  feet 
high,  the  depression  of  the  dew-point  is  small,  but  immediately  after  passing  that  height 
