(I)
c:
.2 .2
(;i
c:
u «
Subsurface flow
l60cm
(I)
(I)
c:
c:
o
0
'; j
'c
6 «
239
Fig. 17.1. Volume-weighted mean concentration of main cations and anions by depth in the soil
water collected from zero-tension lysimeters at a Prades and from throughflow collectors at
b Montseny. Samples are from June 1990 to July 1991 at Prades after Poch (1992), and from May
1985 to May 1988 at Montseny after Avila et al. (1995). Alkalinity was not analyzed at Prades
complexed in soil water but that were included in the atomic absorption determinations. In deep subsurface flow at Montseny, both alkalinity and the
anion deficit were drastically reduced (Fig. 17.1b), probably because the involved organic compounds had been retained or metabolized in the soil. At
Prades, where alkalinity was not analyzed in gravitational water, the anion
charge deficit accounted for more than 50% of the total cation charge at all
depths, and also decreased with depth (Fig. 17.1a). Studies in temperate for-
c:
.2 .2
(;i
c:
u «
Subsurface flow
l60cm
(I)
(I)
c:
c:
o
0
'; j
'c
6 «
239
Fig. 17.1. Volume-weighted mean concentration of main cations and anions by depth in the soil
water collected from zero-tension lysimeters at a Prades and from throughflow collectors at
b Montseny. Samples are from June 1990 to July 1991 at Prades after Poch (1992), and from May
1985 to May 1988 at Montseny after Avila et al. (1995). Alkalinity was not analyzed at Prades
complexed in soil water but that were included in the atomic absorption determinations. In deep subsurface flow at Montseny, both alkalinity and the
anion deficit were drastically reduced (Fig. 17.1b), probably because the involved organic compounds had been retained or metabolized in the soil. At
Prades, where alkalinity was not analyzed in gravitational water, the anion
charge deficit accounted for more than 50% of the total cation charge at all
depths, and also decreased with depth (Fig. 17.1a). Studies in temperate for-