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Evidence for solum recarbonation following forest invasion of a
grassland soil
Fuller, L. G.; Wang, D. L.; Anderson, D. W.
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Evide nc e for solum re c a rbona t ion follow ing fore st inva sion of a
gra ssla nd soil
N R C C - 5 0 8 2 4
F u l l e r , L . G . ; W a n g , D . L . ; A n d e r s o n , D . W .
M a y 1 9 9 9
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Canadian Journal of Soil Science, 79, pp. 443-448, May 17, 1999
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Evidence for solum recarbonation following forest
invasion of a grassland soil
L. G. Fuller
1,D. Wang
2,and D.
W.
Anderson
21
AXYS Environmental Consulting Ltd., Calgary, Alberta, Canada T2P 3E7; 2Department of Soil Science,
University of Saskatchewan, Saskatoon, Saskatchewan, Canada S7N 5A8. Received 22 January 1998,
accepted
17May 1999.
Fuller.L.G., Wang, D. and Anderson, D. W. 1999. Evidence for solum recarbonation following forest invasion of a grassland
soil. Can.1. Soil Sci. 79: 443-448. Calcareousｯｲｧ｡ｮｩ｣Ｍｭ｡ｴｴ･ｲｾｲｪ｣ｨ Black Chernozemic soils often persist under poplar forests in Saskatchewan, not acquiring the Ae horizons and related properties more characteristicof GrayLuvisol soils. These are Rego Black Chemozems, locally tenned "Wooded Calcareous" becauseof the occurrence ofa dark. calcareous horizon (AC) at depths of 10 to
30 em. We hypothesize that dark, calcareous horizons are fonner 8m horizons that have been recarbonated because of intense
bio-cycling of Ca by aspen(Popu/us tremu/oides). The comparatively small amounts of carbonate occur mainly in the fine silt and
clay fractions, and are dominantly calcite, indicating secondary origin, in comparison to the carbonate minerals of the Ck horizons where both calcite and dolomite occur, the latter more common in coarse fractions. The ol3C valuesof thecarbonate minerals indi-cate that virtually all the carbonate in fine fractionsof theupper horizonsof theWooded Calcareous soil is pedogenic. The dom-inance of pedogenic carbonate in the Ahk and AC horizons of the Wooded Calcareous soil is consistent with a secondary enrichment, a probable result of increased biocycling of Ca where aspen grows on sites with large amounts of soluble Ca in the subsoil. High concentrations of soluble Ca2+and 5°42- in the LFHof theWooded Calcareous are consistent with increasing｢ｩｯ｣ｹｾ clingof theseions. from a gypsum·rich subsoil.
Keywords: Pedogenic carbonate, prairie-forest transition, stable carbon isotopes, biocycling,a13cvalues
)
FuJler,L.G., Wang, D. et Anderson, D. W. 1999. Signe de recarbonatation du solum apres lnvasion dela foret dans un sol
de prairie. Can. J.Soil Sci. 79: 443-448. Les sols noirs, calcaires, riches en matiere organique persistent souvent sous foret de peupliers en Saskatchewan (Canada) et n'aquierent pas les horizons Ae et lesｰｲｯｰｲｩ･ｵｾｳ correspondantes plus typiques des luvi-sols gris. Ce sont des luvi-solsnoirs Rego, appeles iei "luvi-sols calcaires boises" it cause de la presence d'un horizon ca1caire fonce (AC)
a
la profondeur de lOa30cm. Notre hypothese est que cet horizon calcaireet un ancien horizon8Mqui a ete recarbonate a cause des intenses biotransformations du Ca par Ie peuplier faux-tremble(Populus tremuloides). Les relativement petites quantites decarbonate que I'on retrouve surtout dans la fraction limon et la fraction argile consistent essentiellement en calcite, signe d'une origine secondaire, par comparaison avec les carbonates mineraux associes aux horizons Ck qui comprennent a Ja fois Ie calcite et la dolomite, cene derniere etant plus frequente dans les fractions grossieres. Les valeurs
a
13c
des mineraux carbonates montrentque tous les carbonates trouves dans les fractions fines des horizons superieurs des sols calcaires boises sont d'origineｰ･､ｯｧ･ｮ･ｾ
tique. La predominance de carbonate pedogenetique dans les horizons Ahk et AC des sols calcaires boises s'accorde avec I'hy-pothese d'un enrichissement secondaire, resultat probable d'une transformation biologique intense de Ca, litOUIe tremble pousse sur des emplacements it sous-sol riche en Ca soluble. Les fortes concentrations de Ca2+et deSOi- dans I'horizon LFH de ces sols concordent avec 1a transfonnation biologique de ces ionsIipartir d'un sous-sol riche en gypse.
Mots cles:Carbonate pedogenique. transitionｰｲ｡ｩｲｩ･ｾｦｯｲ･ｴＬ isotopes de carbone stables, transfonnation biologique, valeurs
a
l3c
The movement of forest vegetation onto prairie generally results in the alteration of the prairie soil as Chernozemic soils are progressively transfonned into leached, acidic Gray Luvisols. This, however, can only be the case where the eluvial regime of the landscape pennits sufficient base removal and clay translocation. Forested soils exhibiting characteristics similar to ehernozemic soils have been doc-umented in various portions of the Aspen Parkland. These soils have high organic matter and base contents, which is more characteristic of Chernizemic soils than of Luvisolic soils (Mitchell et al. 1950; Fuller and Anderson 1993).
The presence of high base status, dark-colored forested soils has been attributed to drainage characteristics of the site in question (Sanborn and Pawluk 1983; Pettapiece )1969). Where drainage is imperfect or is to some degree
443
restricted, the development of strongly leached Gray Luvisols does not occur. The occurrence of high base status soils under aspen forest has recently been described (Fuller and Anderson 1993).
Calcareous soils occurring under forest vegetation have been referred to as "Wooded Calcareous" soils in the early soil surveys in Saskatchewan (Mitchell et al. 1950). These soils are classified as Rego Black Chernozem by the Canadian System of Soil Classification (Soil Classification Working Group 1998). The Wooded Calcareous soils appear to be a distinctive kind of soil, not merely a young soillaek-ing well-developed horizons or a soil where development is limited by highly calcareous parent materials. Evidence for this postulate includes the high base status, organic matter and nutrient contents that persist under forest.
444 CANADIAN JOURNAL OF SOIL SCIENCE
Table1.Whole soli carbonate content of the Wooded Calcareous (Rego Black Chernozem) and Orthic Black Chernozem solis and the distribution of carbonates in the coarse (5-2000 llm) and fine « 5 /lm) particle size fractions urthe Wooded Calcareous soils
Depth Whole Soil Coarse Fine Coarse/fine Horizon (em) -(gCaC03equivalent kg-I)- ratio
Ahk 10-20 42 9.5 12 0.8 AC 20-l0 100 22 41 0.5 Ck l0-40 132 32 74 0.4 Csc, 5Q-60 320 176 Il7 1.3 Csk 200-225 238 179 40 4.4
%
pedogenic carbonate=[(813C I - 813Cp )/ 13 13' sampe In (8 Cpedogenic - 8 Cpm)] x 100 (I) Where 81lC m Ie=
81lC value for carbonates of the bulk soil sample,ＸＡｾ｣［ＬＮｦＧｬ
=813C value for parent materialCar-bonates (-0.6%0), 8 3Cpedogenic= 8 1lC value for pedogenic carbonate (-10.0%0).
The stable C isotopic composition of the primary carbon-ate minerals in the parent mcarbon-aterials (deep Ck horizon) was determined to be -0.6%0. For the stable C isotopic composi-tion of the pedogenic carbonate, it was assumed that soil is an open system (Margaritz and Arniel 1980), all the newly formed carbonates are in the form of calcite or Mg-bearing calcite (Rostad and St. Arnaud 1970; 51. Arnaud and Herbillon 1975; 5t. Arnaud 1979), and the 8 1lC values of
contents in each size fraction converted to CaC03 equiva-lent in the size fraction, and then using particle size data expressed on a total soil basis. The coarse carbonate sizes were considered to be the sand, coarse silt, and medium silt, whereas the clay and fine silt fractions constituted the fine carbonate. X-ray diffractograms were prepared using Cu Ka radiation at a scanning speed of 3° min-Ion a Rigaku X-ray diffraction system.
Soluble cations and electrical conductivity (EC) were determined on extracts of a I: I soil to water mixture. Soil <2 mm was used for these determinations. Soluble Ca and Mg were determined by atomic absorption spectroscopy, soluble Na and K by flame emission spectroscopy. Soluble Cl- and SOl- were determined by liquid chromatography.
Stable C isotopic compositions were measured by the method of Rask and Schoenau (1993). Carbonate-C was converted into CO2by adding H3P04 to the sample under vacuum in a Y-shaped reaction chamber. The CO2evolved from the sample was purified in a cold trap system and sealed in a Pyrex glass tube. 81lC value of the evolved CO2 was measured on a VG-SIRA 12 mass spectrometer. The isotopic data are presented in 8 notation as a relative devia-tion from the Pee Dee belemnite (PDB) internadevia-tional stan-dard (Craig 1957). Percent pedogenic carbonate was calculated using Equation I (Salomons and Mook 1976).
282 264 30-40 4Q-60 Orthic Black Ck1 Ck2
MATERIALS AND METHODS
Two soils were obtained for this study from east-central Saskatchewan on a gently undulating till plain near the base of Last Mountain: (I) Rego Black Chemozem (hereafter termed the "Wooded Calcareous" soil; and, (2) Orthic Black Chemozem. Both soils were developed from calcareous till deposits and are included within the Oxbow soil association. Detailed physical and chemical analyses of these soils as well as site descriptions are found elsewhere (Fuller and Anderson 1993). The Orthic Black Chemozems were found under native prairie grasses just outside the forest. Within the forested area, which surrounds a local recharge depres-sion, the soils on planar, gentle slopes were calcareous with no B horizon development, occurring in landscape positions similar to those where Orthic profiles are found. These soils are not simply examples of strongly carbonated Rego Black or "rego ring" soils commonly found encircling recharge wetlands. The Wooded Calcareous soils occur above the rego rings, and have a dark-colored horizon 10 to 20 em thick between the Ah and Ck horizon, termed an AC hori-zon. The forest boundary generally coincides with the boundary between the Orthic Black and Wooded Calcareous profiles. Based on these observations it was hypothesized that migration of forest vegetation onto Black soils under prairie results in recarbonation of the solum (Fuller and Anderson 1993). To test this hypothesis, analysis of the par-ticle size disttibution of the carbonates, the mineralogy of the carbonates and the 813C values of the carbonates were determined for the calcareous horizons of the Wooded Calcareous soils (Ahk, AC, Ck, esca) and compared to the Ck horizons of the Orthic Black Chemozem.
The soil samples were dispersed by ultrasonic vibration for 30 min, then separated into sand (2000-50 Jlm), coarse silt (50-20 Jlm), medium silt (20-5 JlIl1)fme silt (5-2 Jlm) and clay «2 Jlm) (Rostad and St. Arnaud 1970). All size fractions were dried 5Q-60°C to prevent destruction of the carbonates. Inorganic C was determined on each size frac-Stable carbon isotopic methods have been used to study the presence and content of pedogenic carbonate in soils containing both pedogenic and lithogenic carbonates (Salomons and Mook 1976; Margaritz and Amiel 1980; Rabenhorst et a1. 1984; Amundson et a1. 1989). This approach presumes that the enrichment of IlC is 10.0 to 14.6%0 in the pedogenic carbonate relative to soil organic matter in soils of arid and semi-arid climatic regions. More recent studies have shown that fractionation can result in a 13.5 to 16.5%0 higher 81lC value for pedogenic carbonate relative to soil organic matter in the temperature range of 0 to 25°C (Cerling and Quade 1993). The isotopic methods show promise as a means to quantitY pedogenic carbonates in soils of Western Canada (Wang and Anderson 1998).
The objective of this study was to investigate the nature of the carbonate minerals in a Rego Black Chemozem (or Wooded Calcareous soil) using mineralogical and isotopic methods in order to understand the relationship of carbonate mineralogy to soil-landscape processes.
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40-60emDepth 28 30 32 lO"Cu-Ka 3D 32 ZO" Cu-KaOrthic Black Chernozem
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ｾ D I 10"Cu-Ka..
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20<IDemDepthWooded Calcareous (Rego Black Chemozem)
28 30 32 m !l D
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I 10'" Cu-Ka 10-20anDepth 28 30 32 ｾ Oay Fine Silt Medium Silt CoarseSilt,.' ,
446 CANADIAN JOURNAL OF SOIL SCIENCE
Table 2. Stable carbon Isotopic composition and the percentage of pedogenic carbonate calculated in each particle size fraction
Clay Fine silt Medium silt Coarse silt
Sample 013cz PC' B"C PC S13C PC OllC PC Wooded Calcareous Ahk -9.7 96.8 -10.0 100 -7.8 76.6 -6.5 62.8 AC -9.3 92.6 -8.0 78.7 -5.7 54.3 -3.9 35.1 Ckl -9.4 93.6 -6.6 85.1 -7.3 71.3 -5.5 52.1 Ck2 -7.9 77.7 -6.5 62.8 -6.4 61.7 -5.2 48.9 Csea -6.1 79.8 -7.0 68.1 -4.3 39.4 -3.0 25.5 Orlhic Black Ckl -7.7 75.5 -6.6 63.8 -2.1 16.0 Ck2 -6.0 78.7 -6.0 57.4 -2.9 24.5 -2.2 17.0
zODe values are expressed in%0.
ype represents percentageof pedogeniccarbonate expressed relative to the total carbonate in the particle size fraction.
factors of 16.0%. relative to the oJJC value of soil organic matter (Cerling and Quade 1993). A oJJC value of -26.00/00 for soil organic matter was determined for similar soils adja-cent to the study area (Wang and Anderson 1998).
RESULTS AND DISCUSSION
The Ahk, AC, Ck I, Csca, and Csk of the Wooded Calcareous profile were studied. The ratio of coarse carbon-ate to fme carboncarbon-ate increases from less than I near the sur-face to greater than 4 in the Csk horizon (Table I). There is a greater proportion of clay and fme silt sized carbonate in theAhk,AC and Ckl horizons. Secondary carbonates occur mainly as calcite in the fme silt and clay fractions, while pri-mary or lithogenic carbonates tend to be more coarse (Rostad and St. Arnaud 1970).
Precipitation of carbonate in the soil preferentially occurs as calcite rather than dolomite (Doner and Lynn 1977); however, Mg impurities may occur in the pedogenic calcite (St. Arnaud and Herbillon 1975). If the carbonates in a size fraction are secondary there will be a greater proportion of calcite relative to dolomite. The X-ray diffractograms show that the finer fractions of the AC, Ckl and Csca horizons contain more calcite than dolomite, consistent with a sec-ondary origin for the carbonates (Fig. I). The absence of dolomite in the surface horizons of the Wooded Calcareous and the increased intensity of the dolomite peaks in the medium silt and coarse silt fractions within deeper horizons, as well as the Ck horizons of the Orthic Black are evidence that dolomite has been removed via weathering from the surface horizons of the Wooded Calcareous soil (Fig. 1).
The results of the stable carbon isotopic analysis show that the clay fractions tend to be comprised of a greater pro-portion of pedogenic carbonate than the coarser fractions (Table 2). This is true for all calcareous horizons of the Wooded Calcareous and Orthic Black soils. The Ahk, AC and Ck 1 horizons of the Wooded Calcareous possess fine carbonate fractions comprised primarily of calcite of pedo-genic origin.
The distribution of carbonates in particle size fractions, the dominance of calcite and the isotopic analysis indicate the secondary nature of the carbonate in the Ahk, AC and Ckl horizons of the Wooded Calcareous profile. These
cal-carbonates following forest invasion as have soils typical of upland forests (Fuller and Anderson 1993), but rather have experienced a gain in secondary calcite within the solum. Mitchell et al. (1950) suggest that the presence of calcium carbonate and imperfect drainage in the Wooded Calcareous soils appear to have prevented the development of leached Luvisolic soils under forest. Wooded Calcareous soils are most common under forest and are not reported under prairie (Mitchell et al. 1950). The soils under grassland sur-rounding the Wooded Calcareous soils have carbonate-free Bm horizons, whereas B horizons are absent in the Wooded Calcareous soils. The absence of dolomite in fine carbonate fractions in the surface horizons combined with an increas-ing presence of dolomite with depth in the Wooded Calcareous soil suggests that at one time these soils pos-sessed a lime-free solum if the parent material was indeed a uniform deposit. Therefore, there appears to have been a recarbonation of the Bm horizons as a result of carbonate precipitation in the forested soils. The loss of lime-free B horizons by precipitation of calcite crystals has been shown previously where the destruction of argillic horizons has . been attribted to the growth of calcite crystals (Gile and Grossman 1968; Allen and Goss 1974).
Data for grass opal content in the study soils indicate a recent invasion of grassland at the study site, suggesting that changes may occur rather rapidly (Fuller and Anderson 1993). The precipitation of calcium carbonate may be par-tially responsible for the preservation of the C, Nand P observed in this forested soil through sequestration in organic matter (Duchaufour 1982) and precipitation of acid-extractable calcium phosphates (Fuller and Anderson 1993). The origin of this secondary calcite may be related to the ability of aspen to cycle Ca from the subsoil. Poplar species, including aspen, are known to have a greater demand for calcium relative to other forest species (Alban 1982). The greater electrical conductivity in the Csca horizon, visual identification of gypsum at 50 to 80 cm, and accumulations of sulfate and Ca in the leaflitter ofthe Wooded Calcareous soil suggest that Ca is being returned to the surface from a source of soluble Ca at depth (Table 3). The presence of gypsum at 50-60 cm would provide a soluble source of Ca that could be recycled by the aspen. The common
occur-FULLER ET AL. - CALCAREOUS SOILS UNDER FOREST VEGETATION 447
Table 3. Electrical conductivity and soluble ions for horizons of the Orthic Black Chernozem and Wooded Calcareous (Rego Black Chernozem) soils
ｾＬ
EC Ca2+ Mg2+ Na' K' CI S042
Depth (dSm-') (mg L-') (mg L-') (mg L-') (mgL-') (mg L-') (mg L-')
Soil/Horizon (em) Mean SE' Mean SE Mean SE Mean SE Mean SE Mean SE Mean SE
Wooded Calcareous (Rego Black)
LFH 4--0 2.60 0.30 415 50 125 16 8.3 0.4 132 11 11 1 512 217 Ah 0--10 0.97 0.05 167 10 35 2 6.2 3.0 62 3 3.9 0.1 28 1 Ahk 10--20 0.66 0.01 114 1 22 1 2.1 0.2 34 2 2.5 0.3 15 1 AC 20--30 0.58 0.02 98 2 20 1 2.7 0.9 28 1 1.8 0.1 19 1 Ck1 30--40 0.52 0.Q3 82 5 19 5 1.4 0.2 19 1 2.1 0.3 12 1 Ck2 40--50 0.63 0.12 108 25 24 5 3.7 0.7 15 I 1.8 0.2 151 85 Csca 50--60 2.40 0.01 635 6 37 1 19.7 0.7 25 I 1.8 0.2 1580 8 Or/hie Black Ahl 0--10 0.96 0.02 139 5 38 I 3.0 0.2 59 2 11 1 18 I Ah2 10--22 0.54 0.02 69 3 22 2 1.6 0.1 31 I 2.5 0.2 9.1 0.5 8m 22-33 0.44 0.Q3 60 6 19 1 2.2 0.2 16 I 3.5 0.3 10 I Ck1 3l-48 0.35
om
51 2 12 1 3.2 0.4 16 I 1.4 0.2 12 1 Ck2 4&--60 0.78 0.29 152 74 15 4 4.1 0.9 23 3 1.4 0.1 340 211SErepresents the standard error of the mean of four field replicates.
the development of the Wooded Calcareous soils through Ca-cycling and subsequent precipitation of secondary calcite.
The occurrence of the Wooded Calcareous is likely related to their proximity to the adjacent recharge depres-sion with Luvic Gleysol soils (Fuller and Anderson 1993). Strong recharge within the depression and lateral movement of water from beneath the depression to the Wooded " Calcareous soil may well be responsible for the presence of )ypsuminthe subsoil. Knuteson et al. (1989) have shown that soil water may move from depression-focussed recharge areas to the subsoil of adjacent soils resultingin precipitation of pedogenic calcite. This process was also postulated by Sobecki and Wilding (1983). Precipitation of secondary gypsum in the subsoils of soils adjacent to recharge depressions has also been shown by Steinwand and Richardson (1989) in North Dakota. The genesis of the Wooded Calcareous soil, however, involves mOre than just a "rego-ring effect". It is a combination of hydrological processes and enhanced calcium biocycling by the aspen. Lateral movement of water and capillary rise, coupled with their occurrence on gentle slopes, would reduce the leaching regime of the Wooded Calcareous soils and at the same time transport gypsum to a zone from which aspen would be able to take up soluble Ca.
SUMMARY
The absence ofB horizon development under forest vegeta-tion is common in some forested soils in the Aspen Parkland, which have not been subjected to eluvial develop-ment. These soils maintain high levels of organic matler and a high base status despite their occurrence under forest veg-etation. The calcareous nature of these soils is the result of base cycling by aspen combined with favorable hydrologic conditions for the precipitation of secondary carbonate. Particle size of carbonates, X-ray diffraction and isotopic analysis has revealed the pedogenic nature of the carbonate found within the near-surface horizons of Wooded Calcareous
(Rego Black Chemozem) soils under forest vegetation. The precipitation of this secondary carbonate appears to corre-spond to the recarbonation of a once carbonate-free B horizon in an Orthic Black soil.
This study demonstrates the need to consider individual soils as part of a larger and dynamic soil-landscape system. Soil profile development is a function of a variety of inter-acting processes, and as a result the soil profile itself is an historical record of these processes acting over time, both past and present. The soil profile is a wealth of information for the enviromnental scientist provided that this informa-tion is interpreted within the context of the landscape with-in which the soil occurs.
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