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Beltman, B.; Rouwenhorst, T. Gerrit; Kerkhoven, Marianne B. Van; Krift, Theo van der; Verhoeven, Jos T. A.

doi:10.1023/a:1006374018558

Cited by 57 publications

(19 citation statements)

References 26 publications

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“…For instance, through increased availability of N as a result of hydrological alteration (drainage), which increases peat decomposition rates (Holden, Chapman, & Labadz, 2004), but also of input from airborne N deposition (Bobbink, Hornung, & Roelofs, 1998). Whereas P levels may rise in fens that receive polluted groundwater or surface run-off (Beltman, Rouwenhorst, Van Kerkhoven, Van der Krift, & Verhoeven, 2000), or as a result of restoration activities, e.g., from rewetting of highly decomposed peat on formerly drained fens (Emsens, Aggenbach, Smolders, Zak, & van Diggelen, 2017;Zak, Wagner, Payer, Augustin, & Gelbrecht, 2010). Increased levels of both abovementioned nutrients are regarded as one of the major threats to biodiversity (Sala et al, 2000;Smith, Tilman, & Nekola, 1999).…”

Section: Introductionmentioning

confidence: 99%

Long‐term effects of nutrient enrichment controlling plant species and functional composition in a boreal rich fen

Øien

Pedersen

Kozub

et al. 2018

J Vegetation Science

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Questions How does long‐term increase in nutrient availability affect species composition, species diversity and functional composition in boreal rich fens, and how does this differ from short‐term effects? What are the possible mechanisms behind the observed changes, and how does nutrient limitation influence species diversity in these communities? Location Sølendet Nature Reserve, central Norway. Methods A full‐factorial field experiment. Plots in two localities received one of following treatments (n = 3): no nutrient addition (control), N, P, K, NP, NK, PK and NPK addition. Cover of plant species was recorded before treatment, and after two and 15 years of treatment. Results Two years of nutrient addition caused small changes in species composition, but addition of NP led to large increase in abundance of species with high ability to exploit the added nutrients—a direct result of the elimination of nutrient limitation in the communities. After 15 years of nutrient addition there were significant changes following three different pathways, one for each of N, P and NP addition. The addition of NP led to large community shifts, considerable species turnover and reduced species and functional richness, mainly caused by increase in cover of highly competitive and tussock‐forming grasses like Deschampsia cespitosa, Festuca ovina and Molinia caerulea, out‐competing other species, especially bryophytes. Addition of N led to smaller changes in species turnover, and without clear dominant species. Addition of P led to considerable species turnover, but no reduction in species or functional richness, and the bryophyte diversity increased. This is explained by the bryophytes’ association with N‐fixing cyanobacteria, suggesting less N limitation and a greater ability to utilize the added P when vascular plants suffer from N shortage. In addition, bryophytes are more sensitive to low P availability, due to larger P requirements compared to vascular plants. There was no effect of K addition. Conclusions Both N and P limitation is essential for the maintenance of high species diversity in boreal rich fens, and P limitation controls bryophyte diversity. From a management perspective, N and P limitation is vital in the conservation of boreal rich fens or when a functional fen system is reestablished through restoration measures.

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Section: Introductionmentioning

confidence: 99%

Long‐term effects of nutrient enrichment controlling plant species and functional composition in a boreal rich fen

Øien

Pedersen

Kozub

et al. 2018

J Vegetation Science

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“…These minerals, however, have a higher solubility than carbonate minerals and can penetrate deeper into the soil (Reeve and Sumner 1972). Moreover, the sulfate may induce unwanted internal eutrophication in anoxic peat layers (Koerselman et al 1993;Beltman et al 2000). Hence, the effects of such minerals are not straightforward as they may vary with soil chemical, physical and biological conditions (Haynes and Naidu 1998;Hamilton et al 2007;Paradelo et al 2015;Holland et al 2018) and can change over time after application (Neale et al 1997;Grover et al 2017).…”

Section: Introductionmentioning

confidence: 99%

Effects of Ca:Mg ratio and pH on soil chemical, physical and microbiological properties and grass N yield in drained peat soil

Deru

Hoekstra

Agtmaal

et al. 2021

New Zealand Journal of Agricultural Research

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In three dairy grasslands on peat, minerals were added to manipulate the soil Ca:Mg ratio with or without effect on pH. The responses of soil properties and grass N yield were measured. CaCO 3 application led to higher soil Ca:Mg ratio and pH KCl compared to the untreated control, decreased N total and C total , and increased P availability. Grass N yield increased in the first year by only 6% of the reduction in soil N total , but not in the second year. A higher pH increased SOM decomposition, especially in soils with high P availability. MgCO 3 reduced the Ca: Mg ratio, had little influence on soil parameters and no effect on grass N yield. In contrast, CaSO 4 and MgSO 4 did not influence pH KCl but reduced grass N yield in most cases. Results suggest stabilisation of organic matter by Ca binding in treatments with added Ca. We conclude that grass N yield was not linked with changes in Ca:Mg ratio but with soil pH. The pH effects on SOM decomposition depended on P availability and Ca binding. Hence, to avoid potentially large soil losses of C and N, the current agricultural advice on pH management in peat grasslands should be better adapted to local edaphic characteristics.

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“…To date, there are several issues regarding the metal sources [3,6,7], the conditions of mineral formation [8,14,[17][18][19], and the subsequent evolution of minerals [10] in peat deposits. Metal enrichment of peat is interpreted by one of the following processes or their combination: interaction with underlying rocks and diffusion from groundwater [4,6,7,10,13], precipitation of atmospheric dust caused by natural or anthropogenic factors [9,15,[20][21][22][23], release from plants [4,7,24], and detrital input from surrounding rocks [4,6,10,12].…”

Section: Introductionmentioning

confidence: 99%

Authigenic and Detrital Minerals in Peat Environment of Vasyugan Swamp, Western Siberia

et al. 2018

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Studies of mineral-forming processes in modern peat bogs can shed light on metal concentrations and their cycling in similar environments, especially in geological paleoanalogs. In terms of the mineralogical and geochemical evolution of peat bog environments, the Vasyugan Swamp in Western Siberia is a unique scientific object. Twelve peat samples were collected from the Vasyugan Swamp up to the depth of 275 cm at 25 cm intervals. The studied peat deposit section is represented by oligotrophic (0–100 cm), mesotrophic (100–175 cm), and eutrophic (175–275 cm) peat, and this is underlain by basal sediments (from 275 cm). About 30 minerals were detected using scanning electron microscopy (SEM), X-ray diffraction (XRD), and Raman spectroscopy. The observed minerals are divided into detrital, clay, and authigenic phases. The detrital minerals found included quartz, feldspar, ilmenite, rutile, magnetite, zircon, and monazite. When passing from basal to oligotrophic bog sediments, the clay minerals changed from illite-smectite to kaolinite. Authigenic minerals are represented by carbonates (calcite and dolomite), iron (hydro-)oxides, galena, sphalerite, pyrite, chalcopyrite, Zn-Pb-S mineral, barite, baritocelestine, celestine, tetrahedrite, cassiterite, REE phosphate, etc. The regular distribution of mineral inclusions in peat is associated with the (bio)geochemical evolution of the environment. The formation of authigenic Zn, Pb and Sb sulfides is mainly confined to anaerobic conditions that exist in the eutrophic peat and basal sediments. The maximum amount of pyrite is associated with the interval of 225–250 cm, which is the zone of transition from basal sediments to eutrophic peat. The formation of carbonate minerals and the decreasing concentration of clay in the association with local sulfide formation (galena, sphalerite, chalcopyrite, stibnite) begins above this interval. The peak of specific carbonation appears in the 125–150 cm interval of the mesotrophic peat, which is characterized by pH 4.9–4.5 of pore water. Kaolinite is the dominant clay mineral in the oligotrophic peat. Gypsum, galena, chalcopyrite, sphalerite, and relicts of carbonate are noted in association with kaolinite. Changes in oxygen concentrations are reflected in newly formed mineral associations in corresponding intervals of the peat. This can be explained by the activity of microbiological processes such as the anaerobic oxidation of methane (AOM) and bacterial sulfate reduction (BSR), expressed in specific carbonatization (100–225 cm) and sulfidization (175–250 cm), respectively.

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Cited by 57 publications

References 26 publications

Long‐term effects of nutrient enrichment controlling plant species and functional composition in a boreal rich fen

Long‐term effects of nutrient enrichment controlling plant species and functional composition in a boreal rich fen

Effects of Ca:Mg ratio and pH on soil chemical, physical and microbiological properties and grass N yield in drained peat soil

Authigenic and Detrital Minerals in Peat Environment of Vasyugan Swamp, Western Siberia

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