The CaCO3
-CO2
-H2
O system in soils

Robbins, CW

doi:10.2134/jae1985.0003

Cited by 18 publications

(3 citation statements)

References 16 publications

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“…The quantitative relationship of the above three components can be described with the following equations [ Robbins , ]:

([], H_{2} {C O}_{3}^{*}) = \frac{([], {normalH normalC normalO}_{3}^{-}) \times H^{+} true]}{K 1}

K 1 = 10^{(- 14.8435 + \frac{3404.71}{T} + 0.032786 \times T)}

where C HCO3 is the bicarbonate concentration in water ( M ); C H is the concentration of protons ( M ); K 1 is the equilibrium coefficient for H 2 CO 3 * dissociation ( M ); and T is temperature (K).…”

Section: Methodsmentioning

confidence: 99%

Anthropogenic and climatic influences on carbon fluxes from eastern North America to the Atlantic Ocean: A process‐based modeling study

et al. 2015

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The magnitude, spatiotemporal patterns, and controls of carbon flux from land to the ocean remain uncertain. Here we applied a process-based land model with explicit representation of carbon processes in streams and rivers to examine how changes in climate, land conversion, management practices, atmospheric CO 2 , and nitrogen deposition affected carbon fluxes from eastern North America to the Atlantic Ocean, specifically the Gulf of Maine (GOM), Middle Atlantic Bight (MAB), and South Atlantic Bight (SAB). Our simulation results indicate that the mean annual fluxes (±1 standard deviation) of dissolved organic carbon (DOC), particulate organic carbon (POC), and dissolved inorganic carbon (DIC) in the past three decades were 2.37 ± 0.60, 1.06 ± 0.20, and 3.57 ± 0.72 Tg C yr À1, respectively. Carbon export demonstrated substantial spatial and temporal variability. For the region as a whole, the model simulates a significant decrease in riverine DIC fluxes from 1901 to 2008, whereas there were no significant trends in DOC or POC fluxes. In the SAB, however, there were significant declines in the fluxes of all three forms of carbon, and in the MAB subregion, DIC and POC fluxes declined significantly. The only significant trend in the GOM subregion was an increase in DIC flux. Climate variability was the primary cause of interannual variability in carbon export. Land conversion from cropland to forest was the primary factor contributing to decreases in all forms of C export, while nitrogen deposition and fertilizer use, as well as atmospheric CO 2 increases, tended to increase DOC, POC, and DIC fluxes.

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“…The quantitative relationship of the above three components can be described with the following equations [ Robbins , ]:

([], H_{2} {C O}_{3}^{*}) = \frac{([], {normalH normalC normalO}_{3}^{-}) \times H^{+} true]}{K 1}

K 1 = 10^{(- 14.8435 + \frac{3404.71}{T} + 0.032786 \times T)}

Section: Methodsmentioning

confidence: 99%

Anthropogenic and climatic influences on carbon fluxes from eastern North America to the Atlantic Ocean: A process‐based modeling study

et al. 2015

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“…Rhizoliths form only in semi-wet shallow desert soils, when Ca 2+ and HCO become supersaturated around deceased roots of Artemisia. This corresponds to a dewatering (evaporative) phase (Breecker et al, 2009), concomitant with a decrease of pCO 2 (Robbins, 1985;Salomons & Mook, 1976). During this transition phase from wet to dry conditions, as Ca 2+ cations are generally sufficiently abundant in the dune soils, they form carbonate minerals with HCO 3 -, which is confirmed by the carbonate content of the soils.…”

Section: Carbonate Epidiagenesis In Semi-closed Desert Soil 25 / 51mentioning

confidence: 81%

Characterization and formation of the pristine rhizoliths around Artemisia roots in dune soils of Tengeri Desert, NW China

Sun

Zamanian

Huguet

et al. 2020

CATENA

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Rhizoliths are the products of mineralization, petrification, or fossilization around and/or within plant roots. Among them, carbonate rhizoliths are the most common.Pristine carbonate rhizoliths with co-existing plant root relicts in the Tengeri Desert, NW China were studied, with a combination of intensive field observations and laboratory methods such as microscopy, scanning electronic microscopy, energy dispersive X-ray spectra, radiocarbon dating, and isotope mass spectrometer. The field observations revealed that the pristine rhizoliths are only present at the sites where Artemisia sphaerocephala Krasch are growing i.e. in swales among sand dunes. Soil moisture of the swales is the main controlling factor of rhizoliths *Revision, Unmarked Click here to download Revision, Unmarked: Catena10368 Pristine Rhizoliths Revision unmarked 2020 03 25.1 V2.doc 3 / 51

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“…Acid wheys and sweet wheys that contain less than 1000 mg Na kg-1 (SAR less than 10) are ideal for reclaiming sodic and saline-sodic soils. These wheys are mild acids that will lower the soil pH by neutralizing soil solution carbonates and bicarbonates and consequently increase the solubility of calcium carbonates (lime) which, in turn, decreases the soil SAR and ESP (Robbins 1985). Whey contains about 5% readily decomposable organic matter (measured as chemical oxygen demand of COD), and its decomposition contributes to the lowering of soil pH by generating additional organic acids and mineralization of nitrogen to nitrate.…”

Section: Whey As An Amendment For Sod1c and Saline-sodic Soilsmentioning

confidence: 99%

Cheese Whey as a Soil Conditioner

Robbins¹,

Lehrsch²

2020

Handbook of Soil Conditioners

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Whey is the liquid by-product of cheese and cottage cheese manufacture from milk. Each kg of cheese produced results in the production of about 9 kg of whey. In 1993, the U.S. cheese and cottage cheese industry produced approximately 23 x 106 m3 (6 x 109 gal) of whey (National Agricultural Statistics Service, 1994). Most of this is used directly as livestock feed or concentrated or dehydrated and used in human food and animal feed manufacture. Depending on the locality and economic factors, 20 to 100% of the whey produced is applied for beneficial effects on soils, or is land applied as a disposal procedure. Fresh whey composition varies depending on the cheese manufacture process used (Table 1). Most cheeses are made by biological culture processes that coagulate the milk proteins, and the resulting whey is often called "sweet" whey. Some cottage and creamed cheeses are made by coagulating the milk proteins using an equivalent of 3 g H3PO4 per kg of milk, and the resulting whey is often called "acid" whey. Sodium chloride is also added in some cheese-making processes. Even without salt or acid additions, whey is very salty due to the salts that come from the milk. Ryder (1980) discusses eleven useful whey byproduct separation methods that separate usable carbohydrates or proteins from the liquid phase. Most of these processes still produce large volumes of liquid waste with essentially the same mineral composition as fresh whey. As a consequence of differences in methods, whey and these other wastes vary in composition somewhat from one 167 Water Total solids CODs pH Electrical conductivity 92% 92% 8% 8%

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The CaCO₃ -CO₂ -H₂ O system in soils

Cited by 18 publications

References 16 publications

Anthropogenic and climatic influences on carbon fluxes from eastern North America to the Atlantic Ocean: A process‐based modeling study

Anthropogenic and climatic influences on carbon fluxes from eastern North America to the Atlantic Ocean: A process‐based modeling study

Characterization and formation of the pristine rhizoliths around Artemisia roots in dune soils of Tengeri Desert, NW China

Cheese Whey as a Soil Conditioner

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The CaCO3 -CO2 -H2 O system in soils

Cited by 18 publications

References 16 publications

Anthropogenic and climatic influences on carbon fluxes from eastern North America to the Atlantic Ocean: A process‐based modeling study

Anthropogenic and climatic influences on carbon fluxes from eastern North America to the Atlantic Ocean: A process‐based modeling study

Characterization and formation of the pristine rhizoliths around Artemisia roots in dune soils of Tengeri Desert, NW China

Cheese Whey as a Soil Conditioner

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Product

Resources

About

The CaCO₃ -CO₂ -H₂ O system in soils