Determination of Carbonate Concentrations in Calcareous Soils with Common Vinegar Test

Calcareous soils are those that have free calcium carbonate (CaCO3) and have pH values in the range of 7.0 to 8.3. If they are managed properly, calcareous soils can be used to grow any crop. Before employing any management practices, it is important to know how much carbonate exists in the soil. Soil carbonate is usually quantified by acid dissolution followed by the volumetric analysis of the released carbon dioxide (CO2). In geological sciences, a simple acid test consists of placing a drop of dilute hydrochloric acid on a rock or mineral and observing if there are CO2 bubbles released; the bubbles indicate the presence of carbonate minerals. The household test below uses vinegar and other simple instruments to estimate soil carbonate concentration. Minor revision with an added author.

Using Triple Oxygen Isotopes of Pedogenic Carbonate to Identify Ancient Evaporation: First Steps from Modern Soils

<p>The stable isotope composition of soil carbonates is commonly used to reconstruct continental paleoclimates, but its utility is limited by an incomplete understanding of how soil carbonates form. In particular, it is often unclear if the parent soil water has been enriched in <sup>18</sup>O due to evaporation, muddying our ability to infer meteoric water δ<sup>18</sup>O from paleosol carbonates. Here we demonstrate the potential use of triple oxygen isotopes (termed ∆’<sup>17</sup>O) to account for evaporation and identify formation process through a study of modern soil carbonate isotope values.  Evaporation results in a decreased slope in the relationship between δ<sup>17</sup>O and δ<sup>18</sup>O and deviations from the global meteoric water line, such that ∆<sup>’17</sup>O values in soil water and resulting carbonate decrease with increased evaporation. We report ∆<sup>’17</sup>O values of CO<sub>2</sub> derived from soil carbonates and measured as O<sub>2</sub> on a mass spectrometer, with 1-4 replicates per soil carbonate. We find a step-like relationship between ∆’<sup>17</sup>O in globally distributed Holocene soil carbonate samples and aridity, where aridity is defined using the aridity index (AI, mean annual precipitation/potential evapotranspiration). Low ∆<sup>’17</sup>O values occur in hyper-arid climates (AI < 0.05), with mean ∆<sup>’17</sup>O = -0.164 ‰, SD = 0.004 ‰. A transition, or step, occurs in arid climates (AI from 0.05 to 0.2), with ∆<sup>’17</sup>O values that range from -0.129 ‰ to -0.165 ‰, and mean ∆<sup>’17</sup>O of -0.148 ‰, SD = 0.010‰. High ∆<sup>’17</sup>O values occur in semi-arid through humid climates (AI >0.5) with mean ∆<sup>’17</sup>O of -0.135 ‰, SD = 0.008 ‰.  The lowest observed ∆<sup>’17</sup>O values are consistent with extensive evaporation – for context, the ∆<sup>’17</sup>O values are similar to those measured in lacustrine carbonates from closed lake basins. The highest ∆<sup>’17</sup>O values are consistent with little soil water evaporation. We interpret the step-like pattern in ∆’<sup>17</sup>O values as an indication of the threshold in the importance of evaporation vs. transpiration in soil dewatering. This data highlights the potential to use ∆<sup>’17</sup>O to identify the extent of evaporation in paleosol carbonates. Eventually, we hope that this novel technique will lead to quantitative accounting of evaporation in soil water and improved reconstructions of meteoric water δ<sup>18</sup>O from soil carbonates. The ability to constrain the evaporative conditions of soil carbonate formation will also aid interpretations of δ<sup>13</sup>C (including pCO<sub>2</sub> reconstructions) and clumped isotope-based temperatures. These efforts will ultimately aid in our ability to integrate paleoclimate data from soil carbonates with data from other terrestrial records.  </p>