Activity and Concentration• Activity – “effective concentration”• Ion-ion and ion-H2O interactions (hydration shell)cause number of ions available to react chemically("free" ions) to be less than the number present• Concentration can be related to activity using theactivity coefficient γ, where [a] = γ (c)Until now we have assumed that activity, a, is equal toconcentration, c, by setting γ = 1 when dealing withdilute aqueous solutions…But ions don’t behave ideally . . .• Concentration related to activity using the activitycoefficient γ, where [a] = γ (c)• The value of γ depends on:– Concentration of ions and charge in the solution– Charge of the ion– Diameter of the ion• Ionic strength, I = concentration of ions and charge insolutionI = 1/2 Σmizi2– where mi = concentration of each ion in moles per L,zi = charge of ion• Activity coefficient γz → 1 as concentrations → 0 and tendto be <1 except for brinesCalculation of Ionic StrengthI = 1/2 Σmizi2I = 0.5[(HCO3–)·12 + (SO42–)·22 + (Cl–)·12 + (NO3–)·12 + (Ca2+)·22 +(Mg2+)·22 + (Na+)·12 + (K-)· 12 + (Fe2+)·22 + (SiO2)·02]Substituting values for Lake SuperiorI = 0.5(0.00082·12 + 0.00005·22 + 0.00004·12 + 0.000008·12 + 0.00035·22 + 0.00015·22 + 0.00013·12 + 0.00001·12 + 0.000006·22 + 0.00007·02) I = 0.0016 — How does this value compare with other natural waters?Water Typical Ionic StrengthRivers and lakesPotablegroundwaterSeawaterOil field brinesOil0.001 - 0.0050.001 - 0.020.7>5Sources for ions in natural waters?Na+SO42-(from Garrels and Christ, 1965)IγiSeawaterRivers, lakes,groundwaterBrinesCa2+Solution Models• Debye-Hückel EquationPhysical model based onelectrostatic interactions• At higher ionic strength, useextended Debye-Hückelequation• Davies Equationfor higher ionic strengths(<0.5)logγi= −Azi2(I)1/ 2logγi=−Azi2(I)1/ 21+ Bao(I)1/ 2logγi=−Azi2(I)1/ 21+ (I)1/ 2+ 0.3Iwhere I is the ionic strength of the solution as defined above; z is the charge of the ion whose activity coefficient is being calculated; A and B are constants whose values depend on the dielectric constant of the solvent and the temperature; and a is the effective diameter of the ion in the solution in Å.Fig. 2-2. Variation of the activity cofficient for Ca2+ according to the threeforms of the Debye-Hückel equation (Drever, 1997)Debye-HückelExtendedDebye-HückelDaviesDebye-HückelExtended Debye-HückelDaviesI < 5 x 10-3I < 0.1 x 10-3I ≤ 0.5Diagenesis and the growth of concretionsDiagenesis includes all of the chemical, physical, and biologicalprocesses that take place in sediment after it was deposited:Chemical processes: dissolution of minerals in pore water,precipitation of insoluble compounds, and ion exchangereactions between aqueous species and the surfaces of solidsBiological processes: bioturbation, bacteria-driven chemical reactions (reduction of sulfate), biogenic compoundsmay inhibit dissolution of minerals by coating grain surfaces or enhance dissolution by adsorbing ionsPhysical processes: deposition, compaction, flow of pore water…The growth of concretions during diagenesisGrowth of a concretion with a radius ofrc by diagenetic redistribution causedby dissolution of a mineral in the sediment, diffusion of the resulting ionsto the surface of the concretion, andprecipitation of a new mineral in thepore spaces of the sediment. The process is transport-dominated and causes the formation of a depleted zone with a radius rd and a width L. Δc (=cd-cp) is the molar concentration of the material that is dissolving (cd) and precipitating (cp), and F is the flux of ions to the surface of the concretion and leaving the outersurface of the depleted zone.From Faure chapter 15 — “Rates of Geochemical Processes”Minerals may precipitate from pore water of sediment within pore spaces as a cement or replace pre-existing minerals that dissolve, both of which may cause the formation of concretionsCalcite concretionCalcite concretion(coated with hematite)Sandstone concretionSandstone concretionWhat you are given: rc, radius of the concretion = 8.0 cmD, the diffusion coefficient = 5.4 x 10-6 cm2/secφ, porosity = 0.75fd, volume fraction of aragonite in the sediment = 0.15Δc, difference in equilibrium concentration of Ca2+ in pore wateron the surfaces of calcite and aragonite = 2.0 x 10-5 mol/kgVp, volume of calcite = 36.934 cm3/molSo what about rates?Calculate the time required for a calcite concretion to grow by dissolution of disseminated aragonite and diffusion of the resulting Ca2+ ions at 10°C?t = rc22VpDΔc(φfd- 1)rc, radius of the concretion = 8.0 cmD, the diffusion coefficient = 5.4 x 10-6 cm2/sec (T dependent)φ, porosity = 0.75fd, volume fraction of aragonite in the sediment = 0.15Δc, difference in equilibrium concentration of Ca2+ in pore wateron the surfaces of calcite and aragonite = 2.0 x 10-5 mol/kgVp, volume of calcite = 36.934 cm3/molSo what about rates?Calculate the time required for a calcite concretion to grow by dissolution of disseminated aragonite and diffusion of the resulting Ca2+ ions at 10°C?t = (8 cm)22(36.934 )(5.4x10-6 )(2x10-5 )(0.750.15- 1)cm3molcm2secmolkgt = 8.022x109sec•1000 ÷ 3.154x107 sec/year = 254,386