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Saline seepage in western North Dakota occurs when water in excess of crop use leaches soluble salts from the root zone and transports them laterally to lower landscape positions. Evapotranspiration moves these dissolved salts upward through the soil, resulting in salt crust formation at the surface. This study was undertaken to detail the mineralogic changes occurring as saline waters migrate through the soil profile, and to determine the mineralogic composition of the saline efflorescences present at the soil surface of four saline seeps in Hettinger County, North Dakota. Mineralogic changes resulting from upward water movement in soils were accurately predicted using the Hardie‐Eugster model of closed basin brine evolution. The sequence calcite‐gypsum‐ and mixed Na‐Mg‐(SO4) minerals occurs as saline waters migrate upward through the profile. The following minerals occur in surface efflorescences; mirabilite, thenardite, epsomite, hexahydrite, bloedite (Na2Mg(SO4)2·4H20), konyaite (Na2Mg(SO4)2·5H20), loewite Na12Mg7(SO4)13·15H2O), and gypsum. Hydration state, mineral occurrence, and mineral solubility were seasonally dependent.

The saturation‐paste extract (SPE) chemistry of samples collected in the wet‐meadow and shallow‐marsh zones of seven North Dakota wetlands was related to SPE electrical conductivity to investigate the development of hydric‐soil salinity. Study wetlands represent a local, depression‐focused groundwater‐flow system. Recharge wetlands recharge the groundwater whereas discharge wetlands receive the majority of their water as groundwater discharge. Throughflow wetlands receive water from as well as yield water to the system. Development of soil salinity generally followed the Hardie and Eugster model of closed‐basin brine evolution, which considers the composition of solutions undergoing evaporation to be the result of chemical changes imposed by the successive formation of evaporite minerals. Hydric soils of recharge wetlands were nonsaline and free of calcite (CaCO3) and gypsum (CaSO4·2H2O). The chemistry of these soils results from evapotranspiration, recharge hydrology, ionic mobility, and exchange relationships. Increases in SPE Mg2+, Na+, and SO2‐4 dominance in more saline throughflow and discharge wetlands are caused by calcite and gypsum precipitation, with the former controlling alkalinity and the latter Ca2+ concentrations. At high salinities produced by concentration through freezing, mirabilite (Na2SO4·10H2O) crystallizes and controls Na+ levels, resulting in hypersaline solutions enriched in Mg2+ and SO2‐4. Additional variation in the patterns of salinity development can be explained by dominance of recharge over discharge, mixing with fresh or chemically discrete water, and valence dilution effects.