Shewanella putrefaciens CN32 reduces Fe(III) within two illites which have different properties: the Fithian bulk fraction and the <0.2 µm fraction of Muloorina. The Fithian illite contained 4.6% (w/w) total Fe, 81% of which was Fe(III). It was dominated by illite with some jarosite (∼32% of the total Fe(III)) and goethite (11% of the total Fe(III)). The Muloorina illite was pure and contained 9.2% Fe, 93% of which was Fe(III). Illite suspensions were buffered at pH 7 and were inoculated with CN32 cells with lactate as the electron donor. Select treatments included anthraquinone-2,6-disulfonate (AQDS) as an electron shuttle. Bioproduction of Fe(II) was determined by ferrozine analysis. The unreduced and bioreduced solids were characterized by Mössbauer spectroscopy, X-ray diffraction and transmission electron microscopy. The extent of Fe(III) reduction in the bulk Fithian illite was enhanced by the presence of AQDS (73%) with complete reduction of jarosite and goethite and partial reduction of illite. Mössbauer spectroscopy and chemical extraction determined that 21–25% of illite-associated Fe(III) was bioreduced. The extent of bioreduction was less in the absence of AQDS (63%) and only jarosite was completely reduced with partial reduction of goethite and illite. The XRD and TEM data revealed no significant illite dissolution or biogenic minerals, suggesting that illite was reduced in the solid state and biogenic Fe(II) from jarosite and goethite was either released to aqueous solution or adsorbed onto residual solid surfaces. In contrast, only 1% of the structural Fe(III) in Muloorina illite was bioreduced. The difference in the extent and rate of bioreduction between the two illites was probably due to the difference in layer charge and the total structural Fe content between the Fithian illite (0.56 per formula) and Muloorina illite (0.87). There may be other factors contributing to the observed differences, such as expandability, surface area and the arrangements of Fe in the octahedral sheets. The results of this study have important implications for predicting microbe-induced physical and chemical changes of clay minerals in soils and sediments.

Illite from Muloorina, just south of Lake Eyre in South Australia, is commonly used as a standard ferric iron-bearing illite which has a cation exchange capacity (CEC) of ~22 meq/100 g, too high a value for this clay to conform to the most recent conclusions about illite composition. The objective of the present study was to reassess the Muloorina illite to determine the reason for this high CEC value. The composition determined by X-ray fluorescence analysis calculated to a cation charge of +22 is K0.68(Mg0.39Al1.02Fe0.543+Fe0.042+)[Si3.59Al0.38Fe0.033+]O10(OH)2. X-ray diffraction of glycolated and heated K-saturated Muloorina illite revealed no evidence of expandable layers. The cell dimensions are a = 5.314(1)Å, b = 9.040(1)Å, c = 10.135(3)Å, and b = 100.97(3)° (3σ in parentheses). Transmission electron microscopy revealed that Muloorina illite has a remarkably fine and uniform particle size in the form of irregularly stepped hexagonal crystals, averaging 60 nm in diameter at their widest, and 35 nm thick, each step being ~7 nm high. At most steps and between many steps defects occur where a 2:1 layer terminates, with a wide interlayer spacing beyond, commonly reaching to the crystal edge. Even though uninterrupted stacking of >10 or so 2:1 layers across one crystal is uncommon, the irregular distribution of the dislocations leaves appreciable structural continuity so that the mean diffracting thickness is of the order of 16 nm. Muloorina illite is not an interstratified illite-smectite, but a mica mineral with low-charge regions associated with terminating 2:1 layer defects. Such regions are wedge shaped at the nm scale and stabilized by the bonding of the illitic remainder of that interlayer. Approximately 17% of the total volume of each Muloorina illite crystallite is occupied by such low-charge 2:1 layers.