Adequate nutrition is necessary for overall health and development(1). Prisoners in general lack autonomy over their diet, in addition to being a population with a high risk of poor health outcomes(2, 3). It is important therefore that prisons are offered menus which meet dietary reference values (DRVs), as set by the UK government, aiming for equity with the general population, and that prisoners choose food options that are beneficial for their health. The aim of this study was to conduct a nutritional analysis of prisoners’ food diaries to determine whether dietary recommendations were being met.

Seven-day food diaries were collected from prisoners eating the normal food supplied by three young offender institutions in 2009. Food eaten was analysed using DietPlan6 version 6.0 (Forestfield Software Ltd). Individual nutrient data were tested for normality and compared against the UK DRVs and NDNS data from 2008/9 using either the one-sample T-test, or one-sample Wilcoxon Signed Rank Test. Data in the results is presented as (Mean ± SD).

There were n=466 diaries analysed, from male participants aged between 16 to 24 years. Twenty- eight nutrients were compared with their respective DRVs by age categories: 16-18y (n=156), 19-24y (n=310), and 16-24y (n=466).

For ages 16-24y, chloride (5556 ± 1692mg), folate (302 ± 112ug), iodine (195 ± 81ug), monounsaturated fat (35 ± 10g), potassium (3667 ± 1161mg), sodium (3899 ± 1392mg), sugar (136 ± 73g), riboflavin (2 ± 1mg), vitamin B12 (6 ± 4ug), vitamin C (92 ± 63mg), and zinc (11 ± 3mg) exceeded DRV requirements (P<0.01). Carbohydrates (53 ± 5%E), saturated fat (12 ± 5%E), and sugar (19 ± 9%E) all exceeded their DRVs (P<0.05). Vitamin A (553 ± 531ug) and fibre (15 ± 6g) were found 24% and 18% lower than the DRVs, respectively (P<0.01). Fat (34 ± 5%E), polyunsaturated fat (6 ± 1%E), and protein (14 ± 2%E), as a percent of energy, were below the DRV by 3%, 8%, and 7% respectively (P<0.01). Magnesium (301 ± 107mg) was equal to the DRV (P=0.81).

For 16-18, and 19-24 respectively, calcium (1286 ± 928mg; 1337 ± 489mg), copper (1 ± 0.6mg; 2 ± 0.6mg), iron (14 ± 5mg; 15 ± 6mg), niacin (19 ± 7mg; 21 ± 7mg), phosphorus (1545 ± 381mg; 1620 ± 493mg), protein (96 ± 24g; 100 ± 29g), thiamine (2 ± 0.6mg; 2 ± 0.7mg), and vitamin B6 (2.3 ± 0.7ug; 3 ± 0.9ug) exceeded their DRV (P<0.01). For 16-18y, energy (kcals) was equal to the DRV (2748 ± 787kcal, P=0.91). For years 19-24y, energy (kcal) exceeded the DRV (2931 ± 939kcal, P<0.01).

This study represents the largest assessment of dietary intake of prisoners and demonstrates that the prison catering, for the most part, met the DRVs. However, sugar, fat, and energy intake exceeded their DRV target, posing clear risks to health by possibly contributing to later obesity, hypertension, Type 2 diabetes and heart disease.

Effects of acute thermal exposures on appetite appear hypothetical in reason of very heterogeneous methodologies. The aim of this study was therefore to clearly define the effects of passive 24-h cold (16°C) and heat (32°C) exposures on appetitive responses compared with a thermoneutral condition (24°C). Twenty-three healthy, young and active male participants realised three sessions (from 13.00) in a laboratory conceived like an apartment dressed with the same outfit (Clo = 1). Three meals composed of three or four cold or warm dishes were served ad libitum to assess energy intake (EI). Leeds Food Preference Questionnaires were used before each meal to assess food reward. Subjective appetite was regularly assessed, and levels of appetitive hormones (acylated ghrelin, glucagon-like peptite-1, leptin and peptide YY) were assessed before and after the last meal (lunch). Contrary to the literature, total EI was not modified by cold or heat exposure (P = 0·120). Accordingly, hunger scores (P = 0·554) were not altered. Levels of acylated ghrelin and leptin were marginally higher during the 16 (P = 0·032) and 32°C (P < 0·023) sessions, respectively. Interestingly, implicit wanting for cold and low-fat foods at 32°C and for warm and high-fat foods at 16°C were increased during the whole exposure (P < 0·024). Moreover, cold entrées were more consumed at 32°C (P < 0·062) and warm main dishes more consumed at 16°C (P < 0·025). Thus, passive cold and hot exposures had limited effects on appetite, and it seems that offering some choice based on food temperature may help individuals to express their specific food preferences and maintain EI.

The mineralogy of the clay fraction was studied for soils and saprolite on two Blue Ridge Front mountain slopes. The clay fraction contained the weathering products of primary minerals in the mica gneiss and schist parent rocks. Gibbsite is most abundant in the saprolite and residual soil horizons, where only chemical weathering has been operable. In colluvial soil horizons, where both physical and chemical weathering have occurred, the clay fraction consists largely of comminuted primary phyllosilicates —muscovite, chlorite, and possibly biotite—and their weathering products: vermiculite, interstratified biotite/vermiculite (B/V), and kaolinite. The clay-size chlorite contains Fe2+ as indicated by Mössbauer spectroscopy, and is more resistant to weathering than biotite. The vermiculite and B/V, both weathering products of biotite, contain Fe3+. Vermiculite in colluvial soils and, especially, surface horizons is weakly hydroxy-interlayered. The kaolinite in the clay fraction resulted at least partly from the comminution of kaolinized biotite in coarser fractions.

The hematite content ranged from 0 to 8% of the clay fraction and strongly correlates (r =.95) with dry clay redness, as measured by the redness rating: RR = (10 - YR hue) × (chroma) ÷ (value). The hematite is largely a product of the weathering of almandine; thus, the soil redness is dependent on the amount of almandine in the parent materials and its degree of weathering in the soils. Goethite (13–22% of the clay fraction) imparts a yellow-brown hue to soils derived from almandine-free parent rocks. The release of Fe in relatively low concentrations during the weathering of Fe-bearing primary minerals, particularly biotite, appears to have promoted the formation of goethite.

A green, Lithic Torriorthent soil derived from a celadonite-rich, hydrothermally altered basalt immediately north of the Mojave Desert region in southern California was studied to investigate the fate of the celadonite in a pedogenic weathering environment. Celadonite was found to be disseminated in the highly altered rock matrix with cristobalite, chalcedony, and stilbite. X-ray powder diffraction (XRD) showed the soil material to contain celadonite having a d(060) value of 1.510 Å, indicative of its dioctahedral nature. Very little smectite was detected in the parent material, whereas Fe-rich smectite was found to be abundant in the soil. The Fe-smectite and celadonite were identified as the sole components of the green-colored clay fraction (<2 µm) of all soil horizons. The soil clay showed a single d(060) value of 1.507 Å, indicating that the smectite was also dioctahedral and that its b-dimension was the same as that of the celadonite. Mössbauer spectroscopy showed that the chemical environments of Fe in the rock-matrix celadonite and in the smectite-rich soil clay were also nearly identical. These data strongly suggest a simple transformation of the celadonite to an Fe-rich smectite during soil formation.

Supporting evidence for this transformation was obtained by artificial weathering of celadonite, using sodium tetraphenyl boron to extract interlayer K. The intensity of the 001 XRD peak (at 10.1 Å) of celadonite was greatly reduced after the treatment and a peak at 14.4 Å, absent in the pattern of the untreated material, appeared. On glycolation of the sample, this peak expanded to 17.4 Å, similar to the behavior of the soil smectite. The alteration of celadonite to smectite is a simple transformation requiring only the loss of interlayer K. The transformation is apparently possible under present-day conditions, inasmuch as the erosional landscape position, shallow depth, and lack of significant horizonation indicate that the soil is very young.

The acid-catalyzed reaction between methanol and isobutene to give methyl-t-butyl ether may be carried out using a cation-exchanged smectite as the catalyst. In 1,4-dioxan solvent at 60°C smectites exchanged with Al3+, Fe3+, or Cr3+ give yields of ∼60% after 4 hr, whereas smectites exchanged with Cu2+, Pb2+, Ni2+, Co2+, Ca2+, and Na+ give less than ∼8% yield. The reaction is efficient only when certain solvents are used, e.g., with Al3+-smectite the yield is ∼5% when using 1,2-dimethoxyethane, diethyleneglycol diethylether, n-pentane, tetrahydropyran, N-methylmorpholine, or tetrahydrofuran solvents compared with ∼60% using 1,4-dioxan solvent (4 hr). Moreover, the effective solvents depend somewhat on the clay interlayer cation. The use of tetrahydrofuran and tetrahydropyran gives ∼35% yields at 60°C (4 hr) with Fe3+- or Cr3+-smectites but ∼4% yield with Al3+-smectite.

The reaction of 2-methyl pent-2-ene with primary alcohols (C1-C18) at 95°C over an Al-montmorillonite gave yields of 20–90% of ethers of the type R-O-C(CH3)2C3H7. Lower yields were produced if secondary alcohols were employed, and tertiary alcohols gave only a trace of this ether. When a variety of alkenes was reacted with butan-1-ol at 95°C over a similar catalyst, no reaction occurred unless the alkene was capable of forming a tertiary carbonium ion immediately upon protonation. In this case the product was the tertiary ether t-R-O-nC4H9. However, at a reaction temperature of 150°C a variety of products were formed including (1) ether by the attack of butanol on the carbonium ions produced either directly from protonation of the alkenes or by hydride shift from such an ion, (2) alkenes by the attack of n-C4H9+ ions (derived from protonation and dehydration of butanol) on the alkene, (3) di-(but-1-yl) ether by dehydration of the butanol, and (4) small amounts of alcohol by hydration of the alkene. The differences in reactivity below and above 100°C are related directly to the amount of water present in the interlayer space of the clay and the degree of acidity found there. Although the clay behaves as an acid catalyst, the reactions are far cleaner (more selective) than comparable reactions catalyzed by sulfuric acid.

The weathering products of primary biotite, chlorite, magnetite, and almandine in mica gneiss and schist in the North Carolina Blue Ridge Front were determined. Sand-size grains of biotite, the most abundant, readily weathered mineral in the parent rock, have altered to interstratified biotite/vermiculite, vermiculite, kaolinite, and gibbsite in the saprolite and soil. Fe2+-chlorite in the parent rock was relatively resistant to chemical weathering, which appears to be confined to the external surfaces of particles. Magnetite grains in the saprolite are essentially unaltered, but those in the soil contain abundant crystallographically controlled etch pits and are coated with oxidation crusts. Almandine altered to goethite, hematite, and gibbsite as the rock weathered to saprolite. Extensively weathered almandine grains were found to contain etch pits and what appeared to be oxide coatings. Apparently, a rapid release of Fe during weathering produced hematite, whereas slower release of Fe favored the formation of goethite.