Biogeochemical implications of the ubiquitous colonization of marine habitats and redox gradients by Marinobacter species.

The Marinobacter genus comprises widespread marine bacteria, found in localities as diverse as the deep ocean, coastal seawater and sediment, hydrothermal settings, oceanic basalt, sea-ice, sand, solar salterns, and oil fields. Terrestrial sources include saline soil and wine-barrel-decalcification wastewater. The genus was designated in 1992 for the Gram-negative, hydrocarbon-degrading bacterium Marinobacter hydrocarbonoclasticus. Since then, a further 31 type strains have been designated. Nonetheless, the metabolic range of many Marinobacter species remains largely unexplored. Most species have been classified as aerobic heterotrophs, and assessed for limited anaerobic pathways (fermentation or nitrate reduction), whereas studies of low-temperature hydrothermal sediments, basalt at oceanic spreading centers, and phytoplankton have identified species that possess a respiratory repertoire with significant biogeochemical implications. Notable physiological traits include nitrate-dependent Fe(II)-oxidation, arsenic and fumarate redox cycling, and Mn(II) oxidation. There is also evidence for Fe(III) reduction, and metal(loid) detoxification. Considering the ubiquity and metabolic capabilities of the genus, Marinobacter species may perform an important and underestimated role in the biogeochemical cycling of organics and metals in varied marine habitats, and spanning aerobic-to-anoxic redox gradients.

Introduction

Marine habitats are host to a diverse range of substrates and physicochemical regimes. Among these, hydrothermal features attract particular interest owing to ore-grade concentrations of metals, physicochemical extremes, and the presence of chemolithoautotrophic macrofauna and microbiota. Bacteria and Archaea occupying marine habitats have a substantial physical presence. There are an estimated 3.9 × 1030 prokaryotic cells in the open ocean and unconsolidated marine sediments, comprising ~3.1 × 1011 tonnes of carbon (Whitman et al., 1998). This is slightly more than the estimated carbon content of terrestrial prokaryotes, and just under half of that in all plant life. Prokaryotes can contribute significantly to marine ecosystem functioning and biogeochemical cycles (Jørgensen, 2006), owing to their prevalence and enormous capacity for transforming their environments through metabolism of organic and inorganic matter (Gadd, 2010). Yet much of the marine microbial biomass remains unexplored, and there is still much to learn about heterotrophic and autotrophic bacterial functioning in the ocean (e.g., Moran et al., 2004; Emerson et al., 2010; Holden et al., 2012).

Marinobacter is a heterotrophic, and in some instances mixotrophic (Dhillon et al., 2005; Handley et al., 2009a,b), metabolically flexible genus found in an exceptionally wide range of marine and saline terrestrial settings, including various low-temperature hydrothermal environments (Table 1). The genus comprises Gram-negative Gammaproteobacteria within the Alteromonadales order. All known species are motile with polar flagella (excluding M. goseongensis, Roh et al., 2008), slightly to moderately halophilic (cf. DasSarma and Arora, 2012), aerobic heterotrophs (Table 2). However, few are confirmed strict aerobes, and several are facultative anaerobes (Table 1). All are rod-shaped, with the exception of the ellipsoidal M. Segnicrescens (Guo et al., 2007), and most are neutrophilic, except the slightly alkaliphilic M. alkaliphilus, which grows optimally at pH 8.5–9.0 (Takai et al., 2005; also see Al-Awadhi et al., 2007; Table 2). Although most species are mesophilic, many are psychrotolerant (also known as psychrotrophic) and capable of growth down to ~4°C (Table 2; Moyer and Morita, 2007). A couple of other species are either psychrophilic (with a growth optimum near 15°C) or thermotolerant (with growth up to 50°C and an optimum of 45°C). This phenotypic versatility contributes to the ubiquity of this genus, and its ability to occupy diverse physicochemical regimes.

Table 1

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Marinobacter species	HC	CHb	NO−3	Gluc ferm	AA	Anaer	Env	Isolation source
hydrocarbonoclasticus1,a	Y	N	resp	N	Y	Y	–	Oil-polluted sediment; Gulf of Fos; Mediterranean coast; France
aquaeolei2	Y	N	resp	N	Y	Y	–	Oil-producing well-head; offshore platform; Vietnam
excellens3,a	–	Y	resp	Y	Y	Y	12°C	Radionuclide-polluted sediment; 0.5 m depth; Chazhma Bay; Sea of Japan; Russia
lipolyticus4,a	–	Y	N	–	N	st-aer	–	Saline soil; seaside city of Cádiz; Spain
squalenivorans5	Y	–	resp	N	Y	Y	–	Oil-contaminated coastal sediment; Carteau Cove; Gulf of Fos; France
lutaoensis6,a	–	Y	N	N	Y	st-aer	43°C	Coastal hot spring water; Lutao; Taiwan
litoralis7,a	–	–	Y	N	N	N	–	Sea water; Jungdongjin beach; East Sea; Korea
flavimaris8,a	–	Y	Y	–	N	Y	–	Sea water; Daepo Beach; Yellow Sea; Korea
daepoensis8,a	–	–	N	–	N	Y	–	Sea water; Daepo Beach; Yellow Sea; Korea
bryozoorum9,a	–	Y	Y	–	Y	Y	–	Sediment; Bearing Sea; Russia
sediminum9,a	–	Y	–	–	Y	–	–	Sediment; Peter the Great Bay; Sea of Japan; Russia
maritimus10,a	Y	Y	–	–	Y	–	–	Sea water; 110 km SW of subantarctic Kerguelen islands
alkaliphilus11	Y	Y	Y	–	Y	Y	1.7–1.9°C	Subseafloor alkaline serpentine mud; South Chamorro Seamount; Mariana Forearc
algicola12,a	Y	Y	resp	–	Y	Y	–	Dinoflagellate Gymnodinium catenatum; Yellow Sea; Korea
koreensis13,a	–	N	Y	N	Y	Y	–	Sea-shore sand at Homi Cape; Pohang; Korea
vinifirmus14,a	–	N	N	N	N	st-aer	–	Wine tank decalcification wastewater-evaporation pond. Location?
salsuginis15,a	Y	Y	resp	Y	Y	Y	–	Brine-seawater interface; Shaban Deep (a brine-filled deep); Red Sea
gudaonensis16,17,a	Y	Y	Y	–	Y	Y	–	Oil-polluted soil underlying wastewater from the coastal Shengli Oil field; China
segnicrescens17,a	N	Y	Y	–	N	Y	–	Benthic sediment; 1161 m depth; South China Sea
salicampi18,a	–	N	Y	–	–	Y	–	Sediment; marine solar saltern; Yellow Sea; Korea
pelagius19,a	–	N	Y	–	Y	–	–	Coastal seawater; Zhoushan Archipelago; China
guineae20,a	–	Y	resp	N	–	Y	–	Marine sediment; Deception Island; Antarctica
psychrophilus21,a	–	Y	Y	–	Y	–	Freezing	Sea-ice; Canadian Basin; Arctic Ocean
mobilis; zhejiangensis22,a	–	N	Y	–	Y	–	–	Sediment; Dayu Bay; East China Sea (Lat. 27.33, Long. 120.57)
goseongensis23,a	–	N	–	–	N	–	–	Coastal seawater; 100 m depth; East Sea of Korea
santoriniensis24,a	G	N	resp	N	–	Y	25°C	Ferruginous hydrothermal marine sediment; Santorini; Greece
szutsaonensis25,a	–	Y	Y	–	Y	–	16–17°C	Soil; Szutsao solar saltern; southern Taiwan
lacisalsi26,a	–	N	Y	–	N	–	–	Water; hypersaline lake; ~50 km inland; saline-wetland; Fuente de Piedra; Spain
zhanjiangensis27,a	–	Y	Y	–	N	–	–	Sea water; tidal flat, Naozhou Island; South China Sea
oulmenensis28,a	–	Y	N	N	Y	–	–	Brine; salt concentrator (input material?); ~60 km inland; Ain Oulmene; Algeria.
daqiaonensis29,a	–	Y	N	N	–	–	–	Sediment; Daqiao salt pond; Yellow Sea; east coast of China
adhaerens30,a	–	Y	N	–	Y	–	–	Thalassiosira weissflogii diatom aggregates; Wadden sea surface; Germany
antarcticus31,a	–	Y	Y	–	Y	–	–	Intertidal sandy sediment; Larsemann Hills; Antarctica
xestospongiae32,a	–	Y	Y	Y	Y	–	–	Coastal marine sponge; 8 m depth; Obhor Sharm; Red Sea; Saudi Arabia
Terrestrial strain MB33	–	–	–	–	–	Y	–	Cyanobacterial mat; saline lake; near the Red Sea
manganoxydans34	G	–	–	–	–	–	–	Heavy metal-rich sediment; hydrothermal vent; Indian Ocean (Lat. 25.32, Long. 70.04)
Marinobacter-like isolates35,c	–	N	–	–	–	Y	~4°C	Weathering metal sulfide rock and sediment; Main Endeavour/Middle Valley; JdFR
Marinobacter-like clones36,d	–	–	–	–	–	–	≥4°C	Metal sulfides rock and sediment; Main Endeavour/Middle Valley; JdFR
Marinobacter clones37,e	–	–	–	–	–	–	4°C	Relict 50 ka metal sulfide sediment; Alvin mound; TAG; Mid-Atlantic Ridge
Marinobacter isolates38,f	–	–	–	–	–	–	~2°C	Lateral hydrothermal plumes; Mothra vent field and Axial Seamount; JdFR
Marinobacter env/enrich39,g	–	–	–	–	–	–	−0.4–−0.8°C	Fresh basalt; Arctic oceanic spreading ridges; Norwegian-Greenland Sea

Validly published species names as of April 2013.

Carbohydrates used by species are glucose, glycerol, fructose, maltose, mannitol, sucrose, cellobiose, galactose, dextrin, sorbital, trehalose, xylose, ribose, sorbose, erythritol, inositol, dulcitol, arabinose, and N-acetyl-D-glucosamine.

87–94%, 89–97%, 96–99%, 99%, 96–98% 16S rRNA gene sequence similarity to Marinobacter species, respectively.

Abbreviations: HC, hydrocarbon utilization; CH, carbohydrate utilization; NO.

1–39References:

Gauthier et al., ;

Huu et al., ;

Gorshkova et al., ;

Martín et al., ;

Rontani et al., ;

Shieh et al., ;

Yoon et al., ;

Yoon et al., ;

Romanenko et al., ;

Shivaji et al., ;

Takai et al., ;

Green et al., ;

Kim et al., ;

Liebgott et al., ;

Antunes et al., ;

Gu et al., ;

Guo et al., ;

Yoon et al., ;

Xu et al., ;

Montes et al., ;

Zhang et al., ;

Huo et al., ;

Roh et al., ;

Handley et al., ;

Wang et al., ;

Aguilera et al., ;

Zhuang et al., ;

Kharroub et al., ;

Qu et al., ;

Kaeppel et al., ;

Liu et al., ;

Lee et al., ;

Sigalevich et al., ;

Wang et al., ;

Edwards et al., ;

Rogers et al., ;

Müller et al., ;

Kaye and Baross, ;

Lysnes et al., 2004.

Table 2

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Marinobacter species	Halophilic	Optimum salinity (%)	Salinity range (%)	Mesophilic	Optimum temp (°C)	Temp range (°C)	Optimum pH	Major resp. quinone (ubiquinone)	G + C (%)a	Motility mechanismb
hydrocarbonoclasticus1,2	s-mod	3–6	0.5–20	Y	32	10–45	7.0–7.5	Q9	(52.7) 57.3	Polar flagellumc
aquaeolei2	slighlty	5	0–20	Y	30	13–50	–	Q9	55.7	Polar flagellum
excellens3	–	–	1–15	Y	28	10–41	7.5	Q9	56	Polarly flagellated
lipolyticus4	mod	7.5	1–15	Y	37	15–40	7.5		57	–
squalenivorans5	–	–	>0	Y	32	–	–		54.3	Polar flagellum
lutaoensis6	slighlty	3–5	0.5–12	therm	45	25–50	7.0	Q8	63.5	One–several flagella
litoralis7	s-mod	2–7	0.5–18	psyt	30–37	4–46	7.0–8.5	Q9	55	Polar flagellum
flavimaris8	s-mod	2–6	>0–20	psyt	37	≤4–45	7.0–8.0	Q9	58	Polar flagellum
daepoensis8	s-mod	2–6	>0–18	psyt	30–37	>4–45	7.0–8.0	Q9	57	Polar flagellum
bryozoorum9	–	–	1.0–18	Y	–	7–42	–		59.6	–
sediminum9	–	–	0.5–18	psyt	–	4–42	–		56.5	–
maritimus10	slighlty	4	1–13	psyt	22	4–37	8.5	Q9	58	–
alkaliphilus11	slighlty	2.5–3.5	0–21	Y	30–35	10–45	8.5–9.0	–	57.5	Polar flagellum
algicola12	s-mod	3–6	1.0–12	psyt	25–30	5–40	7.5	Q9	54–55	Polar flagellumc
koreensis13	s-mod	3–8	0.5–20	Y	28	10–45	6.0–8.0	Q9	54.1	Polar flagellum
vinifirmus14	s-mod	3–6	0–20	Y	20–30	15–45	6.5–8.4	–	58.7	–
salsuginis15	slighlty	5	1–20	Y	35–37	10–45	7.5–8.0	Q9	55.9	Polar flagellum
gudaonensis16	slighlty	2.0–3.0	0–15	Y	–	10–45	7.5–8.0	Q9	57.9	Polar flagellum
segnicrescens17	s-mod	4–8	1–15	Y	30–37	15–45	7.5–8.0	Q9	62.2	Polar flagellum
salicampi18	s-mod	8	>0–15	psyt	30	4–39	7.0–8.0	Q9	58.1	Polar flagellum
pelagius19	slighlty	5.0	0.5–15	psyt	35–30	4–48	7.0–8.0	–	59.0	–
guineae20	–	–	1–15	psyt	–	4–42	–	Q9	57.1	Polar flagella
psychrophilus21	–	–	2–8	psyph	16–18	0–22	6.0–9.0	Q9	55.4	–
mobilis22	slighlty	3.0–5.0	0.5–10.0	Y	30–35	15–42	7.0–7.5	–	58.0–58.9	Polar flagellum
zhejiangensis22	slighlty	1.0–3.0	0.5–10.0	Y	30–35	15–42	7.0–7.5	–	58.4	Polar flagellum
goseongensis23	slighlty	4–5	1–25	Y	25–30	10–37	7.5	–	–	–
santoriniensis24	mod	5–10	0.5–16	Y	35–40	15–45	7–8	Q9	58.1	Polar flagellum
szutsaonensis25	slighlty	5	0–20	Y	35–40	10–50	7.5–8.0	Q9	56.5	Polar flagellum
lacisalsi26	mod	7.5	3–15	Y	30–35	20–40	7.0	–	58.6	Polar flagellum
zhanjiangensis27	slighlty	2–4	1–15	psyt	25–30	4–35	7.5	Q9	60.6	Polar flagellum
oulmenensis28	mod	5–7.5	1–15	Y	37–40	30–47	6.5–7.0	Q9	57.4	–
daqiaonensis29	mod	5–10	1–15	Y	30	10–45	7.5	Q9	60.8	Polar flagellum
adhaerens30	s-mod	2–6	0.5–20	Y	34–38	4–45	7.0–8.5	Q9	56.9	Polar flagellum
antarcticus31	slighlty	3.0–4.0	0–25	psyt	25	4–35	7.0	–	55.8	Polar flagellum
xestospongiae32	slighlty	2.0	0.5–6.0	Y	28–36	15–42	7.0–8.0	Q9	57.1	Polar flagellum

GC contents range from 54.0–63.5% (average, 57.6%), using the Márquez and Ventosa (.

All species are motile, excluding M. goseongensis. M. lutaoensis also has bipolar pili. The number of flagella on M. guineae cells is unknown.

Unsheathed flagellum.

Abbreviations: Haloph, halophile; Mesoph, mesophile; temp, temperature; resp, respiratory; Y, yes; N, no; –, unknown; s-mod, slightly-moderately; psyt, psychrotolerant; psyph, psychrophile; therm, thermotolerant.

References: refer to Table 1.

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Marinobacter hydrocarbonoclasticus, denitrification and hydrocarbons

The genus was created for M. hydrocarbonoclasticus, which was isolated from hydrocarbon-polluted sediment, collected from the mouth of an oil refinery outlet along the French Mediterranean coast (Gauthier et al., 1992), and includes the later heterotypic synonym, M. aquaeolei (Huu et al., 1999; Márquez and Ventosa, 2005). The species has an obligate requirement for sodium. It grows readily on complex organic media containing yeast extract and peptone, and aerobically on a range of organic acids (acetate, butyrate, caproate, fumarate, adipate, lactate, citrate), and the amino acids L-glutamate, L-glutamine, and L-proline. Under anaerobic conditions M. hydrocarbonoclasticus can perform denitrification using a membrane-bound respiratory NarGHI complex to reduce nitrate (Correia et al., 2008). The nitrite formed is reduced to N2 via nitrite reductase cytochrome cd1 (Besson et al., 1995), nitric oxide reductase NorBC (EMBL-EBI ABM20188.1, ABM20189.1), and nitrous oxide reductase (Prudêncio et al., 2000). M. hydrocarbonoclasticus is most notable, however, for its ability to aerobically degrade liquid and solid, aliphatic (pristane, heneicosane, eicosane, hexadecane, tetradecane) and aromatic (phenanthrene, phenyldecane) hydrocarbons. It uses each hydrocarbon as a sole energy source, and produces large quantities of bioemulsifier. Bioemulsifiers (biosurfactants), are thought to aid in bacterial adhesion to hydrophobic surfaces, water-immiscible material breakdown, and competitor inhibition, and are attracting increasing interest for various industrial applications (Banat et al., 2000; Nerurkar et al., 2009; Williams, 2009; Soberón-Chávez and Maier, 2011).

Of the 34 species named since the genus was created, several exhibit hydrocarbonoclastic activity, while others remain untested (Table 1). Additional hydrocarbons utilized by Marinobacter species include squalene, which is metabolized under denitrifying conditions (Rontani et al., 2003), polycyclic aromatic hydrocarbons (PAHs) (Cui et al., 2008), hexane, heptane, petroleum ether (Shivaji et al., 2005; Antunes et al., 2007), n-pentadecane, n-tridecane, n-undecane, n-decane, n-nonane, butane, and kerosene (Takai et al., 2005).

This hydrocarbonoclastic capacity in Marinobacter has attracted attention owing to the potential for these bacteria to remediate crude oil contamination in environments as diverse as the Arabian Gulf (Al-Awadhi et al., 2007) and Artic sea ice (Gerdes et al., 2005). Nitrate reduction by Marinobacter species has also been exploited for potential use in oilfield maintenance. Dunsmore et al. (2006) showed reduction of added nitrate prevented deleterious growth of sulfate-reducing bacteria in produced water from a North Sea oilfield oil reservoir, controlling microbial souring reactions. The beneficial reduction of nitrate was largely attributed to indigenous Marinobacter species.

Expanded functional traits of the genus

Following the characterization of M. hydrocarbonoclasticus, the functional range of the genus has been further expanded to include (non-exhaustively) fermentation; the ability to respire at least 19 different carbohydrates (Table 1) and several extra amino (e.g., L-alanine, D-glutamate, L-phenylalanine; Antunes et al., 2007 and Green et al., 2006) and organic acids [e.g., malonate, formate, pyruvate, alpha-ketoglutarate; Kim et al. (2006) and Kharroub et al. (2011)]; degradation of the isoprenoid ketone 6,10,14-trimethylpentadecan-2-one (Rontani et al., 1997); growth on ethanol (Gu et al., 2007; Huo et al., 2008), phenol (Liebgott et al., 2006), and various Tweens (e.g., Takai et al., 2005; Green et al., 2006) following enzymatic evidence in M. hydrocarbonoclasticus; utilization of fumarate as an electron acceptor (Takai et al., 2005; Handley et al., 2009a); and oxidation/reduction of arsenic, iron or manganese (Handley et al., 2009a,b; Wang et al., 2012).

As for M. hydrocarbonoclasticus, all subsequently described species are able to grow aerobically on complex organic matter, and oxidize organic acids. Many, but not all are enzymatically able to reduce nitrate (Table 1). Lack of fermentation by M. hydrocarbonoclasticus was initially proposed as a distinctive feature of the genus; however, a number of subsequently isolated type strains exhibit both fermentative and respiratory metabolisms, owing to their ability to ferment glucose (Table 1), lactate (Handley et al., 2009a) and other substrates (Lee et al., 2012). Evaluation of recently available genome sequences also suggests certain Marinobacter species may exhibit enzymatic resistance to arsenic and heavy metals (e.g., Wang et al., 2012).

Biogeography and phylogeny

Marinobacter colonize diverse saline habitats, e.g., sea ice and hydrothermal sediments, facilitated by psychrophilic to thermotolerant physiologies, and an ability to metabolize an array of (in)organic compounds under aerobic or anaerobic conditions. However, evaluation of phylogenetic trees, constructed using 16S rRNA gene sequences, suggest the genus is monophyletic, forming a single clade distinct from other closely related epsilonproteobacterial lineages (Figure 1).

Figure 1

16S rRNA gene phylogenetic maximum-likelihood tree comparing The tree indicates the genus is monophyletic, despite the three orders being non-monophyletic (Williams et al., 2010). The same result was obtained using the neighbor-Joining method. Trees were constructed using MEGA v5.0 (Tamura et al., 2011), Clustal W alignments (Thompson et al., 1994), and 1000 bootstrap replicates. Bootstrap values ≥50 are shown. Sequences used were ≥1350 bp long. Marinobacter isolates are in dark font with type species bolded, and closely related Gammaproteobacteria are in pale font. GenBank accession numbers are given in parentheses. The symbols indicate Marinobacter isolate sources.

Despite the physiological versatility of the genus, and the ability of some strains to grow (non-optimally) without salt (e.g., Huu et al., 1999; Sigalevich et al., 2000; Liebgott et al., 2006), Marinobacter appear to be geographically restricted to marine or terrestrial environments rich in sodium salts. This observation is consistent with the hypothesis that microorganisms exhibit non-random biogeographical differentiation and distribution, due in part to environmental selection (Martiny et al., 2006).

In marine environments, dispersal does not appear to be a limiting factor for Marinobacter. Strains have been isolated from, and phylogenetically detected in, oceans (Pacific, Atlantic, Indian, Arctic, and Antarctic) and seas, spanning the globe from pole to equator (Table 1; Kaye et al., 2011). They display both attached and planktonic lifestyles, and the distribution of the genus extends from deep-ocean (hydrothermal) benthic sediment and exposed basalt to surface water, or coastal (hydrothermal) sediment, hot spring water and sand (Table 1; Figure 1).

In many instances, terrestrial isolation sources can be clearly linked to the ocean (e.g., coastal solar salterns and hot springs, and polluted soil from a coastal oil field; Table 1). Isolation of species from terrestrial sources, up to 50–60 km inland, implies a greater degree of terrestrial dispersal (Table 1; Figure 1 and Table S2 in Kaye et al., 2011). However, there is insufficient information regarding the nature of terrestrial isolation sources, and too few isolate and phylogenetic data, to judge how well-dispersed this genus is on land, or whether terrestrial sources are strictly independent from marine influences.

Lifesytles

In many respects Marinobacter species are generalists like their marine and terrestrial Alteromonadales cousins in the Shewanella genus. Shewanella species are respiratory generalists (e.g., Heidelberg et al., 2002), and at least one species (S. baltica) has been described as “very close to the ultimate [marine] r-strategist,” starkly contrasting with genomically streamlined K-strategist (or oligotrophic) marine bacteria like Prochlorococcus (Caro-Quintero et al., 2011). In the presence of surplus organic carbon, Marinobacter can grow rapidly, out-competing other bacteria in enrichment cultures (e.g., Handley et al., 2010). This r-strategist (or copiotrophic) behavior renders them weed-like and relatively easy to cultivate, even compared with other heterotrophic marine bacteria (Kaye and Baross, 2000). Marinobacter can also excel under aerobic-to-anaerobic conditions with no added substrate, while in the presence of Fe(II) (Edwards et al., 2003; Handley et al., 2013a).

This type of lifestyle exhibited by Marinobacter strains has been described as opportunistic or “opportunitrophic” (Singer et al., 2011), following the definition given by Moran et al. (2004) in describing the ability of the marine bacterium Silicibacter pomeroyi to switch rapid between lithoheterotrophy to heterotrophy in response to nutrient pulses. Use of “-troph” in this context describes the mode of obtaining nourishment (as for the term “psychrotroph”) rather than the source of the nourishment (as in “organotroph”), and as such may be considered a misnomer. The term was applied in order to differentiate between types of fast growing and nominally r-strategist bacteria, specifically between specialists (e.g., Geobacter, Mahadevan and Lovley, 2008), and generalists like Marinobacter, Shewanella, Pseudomonas, Vibrio and Roseobacter (Singer et al., 2011)—with the latter two genera already having been deemed opportunistic based on their versatile lifestyles (“opportunitrophs”; Polz et al., 2006). Singer et al. (2011) also identified other potential commonalities shared among the genomes of opportunistic bacteria and M. aquaeolei VT8, including a large genomic toolkit for responding to environmental stimuli and for defense (cf. Polz et al., 2006).

There are few phylogenetic studies of the environments from which Marinobacter species have been isolated that evaluate their in situ relative abundance. Nevertheless, the studies that have been published show two different scenarios for Marinobacter. Strains may be characterized as r-strategists or opportunistic (Polz et al., 2006; Singer et al., 2011), and dominate communities sporadically when stimulated by high nutrient loads, encountered, for example, in marine aggregates or enrichment cultures (Balzano et al., 2009; Handley et al., 2010). In contrast, relatively high in situ abundances of Marinobacter (Müller et al., 2010) and uncultured organisms closely related to Marinobacter (Rogers et al., 2003; Edwards et al., 2004) have been observed in some hydrothermal systems, implying these organisms may play an important and sustained role in post-depositional mineral alteration.

Hydrothermal settings

Marine hydrothermal systems are dispersed throughout the world's oceans (Martin et al., 2008), and support abundant psychrophilic-to-mesophilic life even in close proximity to high-temperature venting (Reysenbach and Cady, 2001; Edwards et al., 2003). A number of studies suggest Marinobacter may be significant in ‘low-temperature’ hydrothermal systems, defined by low-temperature hydrothermalism (e.g., ~8 to ~40°C, McCollom and Shock, 1997) or ambient seawater temperatures (e.g., ~2° in the deep ocean). This is due to their documented association with several different hydrothermal features (Table 1), and to their ability to heterotrophically or mixotrophically respire inorganic compounds abundant in hydrothermal systems.

A common hydrothermal feature found at plate boundaries, and with which Marinobacter or near-relatives have been associated (Edwards et al., 2003; Rogers et al., 2003; Müller et al., 2010), are massive sulfides, which comprise an estimated 6 × 108 tonnes of material globally (Hannington et al., 2011), and adjunct metalliferous sediments. While much of the material for massive sulfides originates from high-temperature hydrothermal fluids (>350°C) emanating from black smoker chimneys (Hannington et al., 2011), particulates distributed locally by plumes and talus from mound and chimney collapse can equilibrate with ambient temperatures (Edwards et al., 2003), or entire mounds can be inactive (Müller et al., 2010). Adjacent to massive sulfide deposits are low-temperature iron- and manganese-rich metalliferous sediments, derived from distal plume fallout with contributions from mound mass wasting (Jannasch and Mottl, 1985; Mills et al., 1993; Hannington et al., 1998)—possibly of the type from which M. manganoxydans was isolated (Wang et al., 2012).

Deposits consisting of iron oxyhydroxides, nontronite (a ferric iron-rich clay) and iron-manganese crusts can form independently at plate boundaries or at places of intra-plate volcanism (e.g., Alt, 1988; Karl et al., 1988; Boyd and Scott, 2001; Kennedy et al., 2004; Edwards et al., 2011). They form from diffuse low-temperature venting (Karl et al., 1988; Edwards et al., 2011), and can span areas >100 m2 (Boyd and Scott, 2001). Similar deposits exist in shallow marine settings, such as the ferruginous arsenic-rich sediments found in Papua New Guinea and Santorini (Smith and Cronan, 1983; Pichler and Veizer, 1999). M. santoriniensis was isolated from the Santorini sediment (Handley et al., 2009a).

Further examples of low-temperature hydrothermal habitats, with which Marinobacter or near relatives are associated, include those created by sharp temperature gradients that form across high-temperature chimney walls (Rogers et al., 2003), or buoyant plumes (Kaye and Baross, 2000) that rise 200–300 m up from these vents and spread laterally (German et al., 1991). Exposed, iron-rich basalt, delivered by oceanic spreading centers, provides another environment associated with many deep-sea hydrothermal systems (Lysnes et al., 2004), whereas M. alkaliphilus was isolated from alkaline serpentine mud (Takai et al., 2005) from a setting peculiar to mud volcanoes on the non-accretionary Mariana forearc (Fryer et al., 1999).

Function, biogeochemistry and hydrothermal systems

The various low-temperature hydrothermal settings Marinobacter(-like) species inhabit are rich in metals/metalloids, such as iron, manganese, arsenic, copper and zinc (Smith and Cronan, 1983; Hannington et al., 1998) that certain Marinobacter strains can transform enzymatically. Moreover, oxygen gradients established in these sediments may be exploited by Marinobacter species able to grow heterotrophically under anaerobic/aerobic conditions and mixotrophically under aerobic conditions.

Among the functions Marinobacter may perform in these environments is ferrous iron oxidation. The potential for Marinobacter Fe(II) oxidation was first suggested by Edwards et al. (2003) after isolating iron-oxidizing bacteria, phylogenetically resembling M. aquaeolei, from low-temperature hydrothermal metal sulfides. The isolates were able to grow chemoautotrophically on pyrite, basalt glass and siderite under micro-aerobic conditions. This promoted subsequent study of M. aquaeolei, including genome sequencing, and identification of its ability to anaerobically oxidize Fe(II) under mixotrophic conditions (Dhillon et al., 2005; Edwards et al., 2006; Singer et al., 2011). Subsequently, M. santoriniensis, which was isolated from iron-rich hydrothermal sediment, was also shown to perform nitrate-dependent Fe(II) oxidation when supplemented with a small amount of organic carbon (Handley et al., 2009a).

Interestingly, M. santoriniensis was isolated from sediment rife with stalk-like cells and bacteria phylogenetically resembling iron-oxidizing Zetaproteobacteria (Handley et al., 2010). Other Marinobacter (or near relatives) were also cultivated from environments containing stalks (Edwards et al., 2003; Lysnes et al., 2004) that speculatively belong to this increasingly characteristic phylum of marine iron-oxidizers—the Zetaproteobacteria (Emerson et al., 2007, 2010; Edwards et al., 2011).

As Marinobacter are reputedly more versatile than Mariprofundus ferrooxydans strains (the sole representatives of the Zetaproteobacteria) it is possible they perform other functions in these environments instead of, or in addition to, Fe(II) oxidation. For instance, Marinobacter and Marinobacter-like isolates have been implicated in Fe(III) reduction, but only in complex or simple co-cultures with other bacteria (Lysnes et al., 2004; Balzano et al., 2009; Handley et al., 2010). This metabolic trait remains to be demonstrated in definitively anexic cultures. M. santoriniensis has the genetic potential to reductively detoxify arsenate and mercury using proteins encoded by an Escherichia coli-like arsC and merRTA genes (Handley et al., 2013c), in addition to being able to conserve energy for growth via arsenate [As(V)] respiration using an unidentified mechanism, and mixotrophically oxidize arsenite [As(III)] using the aro gene cluster—making it one of a handful of bacteria currently known to completely redox-cycle arsenic (Handley et al., 2009b). This is particularly relevant given that the bacterium was isolated from sediment containing ~400 ppm of arsenic.

It remains to be explored whether other Marinobacter species share this ability to respire arsenic. However, there is cursory evidence for non-respiratory arsenate reductase (plus/minus putative respiratory arsenite oxidase) genes in several publically available Marinobacter genomes (namely, M. hydrocarbonoclasticus ATCC49840, GenBank FO203363.1, Grimaud et al., 2012; M. aquaeolei VT8, GenBank CP000514.1, Singer et al., 2011; M. adhaerens HP15, GenBank CP001978.1, Gärdes et al., 2010; M. algicola DG893, GenBank ABCP00000000.1; Marinobacter spp. BSs20148 and ELB17, GenBank CP003735.1 and AAXY00000000.1). Likewise, in a recent genome announcement Wang et al. (2012) described a Marinobacter candidate, M. manganoxydans MnI7-9 that has not only a putative arsC gene for arsenic detoxification (GenBank YP_005884959.1), but also a host of other genes that may be used for nickel, mercury, copper, chromate, zinc, cobalt, and cadmium resistance. This bacterium adsorbs and tolerates high levels of metals/metalloids, alongside a demonstrated ability to oxidize manganese, Mn(II), to a mixed-valency Mn(III)/Mn(IV) product via an unidentified genetic mechanism. Bacterial manganese oxidation is not thought to be an energy conserving process, but it is considered significant in environmental Mn(IV) oxide formation (Geszvain et al., 2012).

Conclusions and future directions

Although the genus is widespread in marine settings, and dozens of cultivated representatives and several sequenced genomes exist, the functional breath of Marinobacter species remains largely unexplored. The ability to metabolize hydrocarbons and inorganic elements (e.g., iron, arsenic, manganese) has been tested in relatively few species. Information, based on cultures and isolation source characteristics, suggests species within the genus are able to contribute, for example, to the degradation of hydrocarbons in oil-polluted sediment, and the oxidation of Fe(II) in ferruginous sediment or basalt. However, we know little about the nature and magnitude of their actual function in the environment. High-throughput omics (genomics, transcriptomics, proteomics) techniques promise to expand our knowledge into the uncultivated black box that encompasses much of the microbiome, and to facilitate in situ investigations of communities (e.g., Ram et al., 2005; Lo et al., 2007; Baker et al., 2012; Handley et al., 2013b), but are limited in part by the large number of genes of unknown function. Much can still be achieved from cultivation experiments. In moving forward, a combination of omics, functional gene expression studies, isotope tracer and cultivation techniques will provide a powerful complement of tools for characterizing both the real and potential function of microorganisms in marine settings and elsewhere, and elucidating the (opportunistic?) role of Marinobacter species in environmental biogeochemical cycles.

Conflict of interest statement

The authors declare that the research was conducted in the absence of any commercial or financial relationships that could be construed as a potential conflict of interest.