Search

We present in‐situ zircon laser ablation‐inductively coupled plasma‐mass spectrometry (LA‐ICP‐MS) U–Pb ages, whole‐rock geochemistry, and Sr–Nd–Pb–Hf isotopes of the Mugagangri monzogranite in the southern margin of the Qiangtang Block, Tibet, western China. The zircons yield a U–Pb age of ca. 123 Ma. The hornblende‐bearing monzogranite shows metaluminous to weak peraluminous and high‐K calc‐alkaline characteristics exemplified by high silica (SiO2 = 67.57–70.57 wt%), high aluminium (Al2O3 = 14.68–15.78 wt%), high potassium (K2O = 4.00–5.14 wt%), high alkali (K2O + Na2O = 7.88–8.62 wt%), and low calcium contents (CaO = 1.72–2.17 wt%), with the aluminium saturation index (A/CNK) ranging from 0.98 to 1.09, suggesting that the Mugagangri monzogranite is a metaluminous to weak peraluminous I‐type high‐K calc‐alkaline granite. Geochemically, similar to the arc magmas, the monzogranite is enriched in large‐ion lithophile elements, and relatively depleted in high‐field‐strength elements. The monzogranite displays relatively high (87Sr/86Sr)i values (0.70972–0.71240), uniform εNd(t) values (−2.24 to −3.40), variable zircon εHf(t) values (−14.1 to +8.0), and high radiogenic Pb isotopic values (206Pb/204Pb = 18.588–18.790, 207Pb/204Pb = 15.616–15.642, and 208Pb/204Pb = 38.838–39.053). These geochemical characteristics indicate that the monzogranite was derived from a mixed source comprising ancient crustal and mantle materials, and experienced fractional crystallization during emplacement. We propose that the parental magma of the Mugagangri monzogranite was most likely generated during northward subduction of the Bangong Co‐Nujiang Meso‐Tethys Ocean. [ABSTRACT FROM AUTHOR]

The Tibetan Plateau is characterized by the largest crustal thickness on Earth, although the timing of formation of the plateau remains debated. In this study, we present in situ laser ablation‐inductively coupled plasma‐mass spectrometry zircon U–Pb ages and Hf isotopes, and whole‐rock geochemical data on porphyritic granitoids of Sebuta in the central Lhasa block. Our zircon U–Pb data indicate that these rocks emplaced at ca. 89 Ma, in the early Late Cretaceous. Geochemically, the Sebuta biotite granite porphyry can be broadly divided into two subtypes, namely metaluminous porphyry and peraluminous porphyry. The metaluminous porphyry has high SiO2, Al2O3, Sr, low Y and Yb contents, and high Sr/Y and LaN/YbN ratios, showing adakitic features. These rocks have high K2O and Th contents, low Ti/Eu and Nd/Sm ratios, indicative of a continental crust affinity. Positive zircon εHf(t) values, along with high Mg#, Cr and Ni, imply that the Sebuta adakitic porphyry was most likely derived from partial melting of a delaminated thickened juvenile lower crust, and that the initial melts interacted with mantle peridotite during ascent. The field features, petrographic characteristics, formation age, ore‐bearing potential, and Hf isotope of the peraluminous porphyry are similar to those of the Sebuta adakitic porphyry, indicating that the peraluminous porphyry was likely formed by contamination with ancient crustal material and fractional crystallization from the same primary adakitic magmas which generated the Sebuta adakitic porphyry. Residual phases of amphibole + plagioclase + garnet + rutile in the source region, together with previous studies, suggest that the crust beneath the central‐northern Lhasa block experienced thickening during the early Late Cretaceous, and had already been thickened to more than 50 km by the Late Cretaceous (ca. 89 Ma). [ABSTRACT FROM AUTHOR]

Himalayan leucogranites are widely distributed in the North Himalayan gneiss dome (NHGD) and at the top of the Greater Himalayan Crystalline Complex (GHC) and are generally controlled by detachment faults. The ages of these prekinematic, synkinematic, and postkinematic leucogranites can be used to limit the activity of detachment structures (such as the South Tibetan Detachment System, STDS). Research on the STDS activity time in the eastern Himalayas is relatively sparse. In this study, the zircon and monazite U–Th–Pb geochronology of synkinematic and postkinematic leucogranites, which are affected by the STDS and NHGD, in four areas (Lhozhag, Kuju, Xiaozhan, and Cuonadong) in Shannan City, Tibet, China, was measured. The results show that the oldest synkinematic two‐mica granite from Lhozhag, which is affected by the STDS, is 24–25 Ma, so the time of STDS activity is at or slightly earlier than 25 Ma. The youngest synkinematic leucogranite is the garnet‐bearing muscovite granite in Cuonadong at 18.4 Ma. The oldest undeformed postkinematic leucogranite (not affected by the STDS) is the muscovite granite in Xiaozhan at 17.4 Ma. Therefore, the end of STDS activity can be limited to 18.4–17.4 Ma. The STDS includes three forms: detachment fault in the NHGD (northern extension of the STDS), the inner STDS between the GHC and Tethyan Himalayan Sequence, and the outer STDS at the bottoms of synformal klippes. In this paper, the active time limits of the above three kinds of detachment zones are comprehensively summarized. Based on this work, the northward extension (ductile deformation) time of the STDS in the region is considered to be 28–17 Ma. The exhumation of the GHC is mainly controlled by in‐sequence shearing: first, the South Tibet Thrust system (predecessor of the STDS) at the top of the GHC thrust southward at 45–28 Ma, then the High Himalayan Discontinuity fault in the middle of the GHC forms south‐vergent ductile thrusts at 28–17 Ma, and finally, the Main Central Thrust at the bottom of the GHC thrust southward at 17–9 Ma. [ABSTRACT FROM AUTHOR]

Miocene postcollisional potassic and adakitic rocks are widely distributed in the southern Lhasa terrane and western central Lhasa terrane. However, coeval potassic and adakitic rocks in eastern central Lhasa terrane were rarely recognized, and their origins and formation mechanism remain controversial. In this paper, we provide new geochronological and geochemical data for the Miocene postcollisional potassic and adakitic intrusions exposed in the Qingdu area, eastern central Lhasa terrane, southern Tibet. The Qingdu Miocene intrusions consist of quartz monzonite porphyry and biotite granite with coeval zircon U–Pb ages of 14.1 Ma and 14.0 Ma, respectively. They have high SiO2 (67.98–75.32 wt.%), Al2O3 (14.13–14.78 wt.%), and K2O (4.06–6.18 wt.%) and low MgO (0.25–1.46 wt.%) contents. They are both enriched in light rare earth elements (LREEs) and depleted in heavy rare earth elements (HREEs), with high (La/Yb)N (25.37–42.32) ratios. The biotite granite samples have low Y (7.10–9.96 ppm) and Yb (0.61–0.85 ppm) contents, and high Sr (229–384 ppm) contents and high Sr/Y (30–41) ratios, which show adakitic geochemical characteristics, whereas the quartz monzonite porphyry samples show potassic geochemical characteristics. They display initial (87Sr/86Sr)i ratios of 0.7083–0.7103, εHf(t) values of −6.7 to −0.1, εNd(t) values of −8.96 to −7.44, (208Pb/204Pb)i ratios of 39.028–39.110, (207Pb/204Pb)i ratios of 15.662–15.684, and (206Pb/204Pb)i ratios of 18.541–18.577. These signatures indicate that both the potassic and adakitic intrusions are more likely to originate from partial melting of a thickened lower crust, which were mainly the products of the binary mixing between the juvenile and ancient crust components. Based on the spatial distributions and isotopic features of the postcollisional potassic and adakitic rocks in the Lhasa terrane, we suggest that the differences of the lower crustal composition played a crucial role in causing the geochemical variations of the Miocene postcollisional adakitic and potassic rocks in Lhasa terrane. [ABSTRACT FROM AUTHOR]

The electromagnetic (EM) vortex imaging has been found to have a great potential application prospect in the imaging radar field. However, current studies focus on the motionless target, which seriously limits its application in practice. Therefore, to achieve EM vortex imaging for the motion target, this study proposes a parametric sparse representation model for EM vortex imaging that takes into account a translational motion target and uses the stepped frequency signal. An iterative algorithm is developed based on the sparse Bayesian learning (SBL) algorithm to estimate the velocity, and accomplish the EM vortex imaging exploiting SBL algorithm. Simulation results demonstrate that the proposed algorithm can improve velocity estimate accuracy in terms of relative error and achieve EM vortex imaging for the motion target. [ABSTRACT FROM AUTHOR]

Two DMTCNQ (DMTCNQ = 2,5‐dimethyl‐7,7,8,8‐tetracyano‐p‐quinodimethane) and DETCNQ (DETCNQ = 2,5‐diethyl‐7,7,8,8‐tetracyano‐p‐quinodimethane) gadolinium complexes [Gd(DMTCNQ)2(CH3OH)(H2O)6][DMTCNQ]·4H2O (1) and [Gd(DETCNQ)(H2O)7][2DETCNQ] (2) were synthesized by reactions of GdCl3·6H2O with Li(DMTCNQ) or Li(DETCNQ). X‐ray diffraction analysis reveals that complexes 1 and 2 are discrete complexes. The central metal atom in 1 is coordinated by two DMTCNQ ligand radicals whereas that in 2 is coordinated by just one DETCNQ ligand radical. The adjacent molecules are connected by the intermolecular hydrogen bonds to form the two‐dimensional (2D) supramolecular layer structures, which are further packed into a three‐dimensional (3D) supramolecular architecture through the π–π interactions between ligand radicals in 1 and 2. Magnetic investigation indicates that the antiferromagnetic interactions between spin carriers exists in 1 and 2. [ABSTRACT FROM AUTHOR]

The Cuonadong Dome in southern Tibet is a newly discovered gneiss dome in the Tethys Himalaya. Here, we investigate the Late Cambrian augen gneiss (orthogneiss) within the core of this dome to address the controversy surrounding early Palaeozoic tectonic evolution of the northern margin of eastern Gondwana. We report new zircon laser ablation multicollector inductively coupled plasma mass spectrometry (LA‐(MC‐)ICP‐MS) U‐Pb ages, Lu‐Hf isotopes, whole‐rock major and trace element geochemistry, and Sr‐Nd‐Pb data on representative samples from the granitic gneiss. The weighted mean of 116 analyses of zircon grains yields an age of 498.2 ± 1.5 Ma (mean square weighted deviation [MSWD] = 1.2). Forty‐one spots analyses on these grains show consistent εHf (t) values of −2 to +4 (average = +1.1), corresponding to Hf crustal model age (TDM2) of 1.3 to 1.6 Ga (average = 1.39 Ga). The orthogneiss (metagranite) is characterized by high Si and K contents, with low Al, Mg, and Ti, and A/CNK values ranging from 0.87 to 0.98 with an average of 0.92, indicating a metaluminous composition and I‐type granitoid affinity. The granitoid displays significant enrichment in light rare earth elements (LREEs) and relatively flat high rare earth element (HREE) patterns, with strong negative Eu anomalies (Eu/Eu* = 0.26–0.31). The primitive mantle‐normalized trace elements show a relative enrichment in large‐ion lithophile elements, such as Rb, and high‐field strength elements, such as Th, U, Zr, and Hf, with depletion in Ba, Nb, Ta, Sr, P, and Ti. The rocks show high initial 87Sr/86Sr ratios (0.7221–0.7248) and low εNd (t) values (−8.9 to −7.3) with Nd model ages (TDM) of 1.79–1.91 Ga. Their radiogenic Pb isotopic compositions show (206Pb/204Pb)t = 18.804–19.110, (207Pb/204Pb)t = 15.730–15.768, and (208Pb/204Pb)t = 38.409–39.054, indicating an ancient upper middle continental crustal origin. Our study shows that the protolith of the metagranite was most likely derived from the partial melting of upper continental crust with a minor contribution of depleted mantle materials. Through integration of the regional information on early Palaeozoic magmatism and metamorphic events, we contend that the protolith of the Cuonadong granitic gneiss formed in an accretionary setting associated with the early Palaeozoic Proto‐Tethys Oceanic plate subduction beneath the Gondwana continent. [ABSTRACT FROM AUTHOR]

The Lhasa terrane is one of the major segments of the Tibetan Plateau, with widespread Mesozoic to Cenozoic magmatic and metallogenic records. Here, we investigate timing and characteristics of magmatism associated with the Lunggar Fe skarn deposit in Central Lhasa. We also present Sr–Nd–Pb and Hf (zircon) isotopic data on three associated intrusions to gain insights on the tectonic and metallogenic evolution of the region. Our data reveal at least two magmatic pulses in Lunggar represented by Early Cretaceous I‐type granodiorite (112.9 ± 1.5 Ma) and granite porphyry (112.6 ± 1.3 Ma) with magma generation related to slab break‐off associated with the Bangong–Nujiang Ocean during closure of the Meso‐Tethyan ocean at ~113 Ma. Iron skarn mineralization at Lunggar was contemporaneous with local Early Cretaceous intrusive activity. Following this, Late Cretaceous adakitic diorite (90.5 ± 1.5 Ma) formed from delaminated thickened crust at ~91 Ma related to the northern subduction of the Yarlung‐Zangbo oceanic plate. We also provide a comprehensive review of the Cretaceous tectonic evolution of Central Lhasa, which trace the tectonic evolution as follows: (a) 145–120 Ma: southward subduction of the Bangong–Nujiang oceanic plate under the Lhasa terrane; (b) 120–115 Ma: Lhasa‐Qiangtang continental collision; (c) 115–110 Ma: slab break‐off of the Bangong–Nujiang Ocean; (d) 110–95 Ma: crustal thickening of the Central Lhasa lower crust; (e) 95–80 Ma: delamination of lithospheric mantle; and (f) 80–65 Ma: northward subduction of the Yarlung‐Zangbo oceanic plate and subsequent slab rollback. The related metallogenic events in Central Lhasa include (a) ~115–110 Ma skarn Fe mineralization associated with slab break‐off; (b) ~90–80 Ma porphyry Cu–Au mineralization formed in delaminated thickened crust of Central Lhasa; and (c) ~65 Ma skarn Pb–Zn mineralization produced from slab rollback of the Yarlung‐Zangbo Ocean. [ABSTRACT FROM AUTHOR]

Abstract: Reactions of N,N′‐bis (salicylidene)‐1,2‐cyclohexanediamine (H2L) with mixed lanthanide counterions of LnCl3·6H2O and Ln (NO3)3·6H2O afford six H2L lanthanide coordination polymers, e.g. {[Pr(H2L)2(NO3)2Cl]·2CH2Cl2}n (1); {[Ln(H2L)1.5(NO3)3]2·5CHCl3·mCH3OH}n [Ln = Sm (2), Eu (3), Gd (4), Tb (5) and Yb (6); m = 1 (2–5); m = 0 (6)]. X‐ray crystallographic analysis reveals that complex 1 exhibits three‐dimensional diamondoid topologic structure and complexes 2–6 are of two‐dimensional structure. Luminescent spectra show that complexes 1 and 6 have characteristic near‐infrared (NIR) emission of praseodymium (III) and ytterbium (III) ions and complexes 2–5 emit luminescence in the visible region. Complexes 3 and 6 reveal sensitive luminescence responses to formaldehyde. [ABSTRACT FROM AUTHOR]

The Duolong porphyry Cu-Au deposit (5.4 Mt at 0.72% Cu, 41 t at 0.23 g/t Au) was recently discovered in the southern Qiangtang terrane, central Tibet. Here, new whole-rock elemental and Sr-Nd-Pb isotope and zircon Hf isotopic data of syn- and post-ore volcanic rocks and barren and ore-bearing granodiorite porphyries are presented for a reconstruction of magmas associated with Cu-Au mineralization. LA-ICP-MS zircon U-Pb dating yields mean ages of 117.0 ± 2.0 and 120.9 ± 1.7 Ma for ore-bearing granodiorite porphyry and 105.2 ± 1.3 Ma for post-ore basaltic andesite. All the samples show high-K calc-alkaline compositions, with enrichment of light rare earth elements (LREE) and large ion lithophile elements (LILE: Cs and Rb) and depletion of high field strength elements (HFSE: Nb and Ti), consistent with the geochemical characteristics of arc-type magmas. Syn- and post-ore volcanic rocks show initial Sr ratios of 0.7045-0.7055, εNd(t) values of −0.8 to 3.6, (206Pb/204Pb)t ratios of 18.408-18.642, (207Pb/204Pb)t of 15.584-15.672 and positive zircon εHf(t) values of 1.3-10.5, likely suggesting they dominantly were derived from metasomatized mantle wedge and contaminated by southern Qiangtang crust. Compared to mafic volcanic rocks, barren and ore-bearing granodiorite porphyries have relatively high initial Sr isotopic ratios (0.7054-0.7072), low εNd(t) values (−1.7 to −4.0), similar Pb and enriched zircon Hf isotopic compositions [εHf(t) of 1.5-9.7], possibly suggesting more contribution from southern Qiangtang crust. Duolong volcanic rocks and granodiorite porphyries likely formed in a continental arc setting during northward subduction of the Bangong-Nujiang ocean and evolved at the base of the lower crust by MASH (melting, assimilation, storage and homogenization) processes. Copyright © 2014 John Wiley & Sons, Ltd. [ABSTRACT FROM AUTHOR]

A series of five l-di- p-toluoyl-tartaric acid ( l-DTTA) lanthanide coordination polymers, namely {[Ln4K4 L6(H2O)x]⋅yH2O}n, [Ln=Dy ( 1), x=24, y=12; Ln=Ho ( 2), x=23, y=12; Ln=Er ( 3), x=24, y=12; Ln=Yb ( 4), x=24, y=11; Ln=Lu ( 5), x=24, y=12] have been isolated by simple reactions of H2L (H2L= L-DTTA) with LnCl3⋅6 H2O at ambient temperature. X-ray crystallographic analysis reveals that complexes 1- 5 feature two-dimensional (2D) network structures in which the Ln3+ ions are bridged by carboxylate groups of ligands in two unique coordinated modes. Luminescent spectra demonstrate that complex 1 realizes single-component white-light emission, while complexes 2- 4 exhibit a characteristic near-infrared (NIR) luminescence in the solid state at room temperature. [ABSTRACT FROM AUTHOR]

The Bangong- Nujiang suture ( BNS) between the Lhasa and Qiangtang terranes is an important boundary and its petrogenesis is controversial. Diabase from the accretionary prism in the southern Qiangtang terrane yields a zircon U- Pb age of 181.3 ± 1.4 Ma. All the diabases show tholeiitic basalt compositions, gentle enrichment patters of light rare earth elements ( REE), variable enrichment in incompatible element concentrations (e.g. Th and Rb), and no anomaly in high field strength elements (e.g. Nb and Ta), similar to that of enriched mid-ocean ridge basalt ( E- MORB). They have relatively homogeneous whole rock Nd (ε Nd(t) = 7.3-9.1) and zircon Hf- O isotopic compositions (ε Hf(t) = 14.8-16.1, and δ18 O = 4.57-6.12‰), possibly indicating melting of the depleted mantle and no significant crustal contamination during the petrogenesis. The element variations suggest that the diabases were formed by plume-ridge interaction at a mid-ocean ridge within the Bangong- Nujiang ocean. [ABSTRACT FROM AUTHOR]

The complexity of natural triacylglycerols (TAGs) in various edible oils is prodigious due to the hundreds of set is of TAG compositions, which makes the identification of TAGs quite difficult. In this investigation, the off-line 2D system coupling of nonaqueous RP and silver-ion HPLC with atmospheric pressure chemical ionization MS detection has been applied to the identification and quantification of TAGs in peanut oil. The method was successful in the separation of a high number of TAG solutes, and the TAG structures were evaluated by analyzing their atmospheric pressure chemical ionization mass spectra information. HPLC and MS conditions have been optimized and the fragmentation mechanisms of isomers have been validated. In addition, an internal standard approach has been developed for TAG quantification. Then this system was applied in peanut oil samples and there was a total of 48 TAGs including regioisomers that have been determined and quantified. [ABSTRACT FROM AUTHOR]

The title compound, {[Co(C9H7O5)2(C10H8N2)(H2O)2]·2H2O} n, has an infinite one-dimensional chain structure along the a axis. The Co atom and the mid-point of the bipyridine group are located on inversion centres. A three-dimensional supra­molecular network is built up by O—H⋯O hydrogen-bonding inter­actions between water mol­ecules, carboxyl hydr­oxy groups and carboxyl­ate groups. [ABSTRACT FROM AUTHOR]

In the title mol-ecular salt, C(14)H(13)N(2)O(2) (+)·ClO(4) (-), the ring systems in the cation are almost coplanar [dihedral angle = 5.53 (13)°]. Intra-molecular N-H⋯O and O-H⋯O hydrogen bonds generate S(6) and S(5) rings, respectively. In the crystal, the two H atoms involved in the intra-molecular hydrogen bonds also participate in inter-molecular links to acceptor O atoms of the perchlorate anions. A simple inter-molecular N-H⋯O bond also occurs. Together, these form a double-chain structure along [101].

In the anion of the title salt, C(6)H(16)N(+)·C(18)H(13)O(8) (-), one of the carboxyl groups is deprotonated. Its O atoms are involved in inter-molecular hydrogen bonding with the carboxyl group of an adjacent anion and the amino group of an adjacent cation. The two benzoyloxy rings are oriented with respect to each other at a dihedral angle of 79.46 (6)°.

In the title complex, [Co(C(22)H(18)N(2)O(4))(CN)(H(2)O)]·0.5CH(3)CN, the Co(III) cation is N,N',O,O'-chelated by a 6,6'-dimeth-oxy-2,2'-[1,2-phenyl-enebis(nitrilo-methanylyl-idene)]diphenolate dianion, and is further coordinated by a cyanide anion and a water mol-ecule in the axial sites, completing a distorted octa-hedral coordination geometry. In the crystal, pairs of bifurcated O-H⋯(O,O) hydrogen bonds link adjacent mol-ecules, forming centrosymmetric dimers. The acetonitrile solvent mol-ecule shows 0.5 occupancy.

In the title compound, [KYb(C(2)O(4))(2)(H(2)O)(4)](n), the Yb(III) ion lies on a site of [Formula: see text] symmetry in a dodeca-hedral environment defined by eight O atoms from four oxalate ligands. The K atom lies on a different [Formula: see text] axis and is coordinated by four O atoms from four oxalate ligands and four water O atoms. The oxalate ligand has an inversion center at the mid-point of the C-C bond. The metal ions are linked by the oxalate ligands into a three-dimensional framework. O-H⋯O hydrogen bonding is present in the crystal structure.

In the title compound, [KLu(C(2)O(4))(2)(H(2)O)(4)](n), the Lu(III) ion lies on a site of [Formula: see text] symmetry in a dodeca-hedron defined by eight O atoms from four oxalate ligands. The K atom lies on another site of the same symmetry and is coordinated by four oxalate O atoms and four O water atoms. The mid-point of the C-C bond of the oxalate group lies on an inversion center. In the packing structure, each oxalate ligand links two Lu(III) and two K atoms, forming a three-dimensional open framework with channels running along [001]. Inter-molecular O-H⋯O hydrogen bonds occur.

In the heterodinuclear title complex, [GdZn(C(22)H(18)N(2)O(4))(CH(3)COO)(3)], the Zn(II) ion is five-coordinated in a square-pyramidal environment defined by two O atoms and two N atoms from the ligand, forming the square plane, and one acetate O atom serving as the apex, while the Gd(III) ion is nine-coordinated in an approximate mono-capped tetra-gonal-anti-prismatic environment defined by four O atoms from the ligand and five acetate O atoms.

In the title complex, [Co(C(22)H(18)N(2)O(4))(CN)(H(2)O)]·CH(3)CN, the Co(III) ion is six-coordinated in a distorted octa-hedral environment defined by two N atoms and two O atoms from a salen ligand in the equatorial plane and one O atom from a water mol-ecule and one C atom from a cyanide group at the axial positions. O-H⋯O hydrogen bonds connect adjacent complex mol-ecules into dimers. C-H⋯N hydrogen bonds and π-π inter-actions between the benzene rings [centroid-centroid distances = 3.700 (2) and 3.845 (2) Å] are also present.

In the title dinuclear Cu(II)-Lu(III) salen-type complex, [CuLu(C(22)H(24)N(2)O(4))(NO(3))(3)], with the ligand 6,6'-dimeth-oxy-2,2'-[cyclo-hexane-1,2-diylbis(nitrilo-methyl-idyne)]diphenolate, the irregular nine-coordinate Lu(III) coordination sphere comprises four O atoms from the ligand and five O atoms from three nitrate groups, two bidentate and one monodentate [Lu-O = 2.230 (3)-2.621 (4) Å]. The slightly distorted square-planar four-coordinate Cu(II) atom comprises two imine N atoms [Cu-N = 1.903 (4) and 1.912 (4) Å] and two phenolate O atoms from the ligand mol-ecule [Cu-O = 1.897 (3) and 1.906 (3) Å]. All atoms of the cyclo-hexane ring of the ligand mol-ecule are disordered over two sets of sites with equal occupancy.

In the title mononuclear salen-type complex, [Eu(NO(3))(3)(C(22)H(26)N(2)O(4))]·CH(3)OH, the Eu(III) ion is ten-coordinated by three bidentate nitrate counter-ions and one organic salen-type ligand, which acts in a bis-bidentate chelating mode through its phenolate and meth-oxy O atoms. The protonated imine groups are involved in intra-molecular N-H⋯O hydrogen bonds to the phenolate O atomss, emphasizing the zwitterionic nature of the ligand. An O-H⋯O hydrogen bond links the complex and solvent mol-ecules.

The mol-ecule of the title compound, C(22)H(26)N(2)O(4), has two azomethine linkages, both of which are in an E configuration. The cyclo-hexyl ring adopts a chair conformation. The dihedral angle between the benzene rings is 66.57 (9)°. The mol-ecular structure is stabilized by two intra-molecular O-H⋯N hydrogen bonds.

In the title mononuclear complex, [La(NO(3))(3)(C(22)H(26)N(2)O(4))]·CH(3)OH, the La(III) ion is coordinated by three bidentate nitrate counter-ions and one zwitterionic 6,6'-dimeth-oxy-2,2'-[(cyclo-hexane-1,2- di-yl)bis-(nitriliomethyl-idyne)]diphenolate ligand through two phenolate and two meth-oxy O atoms, while the protonated N atoms remain uncoordinated. H atoms located on the two N atoms are involved in intra-molecular hydrogen bonds with the deprotonated phenol O atoms, indicating that proton migration occurs during the lanthanum complexation.

In the mononuclear salen-type complex, [Er(NO(3))(3)(C(18)H(20)N(2)O(4))], the Er(III) ion is ten-coordinated in a distorted hexa-deca-hedral geometry by six O atoms of three nitrate anions and four O atoms of the salen-like ligand. Inter-molecular N-H⋯O hydrogen bonds occur. The crystal structure is stabilized by inter-molecular C-H⋯O hydrogen bonds.

In the title mononuclear Schiff base complex, [Dy(NO(3))(3)(C(18)H(20)N(2)O(4))], the Dy(III) ion is ten-coordinated in a distorted hexa-deca-hedral geometry by six O atoms of three nitrate anions and four O atoms of the Schiff base ligand. An intra-molecular N-H⋯O hydrogen bond occurs. The crystal structure is stabilized by inter-molecular C-H⋯O hydrogen bonds.

In the title heteronuclear complex, [CuSm(C(19)H(20)N(2)O(4))(NO(3))(3)(CH(3)COCH(3))], the Cu(II) ion is five-coordinated by two O and two N atoms from the 6,6'-dimeth-oxy-2,2'-[propane-1,2-diylbis(nitrilo-methyl-idyne)]diphenolate ligand (L) and by an O atom from the acetone mol-ecule in a square-pyramidal geometry. The Sm(III) ion is ten-coordinated by six O atoms from the three nitrate ligands and four O atoms from the L ligand. In L, the C atoms of the diamino-propane fragment are disordered over two positions in a 0.674 (10):0.326 (10) ratio.

In the title complex, [Fe(C(22)H(24)N(2)O(4))]·H(2)O, the Fe(II) center is four-coordinated by two O and two N atoms from 2,2'-[6,6'-dimethoxy-cyclo-hexane-1,2-diylbis(nitrilo-methyl-idyne)]diphen-olate (L) ligands in a distorted square-planar geometry. Uncoordinated water and FeL mol-ecules are paired via inter-molecular water-meth-oxy O-H⋯O hydrogen bonds.

In the title heteronuclear complex, [CuTb(C(19)H(20)N(2)O(4))(NO(3))(3)(CH(3)COCH(3))], the Cu(II) ion is five-coordinated by two O and two N atoms from the 6,6'-dimeth-oxy-2,2'-[propane-1,2-diylbis(nitrilo-methyl-idyne)]diphenolate ligand (L) and an O atom from the acetone mol-ecule in a square-pyramidal geometry. The Tb(III) ion is ten-coordinated by six O atoms from three chelating nitrate ligands and four O atoms from the L ligand. In L, the CH(2)-CH-CH(3) fragment is disordered over two conformations, with refined occupancies of 0.725 (11) and 0.275 (11).

In the title complex, [Co(C(22)H(24)N(2)O(4))]·H(2)O, the Co(II) atom is in an almost square-planar coordination environment involv-ing two O and two N atoms from the Schiff base ligand. A water mol-ecule cocrystallizes with the coordination compound and may be held in the crystal by O-H⋯O hydrogen bonds. Heteroatomic π-π ring inter-actions may be present between symmetry-related complexes, with centroid-centroid distances of 3.5661 (8) Å.

The asymmetric unit of the title compound, [Fe(4)(C(9)H(8)O(2))(4)(CH(3)OH)(2)], contains one half-mol-ecule located on a twofold rotational axis. In the mol-ecule, the two Fe(II) ions bridged by two coordinating methanol mol-ecules are separated by 3.1286 (7) Å. Two crystallographically independent methanol mol-ecules are situated on a twofold rotational axis; all attached H atoms are rotationally disordered between two equal orientations.

In the title complex, [Mn(C(17)H(16)N(2)O(2))Cl], the Mn(III) ion is coordinated by two O [Mn-O = 1.719 (2) and 1.813 (2) Å] and two N [Mn-N = 1.824 (2) and 1.931 (2) Å] atoms from the tetra-dentate Schiff base ligand and a chloride anion [Mn-Cl = 2.9634 (16) Å] in a square-pyramidal geometry. In the ligand, the two benzene rings form a dihedral angle of 68.06 (5)°.

In the title complex, [CuEu(C(19)H(20)N(2)O(4))(NO(3))(3)], the Cu(II) ion is four-coordinated in a square-planar geometry by two O atoms and two N atoms of the deprotonated Schiff base. The Eu(III) atom is ten-coordinate, chelated by three nitrate groups and linked to the four O atoms of the deprotonated Schiff base.

In the title complex, [CuSm(C(19)H(20)N(2)O(4))(NO(3))(3)]·CH(3)CO-CH(3), the Cu(II) atom is four-coordinated in a square-planar geometry by two O atoms and two N atoms of the deprotonated Schiff base. The Sm(III) atom is ten-coordinate, chelated by three nitrate groups and linked to the four O atoms of the deprotonated Schiff base.