carbonate

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padc polyallyl diglycol carbonate的中文翻译padc polyallyl diglycol carbonatePADC聚烯丙基二甘醇碳酸酯

就是碳酸氢钠 用来碱化尿液，解救巴比妥中毒!

唉,百度知道上怎么写结构式呀,真是麻烦 CH2=CH-C（=O）-O-C（=O）-OH C（=O）代表羰基,在知道上没办法写出来,你写的时候把碳原子和氧原子用双键链接 一楼的是从百度知道上弄下来的吧,分子式给的不对,他给的是碳酸丙酯!

The geochemical or long-term carbon cycle primarily involves the exchange of carbon between the ‘surficial"and ‘geologic"reservoirs. The former comprise atmosphere，oceans，biosphere， soils，and exchangeable sediments in the marine environment ( Fig. 1) while the latter include crustal rocks and deeply buried sediments in addition to the underlying mantle. How carbon is partitioned between the various reservoirs of the surficial system and between surficial and geologic reservoirs is what sets the concentration of CO2in the atmosphere. Life，and the cycle of organic carbon，as well as its geological ( and subsequent fossil fuel exhumation ) is of particular importance in this regard. The cycle of carbon in its inorganic，calcium carbonate ( CaCO3) form also affects atmospheric CO2，but by more subtle means. It also plays a fundamental role in regulating ocean chemistry and pH—a major factor in the viability of calcareous marine organisms.Carbonate precipitation and burialToday，the surface of the ocean is everywhere more than saturated ( over-saturated) with respect to the solid carbonate phase，with a mean value for the saturation state ( Ω: saturation state of the solution，also known as the solubility ratio) of calcite of 4. 8. In other words，the minimum thermodynamical requirement for calcite to precipitate is exceeded by a factor of almost 5. Despite this，the spontaneous precipitation of CaCO3from the water column is not observed in the ocean. This is because the initial step of crystal nucleation is kinetically unfavorable，and experimentally，spontaneous ( homogeneous) nucleation does not occur in sea water solutions until Ωcalcite＞ ～ 20 – 25 ( Ω = ［Ca2+］×［CO2-3］ /Ksp) . Although CaCO3precipitation occurs as cements and coatings in the marine environment，it is primarily associated with the activities of living organisms， particularly corals， benthic shelly animals， plankton species such as coccolithophores and foraminifera，and pteropods，and where it takes place under direct metabolic control. In comparison，carbonate deposition in fresh-water systems is of only minor importance globally，and will not be discussed further here.While not in itself sufficient to drive substantial abiotic precipitation，the saturation state of the modern ocean surface is favorable to the preservation of carbonates deposited in shallow water ( neritic) environments. Long-term accumulation of this material can result in the formation of extensive marine topographical features such as barrier reefs and carbonate banks and platforms. A different fate awaits CaCO3precipitated in the open ocean by plankton such as coccolithophores and foraminifera，however. This is because oceanic waters become increasingly less saturated with depth. Below the depth of the saturation horizon，conditions become under-saturated ( Ω ＜ 1. 0) and carbonate will start to dissolve. In the modern ocean the calcite saturation horizon lies at about 4500 m in the Atlantic and ～ 3000 m in the Pacific Ocean. Within a further 1000 m sediments are often completely devoid of carbonate particles ( the carbonate compensation depth， or CCD) . Topographic highs on the ocean floor such as the mid-Atlantic ridge can thus be picked out by sediments rich in CaCO3while the adjacent deep basins are low in % CaCO3. The visual effect has been likened to snow-capped mountains. The pressure induced surface-to-deep vertical contrast in Ω is further enhanced by the respiration of organic matter and release of metabolic CO2 in the ocean interior which suppresses the ambient carbonate ion concentration and thus Ω. The greater accumulation of metabolic CO2in the older water masses of the deep Pacific explains why the sea-floor there is much poorer in % CaCO3compared to the Atlantic at a similar depth.Fig. 1 The global biogeochemical cycling of calcium carbonate. ( a) Modes of CaCO3transformation and recycling within the surficial system and loss to the geological reservoir ( labeled ‘1 " through ‘4 ") .① Precipitation of calcite by coccolithophores and foraminifera in the open ocean; Ca+2+ 2HCO－3→CaCO3+CO2( aq)+ H2O. ② Carbonate reaching deep-sea sediments will dissolve during early diagenesis if the bottom water is under-saturated and / or the organic matter flux to the sediments is sufficiently high. ③ Precipitation of CaCO3by corals and shelly animals，with a significant fraction as the aragonite polymorph. Because modern surface waters are over-saturated relatively little of this carbonate dissolves in situ，and instead contributes to the formation of reefal structures or is exported to the adjoining continental slopes. ④ Precipitation of CaCO3 results in higher pCO2at the surface，driving a net transfer of CO2from the ocean to the atmosphere.( b) Modes of CaCO3transformation and recycling within the geologic reservoirs and return to the surficial system ( labeled“5”through“8”) . ⑤ CaCO3laid down in shallow seas as platform and reef carbonates and chalks can be uplifted and exposed to erosion through rifting and mountain-building episodes. CaCO3can then be directly recycled; CO2+ H2O + CaCO3→Ca+2+ 2HCO－3. ⑥ Thermal breakdown of carbonates subducted into the mantle or deeply buried. The decarbonation reaction involved is essentially the reverse of silicate weathering，and results in the creation of calcium silicates and release of CO2; CaCO3+ SiO2→CO2+ CaSiO3.⑦ Weathering of silicate rocks; 2CO2+ H2O + CaSiO3→Ca+2+ 2HCO－3+ SiO2. ⑧ Emission to the atmosphere of CO2produced through decarbonation. This closes the carbon cycle on the very longest time-scales.Unfortunately，the carbonate cycle does not conform to this simple picture，and a significant fraction of CaCO3appears to dissolve in the water column even before it can reach the sediment surface. This has been something of an enigma because the reduction in carbonate flux measured by sediment traps occurs well above the depth at which calcite becomes thermodynamically unstable. Dissolution of carbonate particles in acidic digestive conditions of zooplankton guts has been one proposed mechanism. Acidic micro-environments within individual ‘marine snow " aggregates may also be important. Another possible explanation surrounds the aragonite polymorph because it becomes susceptible to dissolution at much shallower depths than calcite under the same ambient conditions. In support of this are recent estimates of the depth at which most CaCO3 dissolution occurs in the ocean which appears to correspond to the aragonite saturation horizon. However，calculations suggest that solute release from sinking pteropod shells，the main aragonite product in the open ocean，should mostly occur much deeper than this. Dissolution of aragonite also does not help explain how 65% of calcitic foraminiferal tests can be lost at shallow depths. This uncertainty is of concern because a full appreciation of the controls of atmospheric CO2and response to global change requires an understanding of the dissolution and the depth of recycling of CaCO3in the water column.Overall，more than 80 % of all carbonate precipitated in the open ocean dissolves either in the water column or within the uppermost layers of the underlying sediments. The remainder，some 1 Gt CaCO3yr－ 1accumulates in deep-sea sediments. This burial loss，to which can be added as much as another 1 Gt CaCO3yr－ 1of deposition in neritic environments ( although the uncertainty in this figure is substantial) ，must somehow be balanced if the ocean is not to run out of calcium ions! This is achieved through the weathering of carbonate and silicate rocks.Weathering and Carbonate RecyclingThe weathering of calcium carbonate and calcium silicate minerals in soils and at exposed rock surfaces helps balance the CaCO3sedimentation loss by unlocking Ca2 +from the geologic reservoir. Alteration of ocean crust by percolating fluids adds an additional but more minor contribution. The weathering reactions ( see Fig. 1b; ⑤ and ⑦) provide the other raw material necessary for carbonate precipitation— bicarbonate ions ( HCO－3) . However，because the transformation 2CO2→2HCO－3( Fig. 1b; ⑦) is internal to the surficial system and does not represent a source of new carbon，the component of CaCO3burial derived from silicate rock weathering represents a loss of carbon to the geologic reservoir. This must be replaced on the long-term，achieved through the release of CO2to the atmosphere from volcanic sources. ( In contrast，the weathering and burial of CaCO3results into net loss or gain of CO2to the surficial system) .A powerful regulatory mechanism of the Earth system arises because weathering rates respond to surface temperature and atmospheric CO2while simultaneously silicate weathering rates control the rate of transformation CO2→HCO－3and thus rate of loss of carbon through CaCO3burial. This is a negative feedback system and acts to regulate the concentration of CO2in the atmosphere over hundreds of thousands of years.Buried carbonate is eventually recycled back from the geologic reservoir. This can occur if carbonates laid down in shallow seas such as limestones or chalks are subsequently uplifted and exposed to weathering as a result of mountain building episodes. However，carbonates deposited in open ocean sediments are only infrequently exposed at the Earth"s surface，as ophiolite complexes—portions of the oceanic crust and overlying sediments that have been trapped between colliding cratonic blocks and uplifted. Instead，the primary recycling of deep-sea CaCO3occurs through subduction into the upper mantle and decarbonation ( Fig. 1b; ⑥) .At this point it is important to recognize that carbonate burial represents the principal geologic mechanism of CO2removal from the ocean and atmosphere. However，the act of precipitating CaCO3has the effect of re-partitioning dissolved carbon in the surface ocean into CO2 ( aq)，raising ambient pCO2and pH. Thus，precipitation and deposition of CaCO3have the short-term effect of increasing the concentration of CO2in the atmosphere at the expense of the ocean carbon inventory，but at the same time represents the ultimate long-term sink for CO2.Both texts are selected from: The role of the global carbonate cycle in the regulation and evolution of the Earth system，Earth and Planetary Science Letters 234，2005: 299 － 315By: Andy Ridgwell，Department of Earth and Ocean Sciences，The University of British Columbia，6339 Stores Road，Vancouver，British Columbia，Canada V6T 1Z4andRichard E. Zeebe，University of Hawaii at Manoa，SOEST，Honolulu，HI，United StatesNew words and expressionsPart A地球科学专业英语Part B地球科学专业英语

vanadium carbonate是:碳酸钒：V(CO3)2.V 是正四价。碳酸根是负二价。

c H O

caesium carbonate[英][ˈsi:ziəm ˈkɑ:bəneit][美][ˈsiziəm ˈkɑrbəˌnet]n.碳酸铯; 网络释义1. 碳酸铯

sodium carbonate[英][ˌsəʊdiəm ˈkɑ:bənət][美][ˌsoʊdiəm ˈkɑ:rbənət]碳酸钠; 纯碱; 形近词：Sodium Carbonate数据合作方：金山词霸双语例句英英释义1meanwhile, we also provide you trisodium phosphate, alkali protease, sodium carbonate, sodium sulphide and bicarbonate, etc.本公司同时经营磷酸三钠、碱性蛋白酶、硫化碱、纯碱、小苏打等化工产品。

碱式的如magnesium hydroxycarbonate碱式碳酸铜

calcium carbonate n. 碳酸钙;

是碳化钙俗名电石分子式CAC22CAO+5C=2CAC2+CO2

calcium carbonate 英[ˈkælsiəm ˈkɑ:bəneit] 美[ˈkælsiəm ˈkɑrbəˌnet] n. 碳酸钙;

calcium carbonate[英][ˈkælsiəm ˈkɑ:bəneit][美][ˈkælsiəm ˈkɑrbəˌnet]n.碳酸钙; 例句:1.In a computer simulation, the oc-17 protein acted as a catalyst to kickstart the formation of crystals that make up an eggshell by clamping itself on to calcium carbonate particles. 在计算机模拟中，蛋白质oc-17类似于一种催化剂，通过作用于碳酸钙，促进了构成蛋壳的晶体的形成。