Chondrite-normalization

A few REE data on hydrothermal solutions are available (Fig. 2.34). Chondrite normalized REE patterns of hydrothermal solutions from Vienna Wood, Pacmanus and Desmos, Manus Basin exhibit positive Eu anomaly and LREE enrichment are similar to midoceanic ridge solution and Kuroko ore fluids. This positive Eu anomaly (Fig. 2.35) may have been caused by the selective leaking of Eu due to the interaction of an ascending hydrothermal solution and footwall volcanic rocks (Gena et al., 2001). It is interesting to note that altered basaltic andesite has a negative Eu anomaly and this feature is the same as that found in the Kuroko mine area (Shikazono, 1999). 

Chondrite-normalized REE patterns were based on values by Evensen et al. (1978) averaging the samples firstly determined in ppm for each site. 

Fig. 3. Total alkalis versus silica (TAS) and (b) AFM plot of Irvine and Baragar (1971), (c) modified Zr/Ti02-Nb/Y plot (Pearce, 1996) of Winchester and Floyd (1977), (d) Rock/chondrite-normalized REE diagram for rocks of amli-llica pluton and (e) rock/MORB-normalized spidergrams, (f) Th/Yb vsTa/Yb diagram.

Figure 9.9 REE abundances from archaeological glass, showing the effect of chondrite normalization, (a) shows the raw abundances of the REE measured on a set of English medieval window glasses, with the saw-tooth pattern evident, and little indication of differences between any of the samples (apart from perhaps one which has lower overall REE concentrations), (b) shows the same data normalized to the chondrite data (Table 9.1). The saw-tooth has largely disappeared, and close inspection suggests that two samples have a positive europium anomaly, possibly indicating a different geographical origin.

Table 3.9. Chondrite-normalized Ce/Yb ratio of some recent lavas of the Pit on de la Fournaise, Reunion Island (Albarede and Tamagnan, 1988).

The Piton de la Fournaise volcano (Indian Ocean) erupts basalts with chemical compositions that change with time. The rare-earth elements have been measured on eight dated historic lavas (Table 3.9 and Figure 3.7, Albarede and Tamagnan, 1988), and chondrite-normalized (Ce/Yb)N ratios over the time interval 1948-1985 are given in Table 3.9. Calculate an annual interpolation of these results. 

The mafic to intermediate and tholeiitic to transitional rocks of the Bousquet Formation are characterized by moderately enriched chondrite-normalized LREE and MREE patterns, flat HREE profiles and negative Nb, Ta, Zr, and Hf... 

Figure 2. Chondrite-normalized REE-HFSE diagram of Archean F-type rhyolites against the pattern of the LaRonde host felsic rocks. From Mercier-Langevin ef a/.. 2007b).

Chondrite-normalized REE patterns show that all types of dykes are depleted in HREE relative to LREE (Fig. 5). Also dykes display high SrA (ave. 86 ppm) and La/ Yb (up to 80 ppm) ratios. 

Fig. 5. Cl chondrite-normalized REE patterns showing the low HREE relative to LREE, suggesting a garnet-bearing and plagioclase-free source, as well as an adakitic-geochemical composition.

Chondrite-normalized REE profiles (Fig. 1) for massive sulfides exhibit a prominent enrichment in LREE and Eu. The enrichment of LREE over the HREE is substantiated by strong positive REE correlations with La, Ce, Pr, Nd and Sm, and a (La/Lu)N ranging widely from 0.15 to 387. Europium anomalies are distinctly positive with (Eu/Eu )n averaging 4.7, but vary widely, ranging from 0.21 to 36. Minor negative Eu anomalies occur in semi-massive sulfides, due to dilution by volcaniclastic material. A positive... 

Chondrite-normalized REE profiles (Fig. 3) display a distinct enrichment in LREE with prominent negative Eu anomalies, which are broadly consistent with known profiles of monazite in metamorphosed terrains (Spear Pyle 2002). The LREE contents of monazite have fairly restricted compositions dominated by Ce averaging 29.8% Ce203 and behaving sym-... 

Fig. 3. Chondrite-normalized REE profiles for phosphate minerals in massive sulfides, BMC.

Selandian Rb-Sr ages of 59.6 2.8 Ma and 60.3 0.8 Ma were determined for the K1A and K19 bodies, respectively these bodies occur in the southwestern part of the field and are either barren of diamond or have the poorest diamond results within this field (Hood McCandless 2004 Fig 1). Mineralogical (e.g., amphibole, sanidine) and geochemical evidence (e.g., flatter chondrite-normalized REE pattern versus the steep profile of typical kimberlite) enticed Eccles et al. (2008) to conclude that these rocks are better referred to as hybrid kimberlite-ultrabasic rocks. 

Fig. 3. Chondrite-normalized mean REE patterns of different generations of uranium oxides from the Millennium (square) and Eagle Point (triangle) deposits with their corresponding U-Pb isotopic age.

The chondrite-normalized REE patterns for basement-hosted uranium oxides are similar, except for a small variation of LREE abundances, indicating identical physico-chemical deposition conditions (T, pH, fluid composition) for the Eastern part of the Athabasca Basin basement. The previous REE distinction made between Ingress and Egress deposits (Fayek Kyser 1997) is not confirmed by the present study, because both types have similar REE abundance and fractionations, indicating the similarity of the sources and the processes for both deposit types. Thus, these results suggest... 

Fig. 2. Chondrite-normalized REE spectra measured on U-minerals of Cage district.

Chondrite-normalized major and REE host felsic volcanic rocks from various in the TCZ. 

Fig. 3. Correlations of )TREE and chondrite normalized La/Yb ratios with P2O5 for the HQ leachates and residues of the basalt samples.

Elemental abundances in CR2 chondrites normalized to the Cl composition and plotted in order of decreasing volatility from left to right. Lithophile elements are shown with open circles, siderophile elements with black circles, and chalcophile elements with gray circles. CR2 data from Kallemeyn etal. (1994). 

Volatile element abundances in CV chondrites (normalized to Cl chondrites and silicon) lie along a linear array on semi-log plots versus their 50% condensation temperatures. This depletion pattern persists, whether the elements are siderophile, lithophile, or chalcophile. 

Rare earth element patterns for basalt and chondrite, and the chondrite-normalized basalt REE pattern. Normalization removes the zigzag pattern due to differences in odd and even atomic number abundances. The europium (Eu) anomaly in the normalized pattern is due to incorporation of extra plagiodase. 

Bulk compositions of H, L, and LL chondrites normalized to Cl abundances. Elements are plotted in order of decreasing volatility from left to right. Lithophile, siderophile, and chalcophile elements are designated with open, black, and gray symbols, respectively. These diagrams reveal fractionation of these element groups among different ordinary chondrite classes. Data from Kallemeyn et al. (1989). 

Chondrite-normalized element/silicon ratios measured in chondritic porous IDPs. Cl chondrite ratios are shown by the vertical dashed line. Modified from Schramm et al. (1989). 

Mean compositions of tracks and crater residues produced by Stardust particles, compared to Cl chondrite ratios (horizontal lines), (a) Fe- and Cl chondrite-normalized composition determined by averaging 23 track analyses by SXRM (filled squares), (b) Si- and Cl- chondrite-normalized composition of seven crater residue analyses by SEM-EDX (filled squares), and TOF-SIMS analyses for five craters (open squares). Modified from Flynn et al. (2006). 

Figure 12.17a shows lithophile element abundances, and Figure 12.17b shows sid-erophile and chalcophile element abundances in CM chondrites, normalized to Cl chondrites. Illustrated for comparison are the abundances in CO chondrites, which are the anhydrous carbonaceous chondrite group most closely allied to CM chondrites. As in other chondrites, the greatest differences are in volatile elements. The volatile and moderately volatile elements in CM chondrites are present at 50-60% of the abundances of the refractory elements. The volatile elements are primarily located in the matrix, and the matrix comprises 50-60% of CM chondrites. This implies that the matrix has essentially Cl abundances of all elements, while the chondrules and refractory inclusions have Cl relative abundances of refractory elements but are highly depleted in the volatile elements. The sloping transition in the region of moderately volatile elements indicates... 

Chondrite-normalized abundances of siderophile elements in the Earth s mantle. The measured concentrations do not match those expected from low-pressure metal-silicate partition coefficients determined by experiments. Modified from Tolstikhin and Kramers (2008). 

Figure 3, Chondrite-normalized rare earth element patterns of soapstone samples from quarries in the Mbe-marle-Nelson County regions of Virginia and in Crete. For the Albemarh-Nelson quarries f — the two lines give the range of 12 samples analyzed, and for the Crete samples (O — O) the two lines define the range of 19 samples. Two artifacts made of soapstone from the Albemarle-Nelson quarries are shown. One — M) is a pot from a habitation site in Cherokee County, NC and the other (A-- A) a pot from a habitation site near the quarry in Buckingham County, VA.

Figure 5. Chondrite-normalized REE patterns for some soapstone outcrops along the eastern U,S. Piedmont. The source is indicated by the abbreviation of the state. The Md. sample is from Ednor quarry, Montgomery County, MD Va. is from the Albemarle-Nelson County, VA quarry Pa. (A) and (B) are representative of the two types of samples from outcrops in Lancaster and Chester Counties, PA N.C. is from an outcrop in Watuga County, NC R.L is from Oaklawn, RI and Mass, is from Westfield, Mass.

Figure 12. Chondrite-normalized REE patterns from quarries and artifacts in Labrador and Newfoundland. Sample N is from the Fleur-de-Lys quarry on the east coast of Newfoundland L from an outcrop near the Viking habitation site at Vanse aux Meadows in northern Newfoundland F from soapstone outcrops in the Freestone Harbor region and M from outcrops of Moore s and Okak Islands on the central Labrador coast. Both E and A are artifacts which represent a group of artifacts having similar REE patterns but for which no quarry of origin has been found.

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