Host-influenced geochemical signature in the parasitic foraminifera Hyrrokkin sarcophaga

Hyrrokkin sarcophaga is a parasitic foraminifera that is commonly found in cold-water coral reefs where it infests the file clam Acesta excavata and the scleractinian coral Desmophyllum pertusum (formerly known as Lophelia pertusa). Here, we present measurements of the trace element and isotopic composition of these parasitic foraminifera, analyzed by inductively coupled optical emission spectrometry (ICP-OES), electron probe microanalysis (EPMA) and mass spectrometry (gas-source MS and inductively-coupled-plasma MS).

Our results reveal that the geochemical signature of H. sarcophaga depends on the host organism it infests. Sr $/$ Ca ratios are 1.1 mmol mol⁻¹ higher in H. sarcophaga that infest D. pertusum, which could be an indication that dissolved host carbonate material is utilized in shell calcification, given that the aragonite of D. pertusum has a naturally higher Sr concentration compared to the calcite of A. excavata. Similarly, we measure 3.1 ‰ lower δ¹³C and 0.25 ‰ lower δ¹⁸O values in H. sarcophaga that lived on D. pertusum, which might be caused by the direct uptake of the host's carbonate material with a more negative isotopic composition or different pH regimes in these foraminifera (pH can exert a control on the extent of CO₂ hydration/hydroxylation) due to the uptake of body fluids of the host. We also observe higher Mn $/$ Ca ratios in foraminifera that lived on A. excavata but did not penetrate the host shell compared to specimen that penetrated the shell, which could be interpreted as a change in food source, changes in the calcification rate, Rayleigh fractionation or changing oxygen conditions.

While our measurements provide an interesting insight into the calcification process of this unusual foraminifera, these data also indicate that the geochemistry of this parasitic foraminifera is unlikely to be a reliable indicator of paleoenvironmental conditions using Sr $/$ Ca, Mn $/$ Ca, δ¹⁸O or δ¹³C unless the host organism is known and its geochemical composition can be accounted for.

1 Introduction

The foraminifera are a very diverse group of marine shelly organisms that are commonly used for paleoenvironmental reconstructions using the isotopic or elemental composition of their carbonate shell (Petersen et al., 2018; Hönisch et al., 2011; Gray and Evans, 2019; Lear and Rosenthal, 2006; Raddatz et al., 2017). They first appeared in the Cambrian (Culver, 1991) and, over the course of the Phanerozoic, occupied oceanic settings from coastal waters to the open ocean, as well as deep sea benthic habitats (Goldstein, 1999). Multiple feeding methods are known from foraminifera, including suspension feeding, grazing, predation and parasitic feeding (Hancock et al., 2015). The latter is probably the least common feeding mechanism among the foraminifera, with only 9 species that are known to be parasitic and a further 13 that are suspected to be (Walker et al., 2017). One of the known parasitic species is Hyrrokkin sarcophaga (Cedhagen, 1994), a common foraminifera in cold-water coral reefs in the NE Atlantic (Beuck et al., 2008). H. sarcophaga preferentially colonizes the file clam Acesta excavata but also other organisms such as the bivalve Delectopecten vitreus; sponges of the family Geodiidae and Ancorinidae; cold-water corals such as Desmophyllum pertusum (formerly known as Lophelia pertusa; Addamo et al., 2016), Madrepora oculata and Flabellum japonicum; and other foraminifera (Beuck et al., 2008; Cheng and Dai, 2016; Cedhagen, 1994). Besides biogenic hard substrates, H. sarcophaga can also be found settling on rocks, which shows that it can at least survive short periods without a host (Cedhagen, 1994). H. sarcophaga forms an attachment etching, i.e. mirroring its spiral outline on the host. From this depression the foraminifera etch a canal into the shell of the host (Cedhagen, 1994) (Fig. 1). This allows the foraminifera to feed on the bivalve host's tissue (Cedhagen, 1994) and possibly assimilate amino acids from its extrapallial calcifying fluid (Schweizer et al., 2012; Alexander and Delaca, 1987).

Figure 1 Fluorescence microscopic image (excitation 420–490 nm) and schematic figure of H. sarcophaga on A. excavata. A: H. sarcophaga; B: attachment depression corroded by H. sarcophaga; C: bored canal; D: callus built by A. excavata (SRZ: shell repair zone); E: undisturbed shell; E₁: calcitic shell layer (fibrous); E₂: calcitic shell layer (microgranular); E₃: aragonitic shell layer.

The bivalve reacts by building a callus (layered aragonite rich in organics) to seal this boring (Fig. 1D) and defend the organism from the parasite's attack (Beuck et al., 2008). In D. pertusum, borings into the inner calyx area were not observed (Beuck et al., 2008). Instead, multiple whip-shaped tunnels protrude into the coral's skeleton, which possibly serve an anchoring function (Beuck et al., 2008). The pit is possibly formed either as a way to protect itself from cleaning attempts of the host and increase attachment strength or to serve the foraminifera's need for calcium and/or DIC (dissolved inorganic carbon) (Beuck et al., 2008; Cedhagen, 1994).

As the parasitic foraminifera ingests material from its host, the question arises of whether this process exerts an influence on the shell geochemistry of the parasite. Should this be the case, this factor may need to be accounted for, especially as some parasitic foraminifera, such as Cibicides refulgens, are also used in geochemical studies for paleoenvironmental reconstructions (García-Gallardo et al., 2017; Mackensen and Nam, 2014; Rathburn and de Deckker, 1997; Raddatz et al., 2011; Alexander and Delaca, 1987).

Here, we present element-to-Ca ratios (Mg $/$ Ca, Sr $/$ Ca, Na $/$ Ca and Mn $/$ Ca) and stable isotope data (oxygen and carbon) analyzed in H. sarcophaga collected from different host organisms (A. excavata and D. pertusum) from the Trondheimsfjord (also known as Trondheim Fjord, Norway) to explore if and how the different hosts influence the geochemical composition of the test of foraminifera. In addition, we present element maps analyzed by electron microprobe analysis (EPMA) of the callus region of A. excavata in order to explore geochemical differences between the callus region and undisturbed shell areas.

2 Material and methods

2.1 Sampling

All investigated samples were collected in the Leksa Reef, located at the entrance to the Trondheimsfjord in Norway (63.613056^∘ N, 9.384167^∘ E; depth ∼ 200 m) by means of the manned submersible JAGO (GEOMAR Helmholtz-Zentrum für Ozeanforschung, 2017) during the scientific cruises POS473 and POS525 with RV Poseidon (Form et al., 2015; Büscher, 2018; GEOMAR Helmholtz-Zentrum für Ozeanforschung, 2015). In total we analyzed 30 specimens of H. sarcophaga, which were divided into three groups: (1) H. sarcophaga that infested A. excavata with callus formation (henceforth called HAW), (2) H. sarcophaga that infested A. excavata without callus formation (henceforth called HAO; HAW + HAO = HA) and (3) H. sarcophaga that infested D. pertusum (henceforth called HL). Samples of A. excavata and D. pertusum were alive when sampled. We cannot be entirely certain that H. sarcophaga were still alive when sampled, but upon death they easily become detached from the shell, whereas in our samples the foraminifera were still firmly attached. For ICP-OES, ICP-MS and GS-MS, the samples were ultrasonically rinsed in deionized water for 5 min and allowed to dry before crushing in an agate mortar

2.2 Shell carbonate polymorph

The polymorph of the foraminiferal shell was determined using cobalt nitrate solution (Meigen solution). The foraminifera samples were crushed in an agate mortar and transferred to Eppendorf containers. The samples were mixed with 10 wt % Co(NO₃)₂ aqueous solution and allowed to react at 95 ^∘C for 20 min. Afterwards the samples were washed four times with deionized water and inspected under a KEYENCE VHX-S660E microscope. Aragonite stains purple/pink in cobalt nitrate solution, whereas calcite remains unaffected (Kato et al., 2003)

2.3 Fluorescence microscopy

We used fluorescence microscopy to investigate the distribution of the organic material in the foraminifera and the underlying bivalve shell. The sample was cut, ultrasonically cleaned in deionized water, embedded in epoxy resin (Araldite 2020) and polished with 3 µm diamond-lapping paste. Fluorescent images were taken using a Leica DMRX-POL microscope with fluorescent front light and a 50 W mercury lamp. The microscope was equipped with an H3 filter cube, which excites in the wavelength range of blue to violet (bandpass filter: 420–490 nm). The pictures were taken with a digital camera connected to the microscope with 0.25 s exposure time.

2.4 EPMA

Two samples of A. excavata with attached H. sarcophaga were analyzed by electron probe microanalysis (EPMA). The area of interest was cut from the shell with a handheld drilling tool, ultrasonically cleaned in deionized water for 5 min, mounted vertically into circular mounts and embedded in epoxy resin (Araldite 2020). The sample surface was ground with a 9 µm grid with silicon carbide sanding paper and then polished using 3 µm diamond-water-based lapping paste. After polishing the samples were coated with carbon.

The EPMA analyses were conducted at the Goethe University Frankfurt on a JEOL JXA-8530F Plus field emission gun electron probe microanalyzer (FEG-EPMA). The analysis conditions were 15 kV acceleration voltage and 20 nA current with a beam diameter of 3 µm. We used a TAP crystal for Mg, TAPL for Na and Sr, and PETH for S. Detection limits are calculated with the equation given in Goldstein et al. (2018) and amount to Mg = 178 µg g⁻¹ (Mg $/$ Ca = 0.7 mmol mol⁻¹), Na = 170 µg g⁻¹ (Na $/$ Ca = 0.7 mmol mol⁻¹), Sr = 129 µg g⁻¹ (Sr $/$ Ca = 0.1 mmol mol⁻¹), S = 152 µg g⁻¹ (S $/$ Ca =  0.4 mmol mol⁻¹) and Ca = 195 µg g⁻¹. Molar ratios were calculated from the weight fractions of the specific oxides (CaO, MgO, Na₂O, SrO, SO₃) by calculating the concentration of the observed elements (in µg g⁻¹) and normalization to Ca accounting for their relative atomic mass. The chemical maps were recorded with a beam diameter of 2 µm, 15 kV acceleration voltage and 20 nA current.

2.5 ICP-OES

For ICP-OES measurements we used 10 HAW, 10 HAO and 10 HL samples. About 120 µg of sample powder was transferred to Eppendorf tubes (acid cleaned with 5 % HNO₃) and sealed. Each sample was analyzed three times.

Elemental ratios Mg $/$ Ca, Sr $/$ Ca, Na $/$ Ca and Mn $/$ Ca (only for foraminifera and bivalves) were analyzed by inductively coupled plasma–optical emission spectrometry (ICP-OES). ICP-OES analysis was carried out using a Thermo Scientific iCap 6300 Duo at the Institute of Geosciences, Goethe University Frankfurt. The sample powder (≈ 140 µg) was dissolved in 500 µL HNO₃ (2 %), and 300 µL aliquots were separated. Subsequently 1500 µL of 1.2 mg L⁻¹ yttrium solution was added to each aliquot as an internal standard resulting in a concentration of Y = 1 mg L⁻¹ and Ca = 25 mg L⁻¹. The intensity data were background corrected, standardized internally to Y and normalized to Ca. Accuracy is reported in percent deviation from values of standard reference material JCP1 and USGS MACS-3 (n = 5) (Jochum et al., 2005) and is better than 1 % for Mg $/$ Ca and Sr $/$ Ca, 5 % for Na $/$ Ca, and 3 % for Mn $/$ Ca. Precision is reported in relative standard deviation; percent RSD (relative standard deviation) of the USGS MACS-3 and JCP1 carbonate reference material (n = 5) (Jochum et al., 2005) is better than 3 % for all analyzed elements.

Bivalve (n = 3) and coral (n = 3) samples were treated similarly to foraminifera samples. We took 15–20 samples per shell from the outermost shell section along the main growth axis, starting at the ventral margin resulting in a total of 49 samples. The corals were sampled randomly over the whole calyx area, resulting in 44 samples.

2.6 ICP-MS

The manganese concentration of D. pertusum had to be determined by ICP-MS because it was below the limit of detection by ICP-OES. We used three specimens (two from the Leksa Reef and one from the Sula Reef), of which we sampled 150 µg from the fibrous shell section. Each sample was measured twice.

For solution-based ICP-MS measurements we used 150 µg of sample powder and dissolved it in 500 µL 2 % HNO₃. The dissolved sample (300 µL) was mixed with 1500 µL 1.2 mg L⁻¹ yttrium solution, which was used as the internal standard. The reference material ECRM 752-1 (Greaves et al., 2008) was used to monitor measurement precision and accuracy, reported in percent deviation from the reported values of the standard reference material ECRM 752-1 (n = 3) (Greaves et al., 2005), and equals 7 % for this analytical session. Precision is reported in relative standard deviation; percent RSD of the ECRM 752 carbonate reference material (n = 3) is better than 1 % for Mn $/$ Ca.

2.7 Stable oxygen and carbon isotopes

We used 9 HAW, 9 HAO and 10 HL for stable isotope measurements. About 100 µg of sample powder was transferred to borosilicate glass tubes and sealed with plastic caps. Each sample was measured three times.

Stable isotopes were measured at Goethe University Frankfurt on a Thermo MAT 253 mass spectrometer interfaced with a Thermo Fisher Scientific GasBench II. The sample material (100 µg) was reacted with 99 % H₃PO₄ at 72 ^∘C in continuous flow mode. Analytical procedures followed Spótl and Vennemann (2003). δ¹³C and δ¹⁸O values are reported in δ notation, i.e. per mille deviation relative to Vienna Pee Dee Belemnite (VPDB) and Vienna Standard Mean Ocean (VSMOW), respectively. Internal precision is better than 0.06 ‰ (δ¹³C) and 0.08 ‰ (δ¹⁸O).

Samples of the ambient water were collected during scientific cruise POS525 with R/V Poseidon in July 2018 (Büscher, 2018; GEOMAR Helmholtz-Zentrum für Ozeanforschung, 2015). A rosette sampler equipped with conductivity, temperature and depth sensors (CTD, Sea-Bird Scientific, SBE 911 Plus) was used to sample water from the investigated reefs. The water samples were transferred from 12 L Niskin bottles to 250 mL borosilicate bottles and sealed after adding 100 µL HgCl₂ to prevent biological activity of microorganisms that may alter the isotopic composition. The samples were stored in a fridge at 4 ^∘C until measurement.

Water samples were analyzed for their isotopic composition at Friedrich-Alexander-Universität Erlangen-Nürnberg by an automated equilibration unit (GasBench II; Thermo Fisher Scientific) coupled in continuous flow mode to a Delta Plus XP isotope ratio mass spectrometer (Thermo Fisher Scientific, Bremen, Germany).

Water for δ¹³C analyses was extracted from the sample bottles by a 1 mL disposable syringe through the septa without opening the bottle to avoid loss of CO₂ during sample transfer. During water extraction, the removed volume was simultaneously replaced by inert gas through a second needle connected to an argon-filled gas sampling bag (Grace, Deerfield, IL, USA). The samples were injected into 12 mL Labco Exetainers™ (Labco Ltd., Lampeter, UK) that were prepared with phosphoric acid and pre-flushed with helium (purity 99.999 %). For seawater the injection volume was 0.85 mL per vial. Samples were analyzed in duplicates, and the reported values are arithmetic means. All values are reported in the standard δ notation in per mille (‰) vs. VPDB.

Sample bottles for δ¹⁸O were de-capped, and 0.5 mL water was extracted with a pipette for CO₂ equilibration. The samples were transferred into 12 mL Labco Exetainers™ (Labco Ltd. Lampeter, UK) and subsequently flushed with 0.3 % CO₂ in helium. Equilibration time was 24 h at 25 ^∘C. All samples were measured in duplicates, and the reported values are arithmetic means. All values are reported in the standard δ notation in per mille (‰) vs. VSMOW. External reproducibility based on repeated analysis of control samples was better than 0.1 ‰ and 0.05 ‰ for δ¹³C and δ¹⁸O, respectively.

2.8 Statistical computation

We used one-way ANOVA to test the effect of the host species on the elemental and isotopic composition in H. sarcophaga. The Shapiro–Wilk test and Levene's test were used to ensure normal distribution and equal variance of the target variables. Most groups and target variables are normally distributed except for Na $/$ Ca in the HAO group and δ¹⁸O in the HL group. All target variables except for Mn $/$ Ca and Sr $/$ Ca show equal variance based on the Levene's test. Normal distribution and equal variance are considered a prerequisite for ANOVA. As these prerequisites are not met in some sample groups, we additionally tested the data with a Kruskal–Wallis test, which is a non-parametric alternative to ANOVA (Lantz, 2013). Pairwise comparison of the different groups was accomplished with Bonferroni-adjusted Tuckey honest significant difference (HSD) test. To test the relationship between different variables we used a linear regression model fitted with ordinary least squares (OLS). All reported p values are Bonferroni adjusted. Some measurements could be considered outliers, based on the interquartile range (IQR); Q1 − 1.5 × IQR and Q3 + 1.5 × IQR. However, we have not truncated these measurements because most of them are just slightly outside the range mentioned above. Only one measurement shows a high deviation, but keeping it in the dataset does not change the outcome of the analysis.

3 Results

3.1 Carbonate polymorph

The investigated H. sarcophaga samples show no staining (Supplement file S1) under the influence of cobalt nitrate solution. Consequently, the shells are calcitic.

3.2 Fluorescence microscopy

The fluorescence microscopic image of H. sarcophaga attached to A. excavata (Fig. 1) shows distinct fluorescent and non-fluorescent layers in the shell repair zone (SRZ) of the bivalve. Highly fluorescent material is also observable on H. sarcophaga, especially in the test apertures.

The SRZ has a maximum thickness of 900 µm, decreasing in all directions. The fluorescent layers in the SRZ are 20–40 µm thick. These layers taper off distally from the bore canal and disappear. Non-fluorescent layers are generally smaller, ranging from 9–20 µm. The asymmetric pit that is produced by the foraminifera is observable – one side of the pit is rising steeply, whereas the other side has a shallower angle. The bore canal, which starts at the bottom of the attachment etching, is 400 µm long in the undisturbed bivalve shell but continues in the callus by another 240 µm. At the start of the bore the canal it is 340 µm in diameter and continuously narrows to 140 µm. The canal ends in the SRZ with a mushroom-like shape.

3.3 Element composition of point measurements (EPMA)

Within the bivalve shell Mg $/$ Ca varies between 0.2 and 13.7 mmol mol⁻¹ (Fig. 2). The lowest values were found in the aragonitic shell layer (Fig. 1E₃) and the highest values are measured in the microgranular calcitic shell layer (Fig. 1E₂). The highest Mg $/$ Ca ratios are measured in the foraminiferal calcite (mean = 45.0 ± 17.9 mmol mol⁻¹, maximum = 80.6 mmol mol⁻¹).

Figure 2 Results of point measurements by EPMA in different sections of A. excavata and H. sarcophaga (two specimens each). (a) Mg $/$ Ca, (b) Na $/$ Ca, (c) Sr $/$ Ca and (d) S $/$ Ca. Boxes display the interquartile range (IQR) and lines the median values. The whiskers show minimum and maximum values that are within the range of Q1 − 1.5 × IQR – Q3 + 1.5 × IQR. Red circles show the mean values. Sample size = 11, 5, 17 and 16 (calcite, aragonite, SRZ, H. Sarcophaga). Text below the horizontal lines in the legend is the sampled area.

The Na $/$ Ca ratio is characterized by similar values in the different sections when considering the carbonate polymorph, which it is built out of. The aragonitic sections (Fig. 1E₃), bivalve aragonite and SRZ have mean Na $/$ Ca ratios of 22.0 ± 2.3 mmol mol⁻¹ (mean ± SD) and 25.3 ± 3.8 mmol mol⁻¹ respectively. The SRZ displays a higher variability than the undisturbed aragonite. The microgranular calcite is characterized by a mean Na $/$ Ca of 14.8 ± SD = 3.7 mmol mol⁻¹ (Fig. 1E₂).

The SRZ is enriched in Sr $/$ Ca compared to the undisturbed shell sections. Mean ratios are nearly 4 times higher than in the undisturbed aragonitic shell parts (5.9 ± 2.1 mmol mol⁻¹ compared to 1.5 ± 0.2 mmol mol⁻¹). The lowest values are measured in the bivalve's microgranular calcite (mean = 0.9 ± 0.1 mmol mol⁻¹).

S $/$ Ca ratios are comparable in the undisturbed bivalve aragonite and microgranular calcite, with 1.9 ± 0.3 mmol mol⁻¹ and 2.1 mmol mol⁻¹ ± 0.8 mmol mol⁻¹, respectively. Similar to Sr $/$ Ca, the highest mean and maximum S $/$ Ca ratios are measured in the SRZ (mean = 3.8 ± 2.5 mmol mol⁻¹, maximum = 11.1 mmol mol⁻¹). However, all these differences are insignificant (Table 1).

Table 1 Wilcoxon–Mann–Whitney test results of E $/$ Ca comparison between the observed shell sections. Bold fields show significant differences between the two groups. p values are Bonferroni adjusted.

Elemental composition of the SRZ

As also visible in the fluorescence image (Fig. 1), the EPMA chemical maps show a layering pattern (Fig. 3). Highly fluorescent layers that coincide with Mg and S maxima and Ca minima are variable in size, ranging from 15 to 80 µm in thickness. Non-fluorescent layers that coincide with Mg and S minima and Ca maxima are more uniform in size, ranging from 12.5 to 30 µm in thickness. Mean composition of the fluorescent (fl) and non-fluorescent (nfl) layers, based on EPMA point measurements amount to the following: fl – Mg $/$ Ca = 3.8 ± 1.7 mmol mol⁻¹, Sr $/$ Ca = 7.4 ± 1.2 mmol mol⁻¹, Na $/$ Ca = 24.4 ± 5.4 mmol mol⁻¹ and S $/$ Ca = 5.5 ± 2.7 mmol mol⁻¹; nfl – Mg $/$ Ca = 3.2 ± 1.8 mmol mol⁻¹, Sr $/$ Ca = 4.6 ± 1.9 mmol mol⁻¹, Na $/$ Ca = 26.6 ± 1.3 mmol mol⁻¹ and S $/$ Ca = 2.3 ± 0.9 mmol mol⁻¹. Significant mean differences between fluorescent and non-fluorescent layers, based on Wilcoxon–Mann–Whitney test, are evident with regards to the S $/$ Ca (p < 0.001) and Sr $/$ Ca ratios (p=0.006).

Figure 3 EPMA element maps and secondary-electron image from a scanning electron microscope (SEM) image of the callus area of two specimen (a, b) of A. excavata. Intensity scale in counts per second (cps). Minimum–maximum counts amount to Mg (10–24 cps), Na (76–132 cps) Ca (7600–8650 cps) and S (8.5–33 cps).

Figure 4 Elemental composition of the SRZ divided according to their fluorescence. Linear correlations are shown for both layers with 95 % confidence intervals in gray. Correlations are calculated with a linear regression model with OLS.

Mg $/$ Ca and S $/$ Ca as well as Na $/$ Ca and S $/$ Ca display significant correlations in the fluorescent layers (Fig. 4). In the non-fluorescent shell layers, Mg $/$ Ca and S $/$ Ca, Sr $/$ Ca and S $/$ Ca are significantly correlated. In both layers, S $/$ Ca ratios are inverse correlated with Ca wt % (Fig. 4).

3.4 Stable carbon and oxygen isotope

The different H. sarcophaga shells exhibit differences in their isotopic composition based on their host organism (Fig. 5e, f). In particular, δ¹⁸O values are similar in HL and HA with +1.51 ± 0.22 ‰ and +1.80 ± 0.25 ‰, respectively. These values are in accordance with δ¹⁸O values from the host organism A. excavata, which range from +1.52 ‰ to +2.1 ‰. D. pertusum displays more depleted δ¹⁸O and δ^13CC values, ranging from −1.93 ‰ to +0.54 ‰ and −9.41 ‰ to −3.30 ‰.

Larger differences between the different H. sarcophaga samples are observable in the carbon isotopic signature of specimens taken from different host organisms. HA display δ¹³C values of −0.43 ± 0.47 ‰, which is close to the ratios of their host organism, being +0.49 ± 0.28 ‰. HL are more depleted in heavy carbon isotopes with a measured value of −3.61 ± 0.71 ‰. For reference, the isotopic composition of the ambient seawater is δ¹⁸O = +0.26 ‰ and δ¹³C = +0.38 ‰.

The isotopic composition of HAW and HAO can be described by linear functions, whereas the isotopic composition in HL cannot:

$$\begin{array}{}\text{(1)}& {\displaystyle }\begin{array}{rl}& {{\mathit{\delta }}^{\mathrm{13}}\mathrm{C}}_{\mathrm{HAW}}=\mathrm{1.8}\pm \mathrm{0.4}\times {\mathit{\delta }}^{\mathrm{18}}\mathrm{O}-\mathrm{3.4}\pm \mathrm{0.8}\\ & (r^{\mathrm{2}}=\mathrm{0.7},p=\mathrm{0.004},\mathrm{df}=\mathrm{7}),\end{array}\text{(2)}& {\displaystyle }\begin{array}{rl}& {{\mathit{\delta }}^{\mathrm{13}}\mathrm{C}}_{\mathrm{HAO}}=\mathrm{1.1}\pm \mathrm{0.3}\times {\mathit{\delta }}^{\mathrm{18}}\mathrm{O}-\mathrm{2.6}\pm \mathrm{0.6}\\ & (r^{\mathrm{2}}=\mathrm{0.6},p=\mathrm{0.02},\mathrm{df}=\mathrm{6}),\end{array}\text{(3)}& {\displaystyle }\begin{array}{rl}& {{\mathit{\delta }}^{\mathrm{13}}\mathrm{C}}_{\mathrm{HL}}=\mathrm{1.7}\pm \mathrm{1.0}\times {\mathit{\delta }}^{\mathrm{18}}\mathrm{O}-\mathrm{6.2}\pm \mathrm{1.5}\\ & (r^{\mathrm{2}}=\mathrm{0.18},p=\mathrm{0.12},\mathrm{df}=\mathrm{8}).\end{array}\end{array}$$

3.5 ICP-OES results from H. sarcophaga grown on different host organisms

H. sarcophaga samples from different host organisms are similar in their chemical composition with regard to Mg $/$ Ca and Na $/$ Ca (Fig. 5a, b). Mean Mg $/$ Ca ratios range from 42.7 ± 6.8 to 44.4 ± 7.2 mmol mol⁻¹. Both host organisms have lower mean Mg $/$ Ca ratios of 4.3 ± 1.5 and 18.9 ± 4.5 mmol mol⁻¹ in D. pertusum and A. excavata, respectively.

Figure 5 Box and whisker plots displaying the E $/$ Ca (ICP-OES and ICP-MS) and stable isotope analysis (MS) of the investigated specimens. Boxes display the interquartile range and lines the median values. The whiskers show minimum and maximum values that are within the range of Q1 − 1.5 × IQR to Q3 + 1.5 × IQR. Red circles show mean values. Lines in panels (e) and (f) show the isotopic composition of the ambient seawater. Text below the horizontal lines in the legend is the host organism that H. sarcophaga grew on.

Mean Na $/$ Ca ratios range between 15.4 ± 2.1 and 17.6 ± 4.3 mmol mol⁻¹ for H. sarcophaga. The highest Na $/$ Ca ratios and variations are measured in HAO. D. pertusum displays overall higher Na $/$ Ca ratios than H. sarcophaga (26.3 ± 2.8 mmol mol⁻¹). The highest variation is measured in A. excavata, ranging from 9.8 to 55.6 mmol mol⁻¹ with a mean of 19.8 ± 7.3 mmol mol⁻¹.

A clear difference in Sr $/$ Ca of 1.1 ± 0.16 mmol mol⁻¹ is evident between H. sarcophaga from the different host organisms (Fig. 5c). HAW and HAO show mean Sr $/$ Ca ratios of 2.4 ± 0.2 and 2.1 ± 0.5 mmol mol⁻¹, respectively. The host organism A. excavata has lower Sr $/$ Ca ratios (1.2 ± 0.1 mmol mol⁻¹). On the contrary, HL and D. pertusum, display higher mean Sr $/$ Ca ratios of 3.5 ± 0.7 and 10.13 ± 0.3 mmol mol⁻¹ respectively.

Prominent differences between H. sarcophaga groups are also evident in their Mn $/$ Ca ratios (Fig. 5d). HAW, HL and D. pertusum display Mn $/$ Ca ratios of 0.017 ± 0.01, 0.012 ± 0.008 and 0.008 ± 0.001 mmol mol⁻¹, whereas HAO and A. excavata show higher Mn $/$ Ca ratios of 0.077 ± 0.03 and 0.13 ± 0.03 mmol mol⁻¹, respectively.

3.6 Compositional differences in H. sarcophaga related to their host organism

We conducted a one-way ANOVA and Kruskal–Wallis test (Table 2) in order to explore if the investigated H. sarcophaga groups (HAW, HAO, HL) show significant differences in their geochemical composition related to their host organism. We used the measured elemental and isotopic composition as target variables and the host organisms (A. excavata with callus, A. excavata without callus, D. pertusum) as the factor variable. Tukey HSD (Table 3) was used as post hoc test to investigate group-specific mean differences.

Table 2 Results of the one-way ANOVA and Kruskal–Wallis analysis with the host organism as predictor variable. Bold fields show elemental and isotopic ratios in H. sarcophaga that may be significantly influenced by the chemistry of the host organism. p values are Bonferroni adjusted, DFn signifies degrees of freedom in the numerator, and DFd signifies degrees of freedom in the denominator.

Table 3 Tukey-HSD test results. Bold fields show significant differences between the two groups. HAW represents H. sarcophaga that infested A. excavata with callus formation, HAO 0 H. sarcophaga that infested A. excavata without callus formation, and HL represents H. sarcophaga that infested D. pertusum. p values are Bonferroni adjusted.

The one-way ANOVA reveals no significant difference in the Mg $/$ Ca and Na $/$ Ca ratios of the foraminifera that were collected from the different host organisms (Table 2). In contrast, the ANOVA suggests a significant difference between Sr $/$ Ca and Mn $/$ Ca ratios between these two groups. In the case of Sr $/$ Ca, significant differences based on the Tukey-HSD post hoc test are observable between HL and HA, whereas we find no significant differences between HAW and HAO. In addition, we observe no significant differences between HAW and HL in their Mn $/$ Ca composition, but significant differences are present between both these groups and HAO.

In the case of the stable oxygen isotope composition, we observe significant differences between H. sarcophaga specimens from different host organisms. The δ¹⁸O measured in HL is significantly lower than in HAO. Significant differences are also observable for δ¹³C ratios. Here, differences in the isotopic composition are detectable between HL and HA, with the latter showing a higher δ¹³C ratio.

The Kruskal–Wallis test, which was used as a non-parametric cross validation for the ANOVA test, shows the same results as the ANOVA test

4 Discussion

4.1 Mechanisms of etching and boring

The boring and etching of H. sarcophaga in A. excavata and D. pertusum can serve multiple purposes. The attachment etchings of foraminifera have been proposed to serve as an anchoring function and increase protection from predators and the hydrodynamic regime. Possibly, the foraminifera also dissolve the host's carbonate material to satisfy the calcium and/or DIC requirements of H. sarcophaga for the calcification of its shell (Cedhagen, 1994; Vénec-Peyré, 1996; Todd, 1965) rather than expending further energy to source Ca/DIC from the surrounding seawater (Fig. 6a).

Figure 6 Possible pathways of E $/$ Ca and isotopic signals into the foraminiferal calcite. (a) H. sarcophaga on A. excavata, (b) H. sarcophaga on D. pertusum. Blue areas represent the calcifying space, and orange areas represent mantle tissue in A. excavata (a) and organic layer (coenosarc/mucus) in D. pertusum (b). Uptake of seawater and free-floating particles (1), ingestion of host organic material (periostracum, coral tissue/mucus) (2), ingestion of dissolved carbonate material (3), ingestion of extracellular calcifying fluid (ECF) (4), ingestion of Mantle tissue (5), and ingestion of carbonate and organic material from the deposited callus (6). Scale bar is 100 µm. Please note that the calcifying space and organic layers are displayed enlarged for improved visibility. Actual size of the calcifying space amounts to 1–100 nm (Nakahara, 1991; Tambutté et al., 2007). The organic layer (coenosarc) is ∼ 25 µm in thickness (Tambutté et al., 2007).

The boring in A. excavata is presumably produced to access the soft body of the bivalve, indicated by the mantle damage in the vicinity of the boring (Cedhagen, 1994). Additionally, the foraminifera may benefit from ingesting the ECF of the bivalve, containing carbohydrates, proteins, glycoproteins, and amino acids and therefore constituting a valuable nutrient source (Yin et al., 2005). The ECF is also enriched in Ca and CO₂ compared to the ambient seawater, maybe providing additional ions for the calcification of H. sarcophaga (Crenshaw, 1972). Feeding on mantle fluids of bivalves by parasitic foraminifera is also supported by tracer experiments on C. refulgens (Alexander and Delaca, 1987). With D. pertusum as host, the foraminifera can access the coenosarc and underlying calcifying space of the coral without having to bore through the carbonate skeleton (Fig. 6b).

H. sarcophaga probably uses chemical etching, as indicated by the xenoglyph surface texture of the trace that changes in correlation with the host's microstructure (Beuck et al., 2008; Todd, 1965) A possible mechanism was investigated in the non-symbiotic benthic foraminifera Ammonia sp., which uses H⁺-ATPase to actively pump H⁺ ions out of their protoplasm to facilitate calcification (Toyofuku et al., 2017). This proton flux causes a pH decrease by up to 1.1 in a 100 µm wide zone around the foraminifera (Toyofuku et al., 2017). Similar effects are reported from excavating sponges. Cliona varians displays pH values as low as 5 in their filopodia during carbonate dissolution (Webb et al., 2019).

4.2 Sr $/$ Ca differences in H. sarcophaga related to the host organism

We observe significant differences in the Sr $/$ Ca and Mn $/$ Ca composition between H. sarcophaga from different host organisms.

HL show significantly higher Sr $/$ Ca ratios than HA. Given that this result is based on measurements from multiple individuals distributed across more than one host organism, we suggest that this is most likely a signal of the high Sr $/$ Ca aragonite precipitated from D. pertusum that is imprinted into the test of H. sarcophaga. By chemically corroding the attachment etching as well as by the penetrating boring and by taking up the resulting solutions, the foraminifera gains access to a pre-concentrated calcium carbonate solution from which it can precipitate its shell (Fig. 6). Naturally, the foraminifera would also reflect other characteristics of the host, such as the high Sr $/$ Ca ratio from the aragonite of D. pertusum (Raddatz et al., 2013; Schleinkofer et al., 2019). In agreement with the much lower Sr $/$ Ca ratios in calcite and aragonite in A. excavata (Schleinkofer et al., 2021) compared to the coralline aragonite, we do not observe such high Sr $/$ Ca ratios in HA. Still, the observed Sr $/$ Ca ratios in HA are higher by a factor of 2 than in the host organism. Since we do not observe differences between HAW and HAO, the Sr $/$ Ca surplus cannot be derived from the ingestion of organic material from within the shell cavity. We hypothesize that a possible further control is likely provided through the mixture of dissolved host CaCO₃ material and ambient seawater from which the foraminifera calcify, which is explored in more detail in the next section.

4.3 Mixing model

In order to further investigate the observed results, we created a simple two-component model to explore how the trace element chemistry of H. sarcophaga could change by delivery of ions to the calcification site that were derived from dissolution of the host organism. In this model we calculate changes in the foraminifera composition in dependence from an assumed calcification from a variable mixture of seawater and dissolved host carbonate material. We excluded the addition of the hosts calcifying fluid in the model because there are no data available for the chemical composition of the calcifying fluid of D. pertusum or A. excavata and because the model is intended only as an initial exploration of whether the geochemistry of H. sarcophaga can be explained by calcification from a mixture of seawater and dissolved host material. Furthermore, measurements of the chemical composition of the calcifying fluid of other bivalve species indicate that the composition is close to the composition of seawater (Wada and Fujinuki, 1976; Crenshaw, 1972).

The model calculates element $/$ Ca ratios based on calcite precipitation from a fluid that is derived from a mix of seawater (transported to the calcification site; see, e.g., Erez, 2003) and CaCO₃ dissolved from the host organism:

$$\begin{array}{}\text{(4)}& {{\displaystyle \frac{E}{\mathrm{Ca}}}}_{\mathit{Hyrrokkin}}={\displaystyle \frac{E_{\mathrm{SW}}+\frac{{\mathrm{10}}^R}{M_{\mathrm{Carb}}}\times \frac{{\frac{E}{\mathrm{Ca}}}_{\mathrm{Host}}}{\mathrm{1000}}}{{\mathrm{Ca}}_{\mathrm{SW}}+\frac{{\mathrm{10}}^R}{M_{\mathrm{Carb}}}}}\times D_E\times \mathrm{1000},\end{array}$$

where E_SW is the element concentration in seawater, E $/$ Ca_Host is the element $/$ Ca ratio in host carbonate (mmol mol⁻¹), Ca_SW is the calcium concentration in seawater (0.010 mol L⁻¹), D_E is the calcite–water distribution coefficient, M_Carb is the atomic mass of CaCO₃ (100.08 g mol⁻¹), and R is the log mixing ratio between carbonate and seawater (g L⁻¹).

Table 4 Parameters used in the proposed model to explore the effects of carbonate and water uptake of H. sarcophaga on the shell chemistry. Host element $/$ Ca ratios are derived from this study. $D_E^{\mathrm{1}}$ and $D_E^{\mathrm{2}}$ represent the distribution coefficient.

As we have no information about the amount of dissolved material and water that is taken up by H. sarcophaga, we modeled it over 6 orders of magnitude (log dissolved CaCO₃/seawater ratios of −4 to +2). The parameters used are reported in Table 4.

Figure 7 Results of model calculations with the parameters listed in Table 4 for the measured E $/$ Ca ratios. Text below the horizontal lines in the legend is the host organism that H. sarcophaga grew on. Independently of the mixing ratio of dissolved host CaCO₃ and ambient water, no differences of the geochemical signature are predictable in Mg $/$ Ca and Na $/$ Ca. On the contrary, Sr $/$ Ca and Mn $/$ Ca ratios are predicted to diverge at mixing ratios > 0.01 g CaCO₃ L⁻¹ seawater. Solid lines are produced with $D_E^{\mathrm{1}}$ for the calculation, and dotted lines are produced with $D_E^{\mathrm{2}}$ for the calculation (see Table 4). In panels (a) and (b), the different samples overlap each other.

Based on the model shown in Fig. 7, the Mg $/$ Ca and Na $/$ Ca ratios in H. sarcophaga are independent of the geochemical signature of the host it lived on, which is in agreement with our measurements. This is caused by the high concentration of these elements in the ambient seawater in comparison to the host's carbonate. The composition of the mixture is largely controlled by the addition of Ca, which is equal for both host organisms.

In contrast, the model predicts that, at high ratios of CaCO₃ derived from the host compared to the surrounding seawater, different Sr $/$ Ca and Mn $/$ Ca ratios should be observed between foraminifera living on different host organisms. The modeled Sr $/$ Ca ratios for HL are constant at 2.0 mmol mol⁻¹ independent from the mixing ratio (Fig. 7c). When the foraminifera dissolves aragonitic material of D. pertusum and this material is mixed with seawater, the resulting Sr $/$ Ca ratios in this solution do not change due to the aragonitic D_Sr being close to 1. Consequently, if the shell Sr $/$ Ca ratio in H. sarcophaga depends on calcite D_Sr and the Sr $/$ Ca ratio in the calcifying fluid of H. sarcophaga, the resulting Sr $/$ Ca ratio in HL is equivalent to a specimen that calcifies solely from seawater (specimen without a host). As the calcitic D_Sr is below 1 (Raitzsch et al., 2010; Mucci and Morse, 1983; Evans et al., 2015), the addition of dissolved material from A. excavata in the calcifying space results in decreasing Sr $/$ Ca ratios in the calcifying fluid and lower Sr $/$ Ca ratios in the precipitated calcite of the foraminifera. Similar results are obtained in the case of Mn $/$ Ca ratios. The addition of dissolved host material to the calcifying space of H. sarcophaga results in an increase in the Mn $/$ Ca ratio in the calcifying fluid, which leads to increasing Mn $/$ Ca ratios in the foraminiferal calcite.

The proposed model can help us understand why we do not see changes in the Mg $/$ Ca and Na $/$ Ca composition of H. sarcophaga from different host organisms and why Sr $/$ Ca and Mn $/$ Ca ratios differ between these groups (Fig. 2). Nonetheless, other processes are clearly required to explain the details of trace element uptake in H. sarcophaga. Sr $/$ Ca ratios in HL, for instance, can only be modeled up to 2 mmol mol⁻¹, whereas we measure a mean of 3.5 mmol mol⁻¹. The results of this model are largely driven by the distribution coefficients used; however, the distribution coefficients used in this model are not empirically determined on H. sarcophaga but derive from other foraminifera species ($D_E^{\mathrm{1}}$) or inorganic precipitation experiments ($D_E^{\mathrm{2}}$). The model also does not account for growth-rate-driven differences in trace element portioning, while this is especially relevant in the case of Na and Mn (Mucci, 1988; Füger et al., 2019). In addition, we have to consider lattice strain effects that increase the distribution coefficient for other elements such as Sr and Na, as H. sarcophaga has relatively high concentrations of Mg (Evans et al., 2015; Mucci and Morse, 1983).

As discussed above, this is a simplified model that uses seawater and dissolved carbonate as end-members. An additional possibility is that the foraminifera pumps or channels ions into and out of the calcifying fluid. In particular, it has been suggested foraminifera are able to transport Mg out of the calcifying space (Nehrke et al., 2013; Toyofuku et al., 2017; Bentov and Erez, 2006), but intermediate and high-Mg foraminifera such as A. lessonii appear to exert a lower degree of control over the composition of their calcifying fluid compared to low-Mg species (Evans et al., 2018; Geerken et al., 2018). Assuming the calcifying fluid is depleted in Mg in comparison to seawater, the model would predict lower Mg $/$ Ca ratios, although importantly it would still not predict a difference in the Mg $/$ Ca ratios of H. sarcophaga influenced by the host organism.

Another factor that should be considered is the transport pathway of the dissolved material into the foraminifera's calcifying fluid. The dissolution process of the host organism could modify the chemistry of the ambient seawater in a limited area around the foraminifera (Toyofuku et al., 2017), although this process is hard to imagine in an environment (cold-water coral reef) that relies on constant water movement to provide nutrients to the main inhabitants (Mienis et al., 2007). As such, we suggest it is more likely that the dissolved material is transported through the cytoplasm to the calcification site (Spero, 1988; Erez, 2003), although further work is required to confirm this.

4.4 Mn $/$ Ca differences in H. sarcophaga related to the host organism

Based on the ANOVA analysis (Table 2), significant differences are also observable in the Mn $/$ Ca ratios. HAO display 4-times-higher Mn $/$ Ca ratios than in the other two observed groups. HL show similar Mn $/$ Ca ratios as their host organism; both HAW and HAO show lower Mn $/$ Ca ratios. Based on the differences we observe between the samples that were picked from A. excavata, it is unlikely that the Mn $/$ Ca signal in H. sarcophaga derives from the host shell material (Fig. 6a3 and b3). In this case we would expect to see differences between HA and HL as Mn $/$ Ca in A. excavata is approximately 1 order of magnitude higher than in D. pertusum. Influences of the surrounding water cannot explain the observed differences either. Manganese, as a redox-sensitive element, is controlled by the oxygen concentration of the ambient water. Under well-oxygenated conditions, the main species Mn²⁺ is oxidized to Mn oxyhydroxides and precipitated (Calvert and Pedersen, 1996, 1993). Low-oxygen conditions lead to a reduction of Mn oxyhydroxides to the bioavailable Mn²⁺ and a consequent increase in Mn $/$ Ca ratios in biogenic carbonates (Tribovillard et al., 2006; Groeneveld and Filipsson, 2013; Koho et al., 2015). The Leksa Reef, however, is well oxygenated (Milzer et al., 2013; Jacobson, 1983).

An influence of the precipitation rate on the Mn $/$ Ca ratio was shown in inorganically precipitated calcite overgrowths and the planktic foraminifera Orbulina universa (Mucci, 1988; Lorens, 1981; Holland et al., 2017). Generally speaking, increased calcification rates cause Mn $/$ Ca ratios in the precipitates to decrease (Mucci, 1988; Holland et al., 2017). In our investigated samples, this effect would imply lower calcification rates in HAO compared to HAW and HL. The possibility of HAO having low calcification rates is likely, as it is missing a valuable nutrient source (Fig. 6). Due to the high distribution coefficient of manganese, Rayleigh fractionation might add an additional control on Mn $/$ Ca ratios in the foraminifera shell (Holland et al., 2017). The model of Rayleigh fractionation relies on a number of assumptions about the internal reservoir of the foraminifera regarding the size, initial composition, refreshment rate and calcification rate (Elderfield, 1996). As these parameters are not fully understood, both for H. sarcophaga and foraminifera in general, we cannot provide further information about the possible influence.

A significant influence of the potentially Mn-enriched bodily fluids of bivalves (Wada and Fujinuki, 1976) also cannot explain the differences in the chemical composition as the samples that discern from the others are picked from HAO. These foraminifera did not have access to the internal organic material of the bivalve (Fig. 6a4). Instead, the high Mn signal in HAO must derive from a source that is located on the outside of the bivalve host (Fig. 6a2). When the foraminifera initially infests the bivalve and starts boring into the shell, nutrient sources other than the internal organic parts of the bivalve have to be utilized by H. sarcophaga. The organic periostracum of the bivalve could depict this nutrient source as it is a highly nutritional source for organic material on the outside of the bivalve's shell (Secor et al., 1993). High concentrations of Mn and Fe were measured in the periostracum of freshwater and marine bivalves (Swinehart and Smith, 1979; Allen, 1960). The mechanistic explanation for this enrichment of Mn and Fe is reported to be the high amount of the amino acids containing glycine and tyrosine in the periostracum of bivalves (Piez, 1961; Whitney et al., 2019), which act as complexing sites for metal ions (Swinehart and Smith, 1979). The existence of living H. sarcophaga attached to rocks demonstrates that they do not necessarily rely on a living host but can also supply themselves through other feeding strategies (Cedhagen, 1994). Since algae take up Mn and concentrate it internally (Sunda and Huntsman, 1985), the increased Mn $/$ Ca in HAO could also be caused by a facultative suspension-feeding mode of H. sarcophaga during its juvenile stage.

At this point we can only speculate about the mechanistic explanation for the enrichment of Mn $/$ Ca in HAO. Future research on H. sarcophaga should involve spatially resolved Mn and Fe measurements to explore if there is an ontogenetic decrease in Mn $/$ Ca ratios in the test of H. sarcophaga picked from A. excavata. This decrease would mark the time of the first penetration of the bivalve shell.

4.5 Carbonate isotopic composition in H. sarcophaga based on the host organism

The oxygen and carbon isotopic composition of the different organisms are characterized by large differences. A. excavata does not show signs of kinetic effects, which would be indicated by a correlation of δ¹³C and δ¹⁸O values (McConnaughey, 2003; Adkins et al., 2003; Bajnai et al., 2018). Bivalves are largely considered to calcify in equilibrium with the surrounding water (Immenhauser et al., 2016), which appears to be valid for A. excavata as it displays an isotopic composition close to the expected equilibrium (Fig. 8). The host organism D. pertusum displays higher departures from the expected aragonite equilibrium, which is mainly caused by additional incorporation of isotopically lighter, metabolic CO₂ and by kinetic isotope effects associated with hydration/hydroxylation reactions given that this coral raises the calcification site pH to values significantly exceeding seawater pH (Chen et al., 2018; McCulloch et al., 2012).

Figure 8 δ¹⁸O plotted against δ¹³C for H. sarcophaga from different host organisms and the host organisms A. excavata and D. pertusum with a 95 % confidence ellipse. Arrows show compositional changes induced by kinetic effects and respiration. Text below the horizontal lines in the legend is the host organism that H. sarcophaga grew on. Red points show the equilibrium composition for calcite and aragonite as calculated from the isotopic composition of the ambient seawater.

Interestingly, the HA samples display an isotopic composition very similar to the composition of its host organism (Fig. 8). The 95 % confidence ellipsoids of HAW, HAO and A. excavata all overlap at the highest δ¹⁸O values. However, in contrast to A. excavata, HAW and HAO display positive correlations between δ¹⁸O and δ¹³C. This may indicate that all three organisms closely mineralize their carbon from the same source, but hydration/hydroxylation kinetics occur more pronounced in HAW and HAO relative to A. excavata.

The observable differences in the carbon isotopic composition between HA and HL can also be caused by different proportions of the carbon sources. HL presumably have constant access to the host's carbon pool, whereas the access of HA to the host's carbon pool is limited due to the defense mechanism of A. excavata (Fig. 3). When the bivalve has successfully closed the boring of the foraminifera, the foraminifera must use seawater DIC as a carbon source until it penetrates the shell again. This mixing of different carbon sources in HA in contrast to the stable carbon source of HL can explain the lower δ¹³C values in HL due to an increased influence of host-derived carbon.

HL is characterized by significantly more positive δ¹⁸O values than its host and is also characterized by a slightly steeper positive correlation between δ¹³C and δ¹⁸O. Both circumstances point to faster hydration/hydroxylation kinetics to be effective during the mineralization of HL compared to its host (Chen et al., 2018). If the pH at which HA precipitates carbonate is lower than the pH of the calcifying fluid in D. pertusum, the hydration kinetics would be accelerated as a result (Raddatz et al., 2014; Cohen, 2003; Crenshaw, 1972). Both organisms may derive their carbon from the same source, which likely occurs depleted in ¹³C relative to seawater, possibly due to significant admixture from metabolic CO₂. This assertion is supported by the fact that HL has constant access to the host's carbon pool.

Another mechanism potentially altering the δ¹³C from equilibrium might be the etching mechanism that pumps H⁺ ions in the ambient water around the foraminifera (Toyofuku et al., 2017). The decreasing pH around the foraminifera shifts the carbon speciation towards CO₂. As CO₂ is depleted in ¹³C compared to the total inorganic carbon pool, the utilization of CO₂ for calcification would also explain the deviations of the foraminifera's shell δ¹³C from isotopic equilibrium (Toyofuku et al., 2017; McCorkle et al., 1997).

4.6 Implications for paleoceanographic reconstructions

The results presented here have implications for paleoreconstructions in two ways. When using bivalves for paleoreconstructions or geochemical investigations in general, the shells must be carefully examined for potential traces of bioerosion. In case of callus formation, the carbonate formed can have a significantly different composition than the original carbonate mineralogy.

Even more critical are the implications for paleoceanographic reconstructions using foraminifera, which are regularly analyzed for this purpose. Several foraminifera species are known to live on different host organisms and act as parasites and/or bioeroders (Walker et al., 2017; Dupuy et al., 2010; Freiwald and Schönfeld, 1996). Some of these are also used for isotope- and element-based paleoenvironmental reconstructions or geochemical investigations in general, such as Cibicides refulgens (Mackensen and Nam, 2014; Rathburn and de Deckker, 1997; García-Gallardo et al., 2017), Hanzawaia concentrica (Smith and Emiliani, 1968) and Discanomalia coronata (Baranwal et al., 2014).

As an example, we use a δ¹⁸O-temperature conversion formula for benthic foraminifera (Marchitto et al., 2014) and our measured δ¹⁸O ratios to reconstruct a temperature for the Leksa Reef of 7.5 ^∘C using HAO and 7.8 ^∘C using HAW with δ¹⁸O_SW derived from seawater measurements. In situ measurements of the water temperature in the Leksa Reef by CTD show a mean temperature of 7.8 ^∘C (minimum = 7.1 ^∘C, maximum = 8.8 ^∘C) (Büscher, 2018). If we, however, were to use δ¹⁸O ratios from HL, we would reconstruct a water temperature of 8.8 ^∘C and consequently overestimate the water temperature by 1.0 ^∘C.

If the aforementioned species show similar host-specific alterations of their isotopic and elemental composition, paleotemperature reconstructions on the basis of these species could be biased. Given that our results indicate that host-specific isotopic and elemental composition changes can be present in the parasitic foraminifera H. sarcophaga, we draw attention to other parasitic foraminifera that should be investigated for similar host–parasite relations, especially if they are used for geochemical investigations.

4.7 Chemical composition of H. sarcophaga compared to other benthic foraminifera

H. sarcophaga displays significantly higher Mg $/$ Ca ratios than most other benthic foraminifera species with comparable ecology, which show Mg $/$ Ca ratios between 0.5 and 10 mmol mol⁻¹ (Lear et al., 2002). Foraminifera that have comparable Mg $/$ Ca ratios to H. sarcophaga include Amphistegina (23–77 mmol mol⁻¹; van Dijk et al., 2019; Raja et al., 2005; Geerken et al., 2018), Quinqueloculina (50–135 mmol mol⁻¹; Gussone et al., 2016; Toyofuku et al., 2000) and Pyrgo (4–85 mmol mol⁻¹; Gussone et al., 2016), but these species are biologically and mineralogically distinct from H. sarcophaga. Quinqueloculina and Pyrgo are porcelaneous, whereas H. sarcophaga is hyaline. Furthermore, H. sarcophaga is not inhabited by photosymbionts, in contrast to Amphistegina.

The exact processes involved in ion transportation, seawater vacuolization and pH regulation utilized by H. sarcophaga remain to be discovered. High Mg $/$ Ca ratios in H. sarcophaga that are similar to inorganic precipitated calcite (Oomori et al., 1987; Mucci and Morse, 1983) may indicate a calcification mechanism without ways of discriminating against elements such as magnesium. These species rely on an increase in the calcification site pH (Erez, 2003; de Nooijer et al., 2009; Toyofuku et al., 2017) to facilitate calcification. The main control on calcite Mg $/$ Ca ratios is then provided by the composition of the calcifying fluid (Raitzsch et al., 2010). The high Mg content would therefore indicate a calcifying space that is more similar to ambient seawater, i.e. with no or minor modification via ion channels or pumps (de Nooijer et al., 2014; Bentov and Erez, 2006). Additionally, high Mg $/$ Ca ratios in the calcifying space might be necessary for the stabilization of ACC (amorphous calcium carbonate), a suggested metastable calcite precursor phase in foraminifera and other calcifying organisms (Addadi et al., 2003; Jacob et al., 2011, 2017). High amounts of Mg in the calcite can also cause lattice strain effects, due to the size difference of Mg and Ca ions that causes lattice distortion (Evans et al., 2015; Mucci and Morse, 1983). The lattice distortion can cause an increased incorporation of elements such as Sr and Na (Mucci and Morse, 1983; Evans et al., 2015), a feature that we observe in our samples compared to the species A. lessonii, which has slightly lower Mg $/$ Ca ratios than H. sarcophaga (35 vs. 45 mmol mol⁻¹) and consequently lower Na $/$ Ca and Sr $/$ Ca ratios (Geerken et al., 2018).

4.8 Biomineralization in the callus region

In order to protect itself from the parasitizing foraminifera, A. excavata seals the canal etched through the shell. This is accomplished by rapidly calcifying over the foraminifera boring (Beuck et al., 2008; Cedhagen, 1994). The calcification process produces a callus on the inside of the bivalve shell that is 3–5 mm in diameter and 1–2 mm in height. In the SRZ, evidence can be found for the biomineralization model for bivalves proposed by Addadi et al. (2006), Checa et al. (2005), and Wada and Fujinuki (1976), i.e. that this process starts with the formation of an organic sheet indicated by the high fluorescence, high S concentration and low Ca concentration of this region, which then acts as a framework during calcification. The following layer is depleted in S and enriched in Ca and therefore represents a higher Ca concentration (Figs. 3 and 4). This sequence is repeated multiple times, leading to the formation of the visible callus. As long as the foraminifera does not stop the boring process, the bivalve needs to continually counter the boring process by calcifying in the region of infestation.

The callus displays high concentrations of organic material that are not observable in the undisturbed regions. The layers that are characterized by high organic contents appear to be preferentially dissolved (Fig. 3b). In cross sections, organic-rich areas make up 50 % of the callus (Fig. 1D). It appears unlikely that the high amounts of organic material in the SRZ are solely deposited as a calcification framework, considering the differences between undisturbed shell areas and the SRZ. Therefore, the high amount of deposited organic material probably serves some other purpose, such as an increase in the overall material deposition rate and the provision of an initial sealant from the surrounding water.

The boring organisms pose a threat to the bivalve in multiple ways. It has been shown that H. sarcophaga penetrated the mantle of A. excavata, which led to a destruction of the mantle epithelium of the bivalve due to ingestion by H. sarcophaga (Cedhagen, 1994). Infested sections showed larger numbers of cell nuclei, indicating higher cell division rates and higher metabolic rates (Cedhagen, 1994). The pathway through the bivalve shell furthermore allows pathogens to reach and attack the bivalve and could allow surrounding water to permeate into the extrapallial fluid (EPF) of the bivalve. Even though the EPF in several bivalve species shows trace element concentrations close to seawater (Wada and Fujinuki, 1976; Crenshaw, 1972), the bivalve still has to actively concentrate Ca in the calcifying space to reach concentrations that exceed the solubility product (Wilbur and Saleuddin, 1983; Wheeler, 2020). This concentration of Ca is accomplished through active pumping by means of enzymes such as Ca-ATPase (Klein et al., 1996) or through ion channels (Carré et al., 2006). In the case of an unsealed calcifying space, the dilution with seawater makes high concentrations of Ca ions to levels needed for calcification in the extra EPF less likely. A fast-sealing method, by means of organic deposition, is therefore necessary to ensure that the bivalve's calcification capability is not compromised.

Geochemically, the SRZ shows the largest differences compared to the undisturbed aragonite in Mg $/$ Ca and Sr $/$ Ca ratios (Figs. 2 and 3). Mg $/$ Ca ratios are 5 times higher in the SRZ than in undisturbed aragonite. Magnesium is thought to be enriched in organic matrices secreted by the bivalve compared to the shell CaCO₃ (Schöne et al., 2010). The distribution of magnesium in the SRZ, especially its enrichment in fluorescent layers rich in sulfur (Figs. 1, 3 and 4), makes an enrichment of Mg due to high organic concentrations likely. Beside an enrichment of Mg in the secreted organic matter, peptides similar to that found at the site of calcification in bivalves (Moradian-Oldak et al., 1990) can increase the Mg concentration in precipitated calcite by reducing the dehydration enthalpy (Stephenson et al., 2008). These peptides are also regularly found in molluscs (Marin et al., 2007; Falini et al., 1996; Halloran and Donachy, 1995; Zhang and Zhang, 2006). As these peptides do furthermore increase the growth rate by 25 % to 50 % (Stephenson et al., 2008), due to the need of fast calcification (Beuck et al., 2008), it may suggest that a high concentration of peptides in the SRZ is likely. Higher growth rates can additionally lead to an increase in crystal impurities, which could alter other elements besides Mg (Lorens, 1981).

In contrast to Mg, Sr was not found to be enriched in organic matter compared to shell CaCO₃ (Takesue et al., 2008), and therefore the presence of organics cannot explain the observed high Sr $/$ Ca of the aragonite in the SRZ. Yet, there is evidence for the influence of peptides on the incorporation of other elements such as Sr (Stephenson et al., 2008). Sr incorporation in the aragonitic bivalves is considered to be controlled in part by growth rate effects (Lorrain et al., 2005; Füllenbach et al., 2017; Takesue et al., 2008; Carré et al., 2006). A calcification rate control on Sr incorporation is also supported from abiogenic calcite (Gabitov et al., 2014) but not from abiogenic aragonite (Gabitov et al., 2006). Accordingly, this growth rate effect is probably of biologic nature in aragonite precipitates.

Sr likely arrives into the calcifying space via similar pathways as Ca, as was shown by the effects of calcium channel blockers in corals (Ferrier-Pagès et al., 2002). However, Ca-ATPase has a higher affinity for Ca than Sr (Yu and Inesi, 1995). Therefore, a higher Ca-ATPase activity, as a result of increased growth rates, should lead to decreasing Sr $/$ Ca ratios in the precipitates, which was shown in corals (Ferrier-Pagès et al., 2002; de Villiers et al., 1995). As we expect high growth rates in the SRZ, Ca channels that also transport Sr cannot explain the observed Sr distribution in this zone. Alternatively, the organism's metabolic rate has been suggested to control Sr $/$ Ca in bivalves through metabolic pumping (Klein et al., 1996). High metabolic activity was observed in A. excavata infested by H. sarcophaga, indicated by a high concentration of cell nuclei (Cedhagen, 1994). The model of Klein et al. (1996) would predict lower Sr $/$ Ca ratios in these areas; thus, a mechanism other than metabolic pumping must control the high Sr $/$ Ca ratios in the SRZ.

Füllenbach et al. (2017) proposed that in slow-growing areas of bivalves, the organisms exert less biological control over element incorporation, leading to elevated Sr $/$ Ca ratios. While this hypothesis does not fit our observation of elevated Sr $/$ Ca ratios in a potentially fast-growing shell area, a similar hypothesis was suggested concerning Mg $/$ Ca in Mytilus edulis (Lorens and Bender, 1980). The authors found strongly elevated Mg $/$ Ca ratios in shell sections that were precipitated after handling the specimens for size measurements and attributed this effect to stress (Lorens and Bender, 1980). The boring of H. sarcophaga is very likely to be a stress factor on A. excavata. An influence of such stress-related effects on Mg $/$ Ca and potentially Sr $/$ Ca (Fig. 4) is, therefore, possible. The high Mg concentrations in the EPF due to a potential breakdown of Mg-regulating mechanisms, however, would inhibit the organism from calcification due to the inhibiting effects of Mg on crystal nucleation and growth (Pytkowicz, 1965; Lorens and Bender, 1980). A. excavata might circumvent this by releasing additional sulfate-bearing organic molecules that provide additional nucleation sites and higher Ca concentrations at the nucleation sites (Lorens and Bender, 1980), which might potentially be the cause of the observed increased S $/$ Ca ratios in the SRZ (Fig. 4).

5 Conclusion

Our results demonstrate that the elemental and isotopic composition of the parasitic foraminifera H. sarcophaga varies depending on the host organisms that the foraminifera settle on. H. sarcophaga that lived on the coral D. pertusum shows significantly higher Sr $/$ Ca ratios than those that lived on the bivalve A. excavata. Combining these data with a simple mixing model, we propose that this could point towards a biomineralization pathway that is influenced by uptake of carbonate material derived from the host. The dissolution of the host shell could serve to satisfy the foraminifera's demand for calcium and DIC.

We also observe significant differences between H. sarcophaga specimens that grew on A. excavata that can be correlated to the success of the penetration progress. Foraminifera that fully penetrated the bivalve's shell, recognizable by the hosts callus formation, display significantly lower Mn $/$ Ca ratios than foraminifera that did not completely penetrate the shell. This could be an effect of a suspension-feeding period of the foraminifera or grazing of Mn-rich material of the periostracum until it penetrated the bivalve's shell when switching to a parasitic mode of feeding. Other possibilities include differences in the growth rate caused by changes in the nutrient availability or Rayleigh fractionation.

The oxygen and carbon isotopic composition of H. sarcophaga also appears to be influenced by the type of host organism that it infests. Again, this might be an effect of a direct uptake of the host's organic material and/or CaCO₃. Other effects such as different pH regimes in the host organisms and varying equilibration may also play a role. Different extents of the calcification site carbonate system equilibration between H. sarcophaga that infested D. pertusum (HL) and H. sarcophaga that infested A. excavata (HA) could also explain the missing signs of kinetic fractionation in HL compared to HA.

As the elemental and isotopic composition of some parasitic foraminifera is used for paleoceanographic reconstructions, our results indicate that such studies should only be performed when the host organism is known.